Il contributo della geologia alla comprensione dei terremoti

SESSIONE 1
Il contributo della geologia alla comprensione dei
terremoti
CONVENERS
Fabrizio Galadini (INGV Milano)
Paolo Boncio (Università degli Studi “G. d'Annunzio” Chieti)
Alberto Pizzi (Università degli Studi “G. d'Annunzio” Chieti)
Michele Saroli (Università degli Studi di Cassino)
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SESSIONE 1

SESSIONE 1
Struggling from surface observations to seismogenic structures, and
the contribution of seismic reflection profiles
Key words: Active tectonics, earthquake geology, seismogenic
structures, seismic reflection profiles.
INTRODUCTION
Field geology data can greatly help defining the parameters
that characterize active faults. Features like fault direction, fault
length, and fault segmentation can often be constrained by careful
field studies (eg., GALLI &BOSI, 2003). These studies are of
paramount importance in paleoseismology, particularly as a way
to assess the recurrence time interval of larger earthquakes.
However, they address only the surface expression of tectonic
processes that affect the upper kilometers of the Earth crust. On
the other hand, earthquakes, particularly those of larger
magnitude, tend to originate near the base of the brittle crust
(MARONE &SCHOLZ, 1988). Therefore, the link between the
seismogenic fault, located at some kilometers depth, and its
surface expression is not always straightforward. The finding that
in several instances, particularly in compresissonal regime,
active faults can be blind (e.g., MYERS et alii, 2003) adds further
complexities, sometimes resulting in poorly constrained inference
on the seismogenic source. Data on fault length and fault slip can
be used to define the seismogenic source. However, simplified
fault slip models are usually adopted to fit surface observation,
and the result is greatly affected by the quality and spatial
coverage of available constraints.
The seismicity of the Italian region has been well defined by
20 years of instrumental rcording by the INGV seismic network
(CHIARABBA et alii, 2005). Active tectonics occurs with a variety
of structural styles, but deformation rates are rather low,
(VANNUCCI et alii, 2004; SERPELLONI et alii, 2007), for instance
with respect to the Anatolian and Aegean regions; therefore, the
geomorphological/stratigraphic signal of blind faulting can be
subdue, particularly when competing with processes like
differential compaction, gravitational adjustments and fluid
escape.
_________________________
(*) ISMAR-CNR, Bologna, andrea.argnani@ismar.cnr.it
ANDREA ARGNANI (*)
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SOME EXAMPLES
Examples illustrating some of the open and debated issues
concerning active tectonics in the Italian region will be presented,
with particular emphasis on case studies from marine areas. Three
examples of marine areas characterized by large historical
earthquakes are briefly introduced in the followings.
Peri-Gargano region - Seismic data support the conclusion
that the Pliocene-Quaternary deformation offshore of the
Gargano Promontory is progressively localized along a narrow E-
W belt in the South (ARGNANI et alii, 2009a) and along a NE-SW
belt in the North (ARGNANI et alii, 2002), whereas in the same
time span the whole of the Gargano Promontory has been
uplifted. The Present-Day deformation around the Gargano
Promontory is mainly restricted to the regions located to the N-
NE of the promontory. Deformation is typically rather diffuse and
of limited extent; basement was likely involved, as suggested by
both depth of earthquakes and trends of the structures, that bear
little relationship with those of the adjacent fold and thrust belts.
Compressional reactivation of extensional Mesozoic faults is
considered as the most likely mechanism for Neogene
deformation. Messina Straits – In the Messina Straits it is difficult
to find a single fault that is long enough to account for the Mw
7.1, 1908 Messina earthquake (ARGNANI et alii, 2009b, and
references therein). Moreover, the trend of the observed faults,
though consistent with faults onshore Calabria, is different from
the trend of many of the faults proposed on the basis of inversion
of seismological and geodetic data. Seismic data show that there
is no N-S fault cutting the sedimentary successions south of the
epicenter the 1908 earthquake. In fact, the only long fault that is
cutting the sea floor is located at the SW tip of Calabria, trends
NW-SE and dips to the west with a low angle. Such fault
parameters are not compatible with the 1908 earthquake, as the
hypocentral depth would be located too far to the west. A system
of interconnected faults, partly exploiting pre-existing fault
planes, can better describe the observed geological (i.e., long
term) deformation; an interpretation that leaves the possibility to
have more than a fault active at the same time. At present it is
difficult to say whether the observed active faults are just the
surface expression of a single, deeper and blind seismogenic
fault, or if they truly represent the complex response of an area
where more than one fault can be active at the same time. The

large magnitude of the 1908 earthquake makes the first
hypothesis perhaps more appealing.
Eastern Sicily - Oceanic lithosphere has been subducted under
the Calabrian Arc during the opening of the Tyrrhenain backarc
basin. A narrow, 200 km wide, oceanic slab is still present
underneath Calabria, and the Calabrian Arc accretionary prism
currently covers most of the Ionian Sea. Megathrusts originating
large magnitude earthquakes have been shown to characterize the
subduction interface of several Pacific plate boundaries
(HYNDMAN et alii, 1997). Large historical earthquakes have been
reported in the regions around the Ionian Sea, particularly in
eastern Sicily, often with associated tsunamis (LORITO et alii,
2008). The January 1693 earthquake, possibly the largest known
Italian earthquake (CPTI, 2004), has been recently attributed to a
subduction fault plane (GUTSCHER et alii, 2006); modelling of the
related tsunami, however, show waves which are larger in
Calabria than in eastern Sicily, unlike historical records (TINTI &
ARMIGLIATO, 2003). The attribution of the January 1693
earthquake to the extensional faults located offshore of eastern
Sicily (ARGNANI & BONAZZI, 2005; ARGNANI, 2009) seems
therefore to be preferred, as also tsunami modelling better fits the
observations (ARGNANI et alii, 2004). It should be mentioned,
however, that the 1693 earthquake has been located on land,
according to other authors (see reviews in the DISS web site
http://diss.rm.ingv.it/diss/), just to highlight the degree of
uncertainty.
REFERENCES
ARGNANI A. (2009) - Evolution of the southern Tyrrhenian slab
tear and active tectonics along the western edge of the
Tyrrhenian subducted slab. In: Van Hinsbergen D. J. J.,
Edwards M. A. and Govers R. (Eds) - Collision and Collapse
at the Africa–Arabia–Eurasia Subduction Zone. Geol. Soc.,
London, Spec. Publ., 311, 193–212.
ARGNANI A. & BONAZZI C. (2005) - Tectonics of Eastern Sicily
Offshore. Tectonics, 24, doi:10.1029/2004TC001656.
ARGNANI A., BONAZZI C. & COSTA PISANI P. (2002) - Neogene
deformation in the central Adriatic Sea. RealMod 2002, 2-4
October 2002, Milano, 135-138.
ARGNANI A., ROVERE M. & BONAZZI C. (2009a) - Tectonics of
the Mattinata Fault offshore south Gargano (southern
Adriatic Sea, Italy): implications on active deformation in the
foreland of the Southern Apennines. G.S.A. Bull., 121, 1421-
1440.
ARGNANI A., TINTI S., ARMIGLIATO A&BONAZZI C. (2004) -
Neotectonics and tsunamigenic potential of the Eastern Sicily
Escarpment. Riassunti GNGTS, 2004, Roma.
3
ARGNANI A., BRANCOLINI G., BONAZZI C., ROVERE M, ACCAINO
F., ZGUR F. & LODOLO E. (2009b) - The results of the
Taormina 2006 seismic survey: Possible implications for
active tectonics in the Messina Straits. Tectonophysics, 476,
159-169.
CHIARABBA C., JOVANE L. & DI STEFANO R. (2005) - A new view
of Italian seismicity using 20 years of instrumental
recordings. Tectonophysics, 395, 251– 268.
GALLI P. & BOSI V. (2003) - Catastrophic 1638 earthquakes in
Calabria (southern Italy): New insights from
paleoseismological investigation. J. Geoph. Res., 108,
doi:10.1029/2001JB001713.
CPTI (2004) - Catalogo Parametrico dei Terremoti Italiani,
versione 2004 (CPTI04). INGV, Bologna.
http://emidius.mi.ingv.it/CPTI/.
GUTSCHER M.-A., ROGER J., BAPTISTA M.-A., MIRANDA J.M. &
TINTI S. (2006) - Source of the 1693 Catania earthquake and
tsunami (southern Italy): New evidence from tsunami
modeling of a locked subduction fault plane. Geoph. Res.
Lett., 33, doi:10.1029/2005GL025442.
HYNDMAN R.D., YAMAN M. & OLESKEVICH D.A. (1997) – The
seismogenic zone of subduction thrust faults. The Island Arc,
6, 244-260.
LORITO S., TIBERTI M.M., BASILI R., PIATANESI A. & VALENSISE
G. (2008) - Earthquake-generated tsunamis in the
Mediterranean Sea: Scenarios of potential threats to
Southern Italy. J. Geoph. Res., 113,
doi:10.1029/2007JB004943.
MYERS D.J., NABELEK J.L. & YEATS R.S. (2003) – Dislocation
modelling of blind thrusts in the eastern Los Angeles basin,
California.. J. Geoph. Res., 108, doi:10.1029/2002JB002150.
MARONE C. & SCHOLZ C.H. (1988) – The depth of seismic
faulting and the upper transition from stable to unstable slip
regime. Geoph. Res. Lett., 15, 621-624.
SERPELLONI E., VANNUCCI G., PONDRELLI S., ARGNANI A.,
CASULA G., ANZIDEI M., BALDI P. & GASPERINI P. (2007) –
Kinematics of the Western Africa-Eurasia plate boundary
from focal mechanisms and GPS data. Geophys. J. Int, 169,
1180-1200.
TINTI S. & ARMIGLIATO A. (2003) – The use of scenarios to
evaluate the tsunami impact in southern Italy. Marine
Geology, 199, 221-243.
VANNUCCI G., PONDRELLI S., ARGNANI A., MORELLI A.,
GASPERINI P. & BOSCHI E. (2004) - An Atlas of
Mediterranean Seismicity. Annali di Geofisica, suppl. vol. 47,
247-306.
SESSIONE 1

SESSIONE 1
Key words: Abruzzo, earthquake, L’Aquila, microzonation.
INTRODUCTION
The April 6 th , 2009 L’Aquila earthquake (5.8 Richter
magnitude) caused severe damage to many ancient hill towns in
the region, killing 308 residents, injuring about 11,600 and
leaving about 65,000 homeless. Owing to an agreement between
the Italian Civil Protection National Service, the Tuscany
Regional Service for Seismic Prevention and the Earth Sciences
Department of the Pisa University, the seismic microzonation of
an area south-west of L’Aquila was performed.
The study focused on the area including some of the most
damaged villages, such as Bagno, Civita di Bagno, San Benedetto
Fig. 1 - Destruction at San Benedetto.
_________________________
The 2009 L’Aquila earthquake (Central Italy):
seismic microzonation of a severely hit area
MASSIMO BAGLIONE (*), GIACOMO D’AMATO AVANZI (**), VITTORIO D’INTINOSANTE (*), PIERANGELO
FABBRONI (*), ROBERTO GIANNECCHINI (**), DARIA MARCHETTI (**), ALBERTO PUCCINELLI (**),
ANDREA SALVETTI (**) & GIUSEPPE TURRINI (**)
(*) Regione Toscana - Coordinamento Regionale Prevenzione Sismica,
massimo.baglione@regione.toscana.it
(**) Università di Pisa - Dipartimento di Scienze della Terra,
damato@dst.unipi.it
4
and Vallesindola (Fig. 1) where several people were killed.
INVESTIGATIONS AND RESULTS
Following the standards and guidelines for the seismic
microzonation issued by the Italian Civil Protection Department
(GRUPPO DI LAVORO MS, 2008) many investigation were carried
out: geologic and geo-engineering survey, geophysical
prospecting, instrumental registration, and geotechnical analyses.
Thus an underground model was defined and depicted by means
of representative geological-technical sections, suitable for the
subsequent modelling phase (FIANCHISTI et alii, 2009).
In the study area geological formations and Plio-Quaternary
continental deposits crop out.
- The former belong to the M. Ocre-Valle Aterno-M.
Camarda Succession and include (CENTAMORE et alii, 2006):
Calcareniti a Briozoi member: it crops out close to the Civita
Lake and is mainly formed of medium-thick strata of white or
grey calcarenite and calcirudite with Bryozoa (Langhian p.p. -
Serravallian). The rock is mainly strong and intersected by joint
sets with moderate spacing, high persistence, moderate to high
aperture and high roughness.
Sandstone-pelite turbidite succession: it crops out at Bagno
Grande and is formed of medium-thick, frequently massive
yellow sandstone with medium-thin pelitic interbeds
(sandstone/pelite > 2) (Lower Messinian p.p.). The rock is
medium strong and intersected by closely spaced, very persistent,
open, smooth or slightly rough, weathered and damp joints.
- The Plio-Quaternary continental deposits include the Aielli-
Pescina Supersynthem (Pliocene (?) - Middle Pleistocene)
gathering most of them, and the Holocene and Present deposits
(landslide bodies, debris, colluvium and alluvial deposits, etc.).
The following ones are most represented:
Fluvial-lacustrine deposits: they crop out close to the S.
Maniero lake and are formed by massive sand with pelitic
interbeds and lens-shaped conglomerate interbeds; these deposits
are very consistent and intersected by two wide-spaced joint sets.
Landslides: many landslides involve the slopes between
Bagno, Civita di Bagno and San Benedetto. Most of them are
dormant. Two coseismic landslides were identified: one on the
slope south-west of the San Maniero lake, the other in the upper
part of Bagno.

Fig. 2 - Geological-technical sections of the San Benedetto area.
Subsequently the underground model was defined and
depicted by means of representative geological-technical
sections, based on geological, geotechnical, geophysical and
seismological data. Fig. 2 shows the example of the San
Benedetto - San Maniero Lake area, where the Plio-Quaternary
deposits attain a great thickness and the bedrock is intersected by
normal faults.
Finally, 1st level and 3 rd level microzonation maps were
performed.
The 1st level map classifies the study area in three categories:
stable zones, stable but amplification subject zones, and
instability subject zones. This map roughly and qualitatively
identifies the areas that could be characterized by specific seismic
local effects.
Fig. 3 - 3rd level map of the San Benedetto area.
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The 3 rd level map, based on the knowledge of several data
(seismic input, geological-technical model and cross sections, in
situ and laboratory geotechnical data, geophysical and
seismological data), identifies homogeneous geologicalgeophysical
units and the related stratigraphic columns, on which
the modelling was performed. Fig. 3 shows the 3 rd level map of
the San Benedetto area.
REFERENCES
CENTAMORE E., CRESCENTI U. & DRAMIS F. (2006) - Foglio 359
L’Aquila e Note Illustrative. Dipartimento Difesa del Suolo -
Servizio Geologico d’Italia. Tip. S.El.CA. (FI), 128 pp.
FIANCHISTI G., BAGLIONE M., D’INTINOSANTE V., FABBRONI P. &
VANNINI F., Eds. (2009) - Microzonazione sismica della
Conca Aquilana (terremoto 06-04-2009). Relazione tecnica
finale di sintesi - Macroarea 9. Regione Toscana, Coord.
Regionale Prevenzione Sismica (unpublished).
GRUPPO DI LAVORO MS (2008) - Indirizzi e criteri per la
microzonazione sismica. Conferenza delle Regioni e delle
Province autonome - Dipartimento della protezione civile,
Roma, 3 Vol. e DVD, 518 pp
SESSIONE 1

SESSIONE 1
Key words: Active tectonics, Central Apennines, earthquake,
L'Aquila, morphotectonics.
In the Central Apennines, active extensional tectonics is
accommodated by a dense array of normal faults. Major tectonic
elements are typically located at the foot of fault escarpments,
tens of kilometres long and some hundreds of meters high.
Subordinate faults within major blocks produce additional
topographic irregularities (i.e. minor graben and fault scarps; Fig.
1; BLUMETTI et alii 1993; SERVA et alii 2002; BLUMETTI &
GUERRIERI, 2007).
During moderate to strong earthquakes (M>6) one or several
or all these faults can be rejuvenated up to the surface, and should
be therefore regarded as capable faults. Thus, their total throw is
the result of a number of surface faulting events over the last few
hundreds of thousands of years. This is true for landscapes that
have a “typical” earthquake magnitude (i.e. the earthquake
magnitude that better “characterizes” the local landscape; SERVA
et alii 2002) of either 6 or 7.
According to this model, in the L’Aquila region the seismic
landscape is the result of repeated magnitude 7 events (Fig. 1).
Thus, the maximum expected magnitude is around 7.
Nevertheless, smaller events like the April 6 th 2009 case are
frequent.
This assessment is confirmed by the historical seismicity
which has recorded in this area two events with Intensity X MCS
occurred on 1461, November 26 th and 1703, February 2 nd . Two
other destructive earthquakes hit the same area in 1349, IX-X
MCS, and in 1762, IX MCS.
Concerning the 1703, February 2 nd event, which was the third
major seismic event of a seismic sequence that in two weeks
shifted from Norcia to Montereale and finally to L’Aquila, a good
dataset of geological effects was provided by contemporary
reports (e.g. URIA DE LLANOS, 1703). This event produced about
20 km of surface faulting along the Pizzoli fault (offsets up to
about half a meter), and impressive secondary effects such as a
river diversion, huge deep-seated gravitational movements and
_________________________
Morphotectonics and seismic hazard in the L’Aquila basin
ANNA MARIA BLUMETTI (*),VALERIO COMERCI (*), PIO DI MANNA (*), LUCA GUERRIERI (*),
ALESSANDRO MARIA MICHETTI (**) & EUTIZIO VITTORI (*)
(*) ISPRA – Istituto Superiore per la Protezione e la Ricerca Ambientale -
Servizio Geologico d’Italia, annamaria.blumetti@isprambiente.it
(**) Dipartimento di Scienze Chimiche ed Ambientali - Università degli
Studi dell’Insubria
6
liquefaction phenomena involving the “ejection of stones and
whitish sulphureous water” along the Aterno River (BLUMETTI,
1995). Such evidence is in line with a characteristic set of ground
effects for magnitude 7 in the Apennines (e.g., PORFIDO et alii.,
2002) and therefore the 1703 event may be considered the typical
earthquake producing the seismic landscape in the L’Aquila
basin.
Instead, surface faulting related to the 2009 event was nearly
continuous along the Paganica Fault (BAGNAIA et alii, 1992) for a
length in the order of 2.6 km with offset not exceeding 10 cm
(BLUMETTI et alii, 2009). Only spot evidence of very small and
thin fractures was reported elsewhere, NW and SE of the village
of Paganica, both aligned or not to the Paganica fault ruptures.
Minor coseismic surface ruptures occurred also along the
Bazzano and Roio Faults. Secondary effects were mapped in an
area not larger than 1,000 km2 including gravitational
phenomena, most of them rock falls/avalanches and small slides,
the latter often affecting artificial material (BLUMETTI et alii,
2009).
Thus, in terms of characteristics and distribution of geological
effects, the 1703 earthquake intensity has been unquestionably
higher than that in the 2009 one (at least one degree, according to
the ESI intensity scale). As suggested by the local “seismic
landscape” and the historical record, the 2009, April 6 th
earthquake should not be seen as the maximum earthquake (e.g.
“characteristic”) expected in the L’Aquila region. Furthermore,
the paleoseismic record along the Paganica Fault has pointed out
the stratigraphic evidence of coseismic effects larger than those
produced in 2009.
Therefore, surface displacements along several capable faults
caused by moderate events should be seen as a typical feature of
the seismic landscape of the Central Apennines (cfr. the 1997,
September 26 th , Colfiorito earthquakes (Mw=5.6 and 6.0) and of
regions characterized by similar crustal extension.

Fig. 1 – 3D view of seismic landscape in the L’Aquila zone. The major faults are marked by up to a thousand meters high fault escarpments. Minor listric fault
within major blocks produce lower fault escarpments.
REFERENCES
BAGNAIA R., D’EPIFANIO A. & SYLOS LABINI S. (1992) – Aquilan
and subequan basins: an example of quaternary evolution in
central apennines, italy. Quaternaria Nova, 2, 187-209.
BLUMETTI A.M., DRAMIS F. & MICHETTI A.M. (1993) - Faultgenerated
mountain fronts in Central Apennines (Central
Italy); geomorphological features and seismotectonic
implications. Earth Surf. Proc. Land., 18, 203-223.
BLUMETTI A.M. (1995) - Neotectonic investigations and evidence
of paleoseismicity in the epicentral area of the January-
February 1703 Central Italy earthquakes. Bulletin of the
American Association of Engineering Geologists, Special
Volume n. 6: "Perspectives in Paleoseismology", Texas A&M
University, 7, 83-100.
BLUMETTI A.M. & GUERRIERI L. (2007) - Fault-generated
mountain fronts and the identification of fault segments:
implications for seismic hazard assessment. Boll. Soc. Geol.
It. (Ital.J.Geosci.), 126 (2), 307-322.
BLUMETTI A.M., COMERCI V., DI MANNA P., GUERRIERI L. &
VITTORI E. (2009) - Geological effects induced by the
L’Aquila earthquake (6 April 2009; ML=5.8) on the natural
7
environment. http://www.apat.gov.it/site/_files/Inqua/2009
_abruzzo_earthquake_report.pdf.
CHIARABBA, C.et alii (2009) - The 2009 L’Aquila (central Italy)
Mw 6.3 earthquake: Main shock and aftershocks. Geophys.
Res. Lett., 36, L18308.
DEMANGEOT J. (1965) - Géomorphologie des Abruzzes
Adriatiques. Mém. Doc. CNRS, Paris.
PORFIDO S., ESPOSITO E., VITTORI E., TRANFAGLIA G. MICHETTI
A.M., BLUMETTI A.M., FERRELI L., GUERRIERI L., & SERVA
L. (2003) - Areal distribution of ground effects induced by
strong earthquakes in Southern Apennines (Italy). Surv.
Geophys, 23, 529-562.
SERVA L. BLUMETTI A.M., GUERRIERI L. & MICHETTI A. M.
(2002) - The Apennine intermountain basins: the result of
repeated strong earthquakes over a geological time interval.
Boll. Soc. Geol. It. Special Volume 1, 939-946.
URIA DE LLANOS A. (1703) - Relazione overo itinerario fatto
dall’auditore Alfonso Uria del Llanos per riconoscere li
danni causati dalli passati terremoi seguiti li 14 Gennaro e 2
Febraro M.DCCIII. Stamperia Gaetano Zenobj, Roma.
SESSIONE 1

SESSIONE 1
Surface Fault Rupture Hazard Zoning: insights from the L’Aquila
2009 earthquake (Mw 6.3, central Italy)
Key words: Apennines of Italy, normal fault, seismic
microzoning, surface fault rupture hazard.
INTRODUCTION
Surface fault rupture hazard (SFRH) is a localized hazard due
to the breaching to the ground surface of the coseismic slip along
a fault during large earthquakes. This might offset, tilt, warp and
damage buildings sited across or in the vicinity of the fault trace.
Thought SFRH should be one of the most easily avoided seismic
hazard, being dependent on a well detectable geologic feature
(the trace of an active fault), the 2009 L’Aquila earthquake
(central Italy, Mw 6.3) demonstrates that we should make much
more efforts in this direction. Indeed, during the 2009
earthquake, normal surface faulting occurred across inhabited
areas (e.g., Paganica, San Gregorio), producing mild-to-moderate
damages on several facilities (pipelines, roads, highway) and
dwellings, also of very recent construction.
A reference point for actions aimed at mitigating the SFRH is
the Alquist-Priolo Earthquake Fault Zoning Act (A-P), which
was adopted by the State of California since 1972 (Bryan and
Hart, 2007). The A-P defines the Earthquake Fault Zones, that
are regulatory zones around the surface traces of active faults
within which fault rupture hazard may occur and detailed
investigations (geological, high-resolution geophysical,
paleoseismological) are required prior to building structures for
human occupancy. The A-P also defines a Fault Setback, that is
the distance from the trace of the ascertained active fault within
which critical facilities and structures designed for human
occupancy cannot be build. The minimum Fault Setback must be
50 feet (ca. 15 m), unless proven otherwise.
In Italy, there are not comparable regulations for planning and
controlling new or renewed constructions across or close to
active faults. The only regulatory notes addressing the problem
are the Guidelines and Criteria for Seismic Microzoning
(Working Group MS, 2008) which define specific micro-zones,
_________________________
PAOLO BONCIO (*), PAOLO GALLI (**), GIUSEPPE NASO (**) & ALBERTO PIZZI (*)
(*) Università “G. D’Annunzio” di Chieti–Pescara, Chieti,
pboncio@unich.it
(**) Dipartimento della protezione civile, Roma
8
named “Zones of Instability”, around active faults. But, there is
not distinction between Earthquake Fault Zones and Fault
Setbacks and general criteria in defining the shape and width of
the zones are not explicated.
In this note, we summarize the main geologic features of the
surface ruptures that occurred during the L’Aquila 2009 normal
faulting earthquake, with particular attention to the Paganica and
San Gregorio inhabited areas. The main purpose is to provide
insights on how field observations could be transferred into
possible general criteria for shaping zones of local SFRH along
Apennine-like active normal faults.
EARTHQUAKE FAULT ZONES AND FAULT SETBACKS
The data from the Paganica (Fig. 1a) and San Gregorio (Fig.
1b) faults are used here to propose criteria for shaping
Earthquake Fault Zones (EFZ) and Fault Setbacks (S).
The model of figure 1c might help in defining general criteria
appropriate for normal faults, that are the most widespread active
faults in Italy. We suggest that both the EFZ and S should be
asymmetrically shaped around the trace of the active fault, whit a
wider zone in the hanging wall compared to the footwall. This is
in agreement with the observation that usually fault ruptures
occur along the fault trace and in the hanging wall. This also
matches with the general geologic observation that the
deformation associated to a dip-slip fault mostly focuses in the
hanging wall block. The width of the main deformation zone
observed along the Paganica fault can be used for defining the
minimum S. The proposed S at the hanging wall (Shw in Fig. 1c)
is 40 m, which includes the belt of coseismic faulting and
fracturing (30-35 m) plus a possible error (5 m) in mapping the
ground ruptures. At the footwall, a general criterion should
include a cartographic error in locating the trace of the active
fault on topographic maps, even if the fault trace is certain. The
error in tracing the fault on a 1:5,000-scale topographic map can
be on the order of 5 m if the fault appears as a well defined fault
plane on lithified rocks; but, it can increase to 10-15 m (2-3 mm
on the map) if the fault appears as a degraded fault scarp on
poorly consolidated deposits, as frequently observed. Therefore
we propose a minimum footwall S (Sfw) of 15 m in order to
account for such an operational uncertainty. The choice of 15 m
is in line with most minimum S values adopted in the USA.

Fig. 1 – Sketches (not to scale) summarizing the occurrence of coseismic surface faulting/fracturing along the Paganica (a) and
San Gregorio (b) normal faults and proposal of general criteria (c to e) for shaping and sizing the Earthquake Fault Zones
(EFZ) and Fault Setbacks (S) at both the hanging wall (hw) and footwall (fw) of active normal faults; c) fault trace certainly
mapped; d) fault trace “bracketed” with a zone of geologic uncertain (g.u.); e) uncertain fault trace.
The EFZ should be wider than the minimum S. In fact, the
EFZ should be a zone mapped before any earthquake during
standard seismic microzoning actions and it should include all
the reasonably inferred fault rupture hazards, including both the
main fault and the possible active branches. Detailed
investigations prior to building structures for human occupancy
will define if there is additional hazard due to active branches or
not. If the active branches are present, they will be traced in
detail and the appropriate S will be defined. Using the Paganica
fault as an example, the associated EFZ must include both the
main deformation zone and the reactivated synthetic splays
located far from the fault trace (120-140 m). Therefore, the EFZ
should extend at the hanging wall of the main fault at least 150 m
(EFZhw in Fig. 1c). At the footwall, probably a width of 30 m is
sufficient for a fault trace certainly mapped (EFZfw in Fig. 1c).
In cases of uncertain fault traces, instead of using wider
EFZs, a “zone of geologic uncertainty” is needed. Figure 1d is an
example of a fault trace “bracketed” within a zone of geologic
uncertainty (g.u.). The resulting EFZ will be the sum of the
hanging wall EFZ and footwall EFZ described above to the width
of the zone of g.u.. In cases where the width of the area of g.u.
cannot be assessed (e.g., areas with flat topography), a possibility
is to adopt symmetric EFZs, centred on the most likely fault trace
9
and having the maximum width at both the hanging wall and
footwall (e.g., 150 + 150 m).
Considering the moderate magnitude (Mw 6.3) and small size
of the coseismic ground offset (max. 10-12 cm) of the L’Aquila
2009 earthquake, it is reasonable to consider this event close to
the lower boundary of the earthquakes able to rupture the ground
surface. This suggests that the dimensions of the EFZ and S
proposed above should be considered as minimum values for
normal faults in Italy.
REFERENCES
WORKING GROUP MS (2008) - Indirizzi e Criteri per la
Microzonazione Sismica. Conferenza delle Regioni e delle
Provincie autonome, Dipartimento della protezione Civile,
Roma, 3 vol. and Cd-rom.
SESSIONE 1

SESSIONE 1
Electrical tomography supporting the geological model for seismic
microzoning: application in the L’Aquila earthquake area
Key words: Abruzzo, electrical resistivity tomography,
microzonation.
INTRODUCTION
As a consequence of the 6th april 2009 Abruzzo earthquake
(Mw 6.3), the town of L’Aquila (Central Italy) and the
surrounding villages along the Aterno river valley suffered huge
damages with more than three hundred victims. After a first phase
devoted to emergency activities, National Department of Civil
Protection (DPC) planned extensive seismic microzoning studies
in various municipalities affected by serious damages related to
the earthquake; ISPRA was involved in coordinating the seismic
microzoning of two Macro-Areas (dr. Amanti M. e Cesi C.
coordinators) and executing geological surveys, geoelectrical
prospection and seismic geotechnical modeling. Within the
working group, the Geophysical Service of ISPRA designed and
performed, in a few months, geoelectrical surveys on ten sites
located in or close to the damaged municipalities surrounding
the earthquake epicentre.
This work concerns the application of geoelectrical resistivity
tomography (ERT) for geological characterization supporting
seismic microzoning studies. Some examples are showed, in
which ERT has led to a decisive improvement of knowledge of
geological setting and has contributed to the proper interpretation
of the geophysical passive seismic results, allowing the location
of subsequent geotechnical investigations also.
GEOLOGICAL FEATURES
The study sites were located toward the terminal portion of
_________________________
(*) I.S.P.R.A., Istituto Superiore per la Protezione e la Ricerca
Ambientale, valeria.eulilli@isprambiente.it
CLAUDIO CESI (*), VALERIA EULILLI (*) & LUCA MARIA PUZZILLI (*)
10
the tectonic depression hosting the high and medium Aterno
Valley for a length of about 30 km NW-SE direction, between the
structural units of the Gran Sasso in the north, and Velino Sirente
- Monti d'Ocre to south. As is well known, the depression has its
origin and development in post-orogenic tectonics that led to the
lowering of the structures and created conditions for significant
continental sedimentation extended throughout the Quaternary
(BOSI &BERTINI, 1970).
The tectonic unit of the Gran Sasso is characterized by
normal faults with NW-SE and EW direction which lower
structures toward SW and bound tectonic depressions located
immediately behind the frontal thrust. In turn Monti d'Ocre Unit,
bounded northward by the thrust Monte Cagno-Monti d'Ocre, is
characterized by direct faults NW-SE that displace compressional
structures, lowering them toward NE and generating a series of
elongated ridges in the Apennine direction. In this context an
important direct fault system, characterized by Quaternary
activity and probably still active, bounds the depression to the
northeast.
The studied areas have different geomorphological settings:
most inhabited were builted along a rock slope or foothill areas
(Stiffe, Valle Cupa, Arischia, Fossa, Casentino), else upon
plateau (Pedicciano) sometimes terraced (S. Demetrio): the
historic centre were generally those most damaged by earthquake,
but significant damage were also found in areas of newer
buildings such as in Arischia – via Macindole.
The perimeter established by DPC for seismic microzoning
studies was of relatively modest extension around historic centre
of each town, with the associated expansion areas that were
included in the study.
GEOELECTRICAL SURVEYS
In each site was carried out at least one multielectrode
geoelectric investigation, which always occurred within the
perimeters identified by DPC, as much as possible near the struck
town with the aim of the geological characterization (depth of
bedrock, geometry of sedimentary bodies, covers thickness, etc.).
Electrode configurations were chosen by combining the need
of obtaining information about lateral and vertical variations of
soil resistivity with the largest depth of investigation required,

Fig. 1 – Preliminary modelling along a fault scarp in San Demetrio ne’
Vestini (a), inversion of synthetic dataset (b) and the tomography obtained
after survey (c).
even along very uncomfortable slope with inclinations more than
34% (Stiffe).
Geoelectrical surveys were performed using a
georesistivimeter SYSCAL R2 equipped with 72 or 96 electrodes
equally spaced 5 meters: the length of profiles varies from 237.5
to 475 m, the depth of investigation from 40 to about 75 m. Very
often, in order to obtain a high quality S/N ratio (ZHOU et alii,
2003) during surveying even upon complex topography, data
were collected using two types of electrode configuration:
Wenner-Schlumberger and Wenner arrays. Only in Arischia, due
to the greater detail required, measurements were performed with
Wenner, Dipole Dipole and Pole-dipole arrays using electrode
distance of 2.5 meters. Data were subjected to qualitative analysis
directly in the field and then processed with software
Damaged building
Higly damaged building
Fig. 2 – High resolution tomographies collected in Arischia in the damaged
area of via Macindole
RES2DINV ® which provides further control over the quality of
measured dataset and take into account topographic modelling in
resistivity imaging inversion (LOKE , 2002).
(a)
(b)
(c)
11
RESULTS
In some areas, poor of geological outcrops and with a
flattening topography, the geoelectrical surveys led to a decisive
improvement of geological model, as in the area of Pedicciano
where only after ERT investigation the location and depth of the
borehole could be established. In the area of San Demetrio ne’
Vestini the target of ERT was to investigate the two main faults,
trending NNW-SSE, which play an important role in seismic risk
of this municipality: in this case ERT were carried out across
fault scarps after modelling (with RES2DMOD ® ) to evaluate the
best array to highlight electrical contrast between sedimentary
layers (Fig.1).
Moreover, in the area of Sant’Eusanio Forconese,
geoelectrical surveys contributed to the better interpretation of
single station HVSR measures and Seismic Arrays (ALBARELLO
et alii, 2010), whereas in Arischia three high resolution ERT,
carried out only few weeks after the 6th April 2009 mainshock,
highlighted high resistivity contrasts in the subsurface of via
Macindole damaged area. The geoelectrical survey contributed to
identify the existence of an ancient landslide (pre-Holocene?) on
which several damaged buildings were constructed (Fig. 2).
REFERENCES
ALBARELLO D., CESI C., EULILLI V., GUERRINI F., LUNEDEI E.,
PAOLUCCI E., PILEGGI D. & PUZZILLI L.M. (2010) – The
contribution of the ambient v ibration prospecting in seismic
microzoning: an example from the area damaged by the 6th
April 2009 L’Aquila (Italy) earthquake, submitted to
B.G.T.A.
BOSI C. &BERTINI T. (1970) - Geologia della Media Valle
dell'Aterno. Mem. Soc. Geol. It., 9, 719-777
DPC (2010) – La microzonazione sismica dell’area aquilana.
On line at http://www.protezionecivile.it/minisite/ index.php?
dir_pk=1275&cms_pk=17444
LOKE M.H. (2002) The use of constraints in 2D and 3D
resistivity modelling 8th EEGS-ES Meeting, Portugal, Sept.
2002
LOKE M.H. (2002) Topographic modelling in resistivity imaging
inversion 62nd EAGE Conference & Technical Exhibition
Extended Abstracts, D-2.
ZHOU B. & DAHLIN T. (2003) - Properties and effects of
measurement errors on 2D resistivity imaging surveying.
Near Surface Geophysics, 105, 105-117
SESSIONE 1

SESSIONE 1
Postseismic displacement field following the 6 April 2009 L’Aquila
earthquake: relations between non-permanent GPS stations
measurements and geological observations
LEONARDO DISPERATI (*), ALBERTO PIZZI (**), SALVATORE VIRDIS (°), ENRICO GUASTALDI (*), ANDREA
RINDINELLA (*), TOMMASO BIGIO (*), CARLO BONANNO (°°), FILIPPO BONCIANI (*), IVAN CALLEGARI (*),
ALICE CIULLI (*), DARIO FIRUZABADÌ (*), LUCA GRAZZINI (*), MATTEO LAPINI (°°),
FRANCESCA CHIARA PASCOLETTI (*), GIUSEPPE POMPOSO (**) & SILVIA RICCUCCI (*)
Key words: Active faults, CGTAbNET, non-permanent GPS
stations, postseismic deformation.
On April 6th, 2009 a wide area neighbouring L’Aquila town
(Abruzzo, Italy) was hit by an earthquake of magnitude Mw 6.3.
Large damages affected several infrastructures and buildings and
about 300 lives were lost. By processing permanent GPS stations
(PGPS) data (ANZIDEI et alii, 2009; CHELONI et alii, 2010;
CIRELLA et alii, 2009; SERPELLONI et alii, 2009) and SAR
imagery (ATZORI et alii, 2009; PAPANIKOLAOU et alii, 2010;
WALTERS et alii, 2009) some authors highlighted a dm-sized
ground deformation developed during the mainshock.
Aftershocks with Mw > 5 occurred within one week after the
mainshock, while tens of Mw>3 aftershocks were recorded within
three months (http://iside.rm.ingv.it/). Field observations allowed
to detect evidence for coseimic ground deformation in the form of
km-long fault and fracture zones, mostly reactivating pre-existing
known faults (e.g., EMERGEO WORKING GROUP et alii, 2009;
BONCIO et alii, 2010). Re-measurements of coseismic faults and
fractures during the first 45 days after the mainshock indicate an
average afterslip throw-rate ranging from 0.5 to 0.6 mm/day and
an average opening-rate ranging from 0.3 to 1 mm/day, along the
Paganica rupture zone (BONCIO et alii, 2010). In this framework
we built a network of non-permanent GPS stations (NPGPS)
within the L’Aquila area among Fucino plain, Gran Sasso massif
and Campotosto lake (the CGTAbNET), with the aim of
depicting the post-seismic ground displacement field until July
2009 and studying correlations with first-order geological
structures.
Compared to PGPS, NPGPS suffer from various sources of
error that should be accurately estimated and/or removed.
_________________________
(*) Università degli Studi di Siena, Centro di GeoTecnologie e
Dipartimento di Scienze della Terra, disperati@unisi.it
(**) Università “G. d'Annunzio” Chieti-Pescara, Dipartimento di
Geotecnologie per l’Ambiente ed il Territorio, pizzi@unich.it
(°) Università degli Studi di Sassari, Dipartimento di Scienze Botaniche,
Ecologiche e Geologiche, virdis@uniss.it
(°°) Ingeo Systems s.r.l. – Leica Geosystems S.p.A.
12
Nevertheless the latter provide data with high spatial density and
geometry which may be strictly tailored to the regional-local
geological framework (PESCI et alii, 2009). These characters
suggest that NPGPS may be particularly useful when cm-sized
signals can be expected, as it may be the case of afterslip
transient deformation along coseismic faults and fractures.
The CGTAbNET is made up of 68 stations spreading over a
1800 km 2 area. The average baselines length is 14 km.
Measurements were performed from 28th April to 30th July 2009
by means of 16 L1-L2 GPS receivers. For five stations (Fucino,
Isola del Gran Sasso, Cagnano, Campotosto, S. Demetrio ne’
Vestini), we performed continuous (24h/day) acquisition
throughout the fieldwork duration. We occupied the remaining
stations (15 occupations per station and 4 h duration as an
average) obtaining, for different epochs, measurements of
CGTAbNET subsets with varying spatial configuration and size.
These data were post-processed with the single baseline
approach, by using final precise ephemerides and including in the
analysis AQUI (http://www.epncb.oma.be) and INGP
(http://ring.gm.ingv.it) PGPS. Then, we performed minimally
constrained network adjustments (GRONTMIJ, 2008) of daily
solutions of the CGTAbNET. By weighted least square linear
regression, we obtained for the NPGPS, a) the average
planimetric (E, N) velocities relative to INGP, b) the velocity
error estimation. Estimated average 2D ground displacements for
the 30th April - 30th July 2009 time span are ca. 45 ± 8 mm/year.
Hence, these postseismic velocities are about one order greater
than those estimated by PGPS (ANZIDEI et alii, 2009; CAPORALI,
2003; CAPORALI et alii, 2003; PESCI et alii, 2009) in the Central
Apennines area for the 1996-2008 interseismic period.
The resulting ground displacement velocity map was finally
analysed within the geological framework of the study area and
compared to the ground deformation features collected in the
field until May 2009. The results could provide some information
about fault behaviour and postseismic deformation patterns both
in the near- and far-field of the activated fault. Namely, along the
coseismic rupture zones, the general patterns of postseismic and
coseismic displacements are quite similar. This can be explained
by coseismic and following aseismic slip with the same sense of

motion (NE to NNE extension) on the main fault (e.g., SHEN et
alii, 1994). Therefore, although L’Aquila earthquake
demonstrates that events of magnitude around 6.3 are capable to
produce coseismic surface faulting in the Apennines, significant
postseismic displacements suggest that strain was not completely
released during the mainshock in the shallow part of the activated
fault. Therefore total displacement on the fault must include a
significant amount of afterslip displacement. This information
may be of general interest for seismic hazard evaluation and
paleoseismological interpretations. GPS measurements showed
significant postseismic velocity rates also away of the rupture
zone. The CGTAbNET data allowed to recognize adjoining
zones, each one characterized by its own ground displacement
field, which seem to be bounded by active normal faults. We
explain this framework with a postseismic kinematic interaction
among the L’Aquila faulted block and the surrounding fault
blocks (e.g., blocks delimited by the Laga and Assergi faults).
REFERENCES
ANZIDEI M., BOSCHI E., CANNELLI V., DEVOTI R., ESPOSITO A.,
GALVANI A., MELINI D., PIETRANTONIO G., RIGUZZI F., SEPE
V. & SERPELLONI E. (2009) - Coseismic deformation of the
destructive April 6, 2009 L'Aquila earthquake (central Italy)
from GPS data. Geophys. Res. Lett., 36.
ATZORI S., HUNSTAD I., CHINI M., SALVI S., TOLOMEI C.,
BIGNAMI C., STRAMONDO S., TRASATTI E., ANTONIOLI A. &
BOSCHI E. (2009) - Finite fault inversion of DInSAR
coseismic displacement of the 2009 L'Aquila earthquake
(central Italy). Geophys. Res. Lett., 36.
BONCIO P., PIZZI A., BROZZETTI F., POMPOSO G., LAVECCHIA G.,
DI NACCIO D. & FERRARINI F. (2010) - Coseismic ground
deformation of the 6 April 2009 L'Aquila earthquake (central
Italy, Mw6.3). Geophys. Res. Lett., 37 (6).
CAPORALI, A. (2003) - Average strain rate in the Italian crust
inferred from a permanent GPS network - I. Statistical
analysis of the time-series of permanent GPS stations.
Geophys. Jour. Intern., 155 (1), 241-253.
CAPORALI A., MARTIN S. & MASSIRONI M. (2003) - Average
strain rate in the Italian crust inferred from a permanent GPS
network - II. Strain rate versus seismicity and structural
geology. Geophysical Jour. Intern., 155 (1), 254-268.
CHELONI D., AGOSTINO N.D., ANASTASIO E.D., AVALLONE A.,
MANTENUTO S., GIULIANI R., MATTONE M., CALCATERRA S.,
GAMBINO P., DOMINICI D., RADICIONI F. & FASTELLINI G.
(2010) - Coseismic and initial post-seismic slip of the 2009
Mw 6.3 L'Aquila earthquake, Italy, from GPS measurements.
Geophys. Jour. Intern., 181 (3), 1539-1546.
CIRELLA A., PIATANESI A., COCCO M., TINTI E., SCOGNAMIGLIO
L., MICHELINI A., LOMAX A. & BOSCHI E. (2009) - Rupture
13
history of the 2009 L'Aquila (Italy) earthquake from nonlinear
joint inversion of strong motion and GPS data.
Geophys. Res. Lett., 36.
EMERGEO WORKING GROUP: ALESSIO G., ALFONSI L., BRUNORI
C.A., CINTI F.R., CIVICO R., CUCCI L., D'ADDEZIO G., DE
RITIS R., FALCUCCI E., FRACASSI U., GASPARINI A., GORI S.,
LISI A., MARIANO S., MARIUCCI M.T., MONTONE P., NAPPI R.,
PANTOSTI D., PATERA A., PIERDOMINICI S., PIGNONE M., PINZI
S., PUCCI S., VANNOLI P., VENUTI A. & VILLANI F. (2010) -
Evidence for surface rupture associated with the Mw 6.3
L'Aquila earthquake sequence of April 2009 (central Italy).
Terra Nova, 22 (1), 43-51.
GRONTMIJ N.V. (2008) - MOVE3 User Manual V.4.0. Grontmij
Nederland bv, Roosendaal, The Netherlands, 55 p.
PAPANIKOLAOU I.D., FOUMELIS M., PARCHARIDIS I., LEKKAS E.L.
&FOUNTOULIS I.G. (2010) - Deformation pattern of the 6 and
7 April 2009, MW=6.3 and MW=5.6 earthquakes in L'Aquila
(Central Italy) revealed by ground and space based
observations. Nat. Hazards Earth Syst. Sci., 10 (1), 73-87.
PESCI A., TEZA G. & CASULA G. (2009) - Improving strain rate
estimation from velocity data of non-permanent GPS stations:
the Central Apennine study case (Italy). GPS Solutions, 13
(4), 249-261.
SERPELLONI E., DEVOTI R. & CAVALIERE A. (2009) - Analysis of
high-rate GPS data collected during the L'Aquila seismic
sequence. Convegno Nazionale GNGTS, 16-19 Novembre
2009, Trieste, Italy.
SHEN Z.-K., JACKSON D., FENG Y., CLINE M., KIM M., FENG P. &
BOCK Y. (1994) - Postseismic deformation following the
Landers earthquake, California, 28 June, 1992. Bull. Seism.
Soc. Am., 84, 780–791.
WALTERS R.J., ELLIOTT J.R., D'AGOSTINO N., ENGLAND P.C.,
HUNSTAD I., JACKSON J.A., PARSONS B., PHILLIPS R.J. &
ROBERTS G. (2009) - The 2009 L'Aquila earthquake (central
Italy): a source mechanism and implications for seismic
hazard. Geophys. Res. Lett., 36.
SESSIONE 1

SESSIONE 1
Key words: Brittle-ductile transition, normal fault, seismic cycle
thrust.
INTRODUCTION
We model a dip-slip fault cross-cutting the brittle upper crust
and the ductile lower crust. In the brittle layer the fault is assumed
to have stick-slip behaviour, whereas the lower ductile crust is
inferred to deform in a steady-state shear. The conflicting
behaviour of the two layers crossed by a seismogenic fault
predicts a strain partitioning at the brittle-ductile transition
(BDT), which is different in the extensional or compressional
settings. During the interseismic period, along a normal fault
there should form a dilated hinge at and above the BDT.
Conversely, an over-compressed volume should develop above
the thrust plane at the BDT. Along a normal fault the earthquake
is associated with the coseismic closure of the stretched hangingwall
generated during the interseismic period. Besides the shear
stress overcoming the friction of the fault, the brittle fault moves
when the weight of the hangingwall exceeds the strength of the
dilated band. Along a thrust fault, the seismic event is rather
associated with the sudden dilation of the previously overcompressed
volume in the hangingwall, a mechanism requiring
much more energy because generally done against gravity. The
motion of an active fault at the BDT can be compared to a spring
anchored to the ductile and brittle parts of the hangingwall.
During the interseismic period, along a normal fault the spring is
elongated, whereas it is compressed in the convergent setting.
During the coseismic stage, the two systems reverse, i.e., the
spring is compressed along a normal fault, while it is elongated
along a thrust.
The model predicts larger fluids discharge along a normal
fault due to coseismic secondary porosity decrease, and viceversa
along a thrust fault.
A model for the seismic cycle
CARLO DOGLIONI (*), SALVATORE BARBA (°) , EUGENIO CARMINATI (*) & FEDERICA RIGUZZI (°)
_________________________
(*) Università di Roma “La Sapienza”, carlo.doglioni@uniroma1.it
(°) INGV, Roma
14
We tested the opposite scenarios with two examples from the
Apennines and Taiwan. GPS data, fluid fluxes, energy dissipation
and strain rate analysis support these contrasting evolutions. Our
model also predicts, consistently with data, that the interseismic
strain rate is lower along the fault segment more prone to seismic
activation.
GEOLOGICAL MODEL
Earthquakes are usually interpreted as the rupture of an
asperity along a fault, and the shear stress overcomes the fault
strength. Why is there a seismic cycle? Why seismicity is not
more randomly distributed if an earthquake is simply associated
to an asperity, which could be smeared out after fault motion?
The origin of the earthquake recurrence or seismic cycle, i.e., the
long interseismic period followed by the coseismic (and
postseismic) period, remains quite obscure. The length of the
interseismic period between two earthquakes along the same fault
is attributed to a number of classic physical parameters, e.g., the
relative velocity between the two walls of the fault, the
composition of the crust, the mineralogy and foliation of the fault
rocks, the morphology and length of the fault plane, the thermal
state, the friction on the fault, the fluid pore-pressure, etc. (e.g.,
SCHOLTZ, 1990; COLLETTINI et alii, 2009). All these parameters
allow first a long, static accumulation of energy during the
interseismic period, which is eventually radiated during the
coseismic time, when the friction on the fault is overtaken. In this
article we contribute to this topic with a geological model to
justify the cyclic occurrence of earthquakes along a crustal fault,
where the aforementioned physical parameters still determine the
timescale of the recurrence. Here we investigate the role of the
brittle-ductile transition (BDT) in controlling the seismic cycle.
We propose a model that links the continuous ductile deformation
at depth with the brittle episodic behaviour of shallow crustal
layers and show how the BDT may play a relevant role in
controlling the seismicity and its evolution in time. The model is
tested numerically and applied to two areas where normal fault
and thrust related earthquakes occurred, i.e., in the central
Apennines (2009) and Taiwan (1999). GPS interseismic and
coseismic data, dissipated energy and fluid flux discharge from
the two cases are shown to be consistent with model predictions,

Fig. 1 – Assuming a steady stated strain rate in the ductile lower crust, stick-slip motion in the brittle upper crust, extensional and compressional faults
generate opposite kinematics and mechanic evolution. In the extensional tectonic environment, the triangle of crust above the BDT remains “suspended”
while a dilated area forms during the interseismic period. Once shear stress along the locked part of the fault becomes larger than fault strength, the
hangingwall will collapse. Conversely, along a thrust plane, an area over-compressed separates the ductile shear from the overlying locked fault during the
interseismic period. The hangingwall is expelled as a compressed spring during the coseismic period. Fluids discharge behaves differently as a function of
the tectonic field (after DOGLIONI et alii, submitted).
where normal faults and thrusts have opposite behaviour.
Similarly to the effects of the lithostatic load, which enhances the
rupture of normal faults and inhibits faulting along thrusts
(CARMINATI et alii, 2004), the two types of faulting are
asymmetric in terms of geological and mechanical behaviour.
A simplified rheology of the crust predicts an upper brittle
layer and a ductile lower crust (e.g., RUTTER, 1983). The
transition between the brittle upper crust and the ductile lower
crust should determine a different tectonic behaviour between the
two domains. The steady state deformation in the ductile lower
crust is in fact at odds with the stick-slip behaviour of the
shallower brittle levels. The constant strain rates measured by
GPS during interseismic periods suggest that the locked status of
faults in the brittle layer does not inhibit continuous ductile shear
below the BDT.
REFERENCES
CARMINATI E., DOGLIONI C. & BARBA S. (2004) - Reverse
migration of seismicity on thrusts and normal faults. Earth
Sci. Rev., 65, 195–222.
15
COLLETTINI C., NIEMEIJER A., VITI C. & MARONE C. (2009) -
Fault zone fabric and fault weakness. Nature, 462 (7275),
907-910, DOI: 10.1038/nature08585.
DOGLIONI C., BARBA S., CARMINATI E. & RIGUZZI F. (2010) –
Role of the brittle/ductile transition on the seismic cycle.
Submitted.
RUTTER E.H. (1986) - On the nomenclature of mode of failure
transitions in rocks. Tectonophysics, 122, 381-387.
SCHOLTZ C.H. (1990) - The Mechanics of Earthquakes and
Faulting. Cambridge; New York: Cambridge University
Press, Ref. QE534.2.S37.
SESSIONE 1

SESSIONE 1
Holocene activity of the Subequana Valley-Middle Aterno Valley
normal fault system, south of the 2009 L’Aquila earthquake
epicentre: implications for seismic hazard in central Apennines
EMANUELA FALCUCCI (*), STEFANO GORI (*), MARCO MORO (**), MICHELE SAROLI (°),
GIANDOMENICO FUBELLI (°°), FABRIZIO GALADINI (*) & PAOLA FREDI (+)
Key words: Active normal faulting, central Apennines , Coulomb
stress diffusion, 2009 L’Aquila earthquake.
INTRODUCTION
The Subequana valley is one of the easternmost depression of
the central Apennines. It is located south of the L’Aquila and
Fossa-San Demetrio basins. The formation and evolution of the
Subequana valley has been conditioned by the activity of a 8-10km
long, NW-SE trending and SW dipping normal fault system
that affects the SW slopes of Mt. Urano which bounds the
depression to NE. The fault system, characterised by a complex
structural evolution, has been responsible for the displacement of
continental deposits spanning the whole Quaternary (MICCADEI et
alii, 1997).
GEOLOGICAL AND PALEOSEISMOLOGICAL
ANALYSES
Geological and geomorphological have been performed in the
Subequana valley area, in particular along the south-western
slope of Mt. Urano, aiming at finding useful elements to
characterise the Late Pleistocene-Holocene kinematic behaviour
of the normal fault system. For this purpose, we dug two
paleoseismological trenches across one of the fault segments
displacing the valley bottom. The trenches revealed two
Holocene faulting events, determining minimum surface
displacement of about 80 cm, with the last event occurred after
2615±19BP (Fig.1a).
Furthermore, geological observations performed at the
_________________________
(*) INGV, Sezione Milano-Pavia, gori@mi.ingv.it
(**) INGV, Sezione CNT, marco.moro@ingv.it
(°) Università degli Studi di Cassino, michele.saroli@unicas.it
(°°) Università degli Studi Roma Tre, fubelli@uniroma3.it
(+) Università di Roma “La Sapienza”, paola.fredi@uniroma1.it
16
northern tip of the Subequana Valley fault defined the presence of
normal-to-transtensive transverse structural features. This faults,
responsible for the displacement of Late Pleistocene-Holocene
fluvial sediments, probably represent connecting faults between
the Subequana Valley fault and the Middle Aterno Valley fault
systems and the Middle Aterno Valley fault system, i.e. an
extensional tectonic structure displaying a dextral en echelon
arrangement with the Subequana Valley, and defined as active by
GALADINI & GALLI (2000). Paleoseismological investigation
(Fig.1b), still in progress, seem to confirm the activity of the
Middle Aterno Valley fault system.
Fig. 1 – Walls of the trenches dug across the Subequana
Valley fault (a) and the Middle Aterno Valley fault (b).

Fig. 2 – Structural setting of the Middle Valle dell’Aterno and Subequana Valley.
CONCLUSIONS
Hence, it is possible to hypothesise that the Subequana Valley
fault and the Middle Aterno Valley fault represent the expression
at the surface of the same seismogenic fault (Fig.2) and that can
activate together during M 6.7-6.8 seismic events.
REFERENCES
GALADINI F. & GALLI P. (2000) - Active tectonics in the central
Apennines (Italy): Input data for seismic hazard assessment.
Natural Hazards, 22, 225-270.
MICCADEI E., BARBERI R. & DE CATERINI G. (1997) - Nuovi dati
geologici sui depositi quaternari della conca Subequana
(Appennino abruzzese). Il Quaternario, 10 (2), 485-488.
17
SESSIONE 1

SESSIONE 1
The 2009 Abruzzo earthquake: the role of Geomorphology and
Quaternary geology for the prevention of seismic risk
PIERO FARABOLLINI (*), ENRICO MICCADEI (**),
GIAN PAOLO CAVINATO (°), PIERO DE PARI (°°) & TOMMASO PIACENTINI (**)
Key words: Geomorphology, L’Aquila earthquake, Quaternary
geology, seismic risk prevention.
On April 6th 2009 at 3:32 a.m., after some three months of
low magnitude tremor, a strong earthquake (MI Richter 5,8) hit
the L’Aquila area. The event was characterized by an extensional
movement along NW-SE fault planes with SW-NE extension
(data available on line at www.ingv.it).
Several post earthquake campaigns of geological and
geomorphological surveys have been carried out in the L’Aquila
area, however, so far, there is not a single geological model
shared by the different scientific communities.
The present work wants emphasize the role of detail
geomorphologic survey (1:10.000 or even 1:5.000 scale) and
Quaternary continental deposits analysis in the L’Aquila basin, as
base for a correct seismic risk prevention, where historical
seismicity and technical rules does not succeed in reducing
seismic risk.
The geomorphological effects (so called surface coseismic
effects) occurred in the epicenter area (particularly Paganica,
Tempera and Onna, that suffered heavy buildings damages), are
mostly rock falls, debris landslides, small landslide reactivations,
very shallow fissures and fractures with variable strike on
different continental deposits, fissures on road pavement, fluvial
embankment local falls, soil liquefaction, and even small snow
avalanches. All these features occurred in almost ground water
saturation of the Quaternary continental surface deposits of the
L’Aquila basin.
Geomorphological effects have been observed up to 50 km far
from the epicenter area. The distribution shows a moderate
directional trend that is NW-SE elongated markedly parallel to
the main faults and particularly to the L’Aquila basin and to the
complex geometry of the basin fill. It is characterized by high and
variable thickness of Quaternary continental deposits (mostly
lacustrine deposits and alluvial fan deposits), that is also
_________________________
(*) Scuola di Scienze Ambientali, Università degli Studi di Camerino,
piero.farabollini@unicam.it
(**) DIGAT Università degli Studi "G. D'Annunzio" Chieti-Pescara
(°) CNR-IGAG Istituto di Geologia Ambientale e Geoingegneria
(°°) Geoservizi Srl
18
confirmed by deep borehole and geophysical investigations.
The distribution of the effects vs. the distance from the
epicenter area shows a peculiar arrangement with few effects in
the 0-5 km interval and a maximum in the 10-15 km interval (Fig.
3a). It suggests a strong control of local topographic and
geomorphologic setting on the effect distribution. The occurrence
of no effects between 30 and 40 km, and several effects (mainly
rock fall) in the 40-50 km interval, provide a further
confirmation. These remote effects are due to a strong local
topographic relief in the Aterno river gorges located close to the
outlet of the river into the Sulmona basin.
Some examples of the geomorphologic effects are rock-falls
and toppling landslides, that occurred along structural controlled
scarps or along calcareous slopes of wide karst landforms. Other
examples evidence the relationship between structural landforms
and landslides and subsidence, or collapse scarps on karst
landforms. The latter are scarps tangential to sink-hole and open
fissures, in many cases, with an annular arrangement, that
suggests a relationship with buried karst landform. Many
phenomena of debris flows also occurred, the evolution of which
led to the denudation of large areas of slope.
As reguards the rock falls, on the base of geomorphological
and morphostructural analysis, the surveyed cases are referable to
three main morphostructural settings: rock falls on calcareous
faulted homocline ridges; rock falls on calcareous rock slopes of
karst landforms; rock falls on scarps developed on conglomerates
and breccias of the Quaternary continental deposits.
These elements provide useful indications both at local scale,
within the studies of seismic microzonation and seismic risk
prevention, and at regional scale, for integration and detailing
studies and inventory of landslides.

Key words: Active tectonics, earthquakes, paleoseismology,
seismic hazard.
INTRODUCTION
The distribution and level of seismicity in Italy have been
narrated since about the fifth century BC by the incomparably
rich and continuous flow of written sources that have
characterized our history through the centuries. These sources
have made the Italian seismic catalogues the most complete and
back-in-time extended in the World. Also for this reason, national
seismic hazard studies have always been mainly based upon this
unique, huge mass of valuable data. Nevertheless, whereas before
we just supposed it, today we know that also the Italian
catalogues reasonably “lack” many M=6.5 earthquakes, the
seismogenetic structures responsible for which are possibly
characterized by recurrence times that are longer than those
accounted by the historical sources. Therefore, also in Italy
earthquake data collected from “alternative” sources - such as
those derived from geological studies - should finally become a
necessary ingredient in seismic risk assessment.
THE PALEOSEISMOLOGICAL STUDIES IN ITALY
Certainly, with respect to the classical historical seismology,
the most reliable alternative approach in ancient earthquakes
hunting is paleoseismology. After a long gestation started with
the introduction of the modern concepts on active tectonics (e.g.,
GILBERT, 1884), the term paleoseismology finally appeared in
Russia in the 1960’s, whereas the first modern studies were
developed in United States, New Zealand and in Japan since the
1970’s (insights in MCCALPIN, 1986).
In Italy, the first paleoseismological case history was
published by GIRAUDI in 1989, that is well after the scientific
community realized that also in the bel paese surface faulting was
_________________________
(*) Dipartimento della Protezione Civile, paolo.galli@protezionecivile.it
(**) CNR-IGAG
Paleoseismology in Italy: latest from L’Aquila
PAOLO GALLI (*)(**)
19
really possible (i.e., 1980 Irpinia earthquake, Mw=6.9).
Fig. 1 – View looking north of the 1980 surface faulting in the Pantano di San
Gregorio (Mw 6.9, Irpinia earthquake). Vintage photo by Prof. F. Carraro.
Indeed, since the Giraudi’s pioneering excavations in the
Aremogna plain (Abruzzo), over the past 20 years some hundred
paleoseismological trenches have been dug in Italy from the Alps
to Sicily. The results of these works have supplied reliable and
conclusive data on the recent activities of many famous, unknown
and/or debated faults, mainly located along the central and
southern Apennines. Through to many robust datings of surface
fault events, they also have provided the ages of several
unexpected or poorly known M=6.5 earthquakes, giving – in any
case – the final proof concerning the Late Pleistocene-Holocene
activity of each single fault.
GALLI et alii (2008) reviewed most of these results, presenting
also a first catalogue of 56 paleoearthquakes of Italy that
occurred mainly in the past 6 kyr. In the intentions of these
authors, the catalogue integrates the historical/ instrumental
seismic compilation, and extends it beyond the recurrence time of
the seismogenetic faults (2,000 ±1,500 yr). Since that review,
other paleoseismological investigations have been carried out
and/or published. For instance, some trenches were dug across a
neglected primary fault running at the border amongst Latium,
Abruzzi, Molise and Campania. Here, the Aquae Iuliae fault has
SESSIONE 1

SESSIONE 1
Fig. 2 – Trench across the Mt. Pettino fault (L’Aquila). Note the rock-fault
scarp and the whitish cataclastic zone on the background. The blackish
stratum in the trench wall is a paleosol dated around 22ka. All the deposits in
the hangingwall are faulted and dragged against the rocky footwall.
been found “guilty” for both the southern catastrophic 1349
mainshock (Mw=6.7), and several others previous earthquakes
(GALLI &NASO, 2009). On the other hand, in the Subequana
valley, the homonymous fault has been trenched by FALCUCCI et
alii. (2009), who have found faulting trace during the Roman
time.
Recently, others studies have been performed in the area of
the 2009 L’Aquila earthquake, both on its causative fault
(Paganica-San Demetrio system) and on different conterminous
faults (Mt. Marine, Mt. Pettino and Roccapreturo faults; CINTI et
alii, 2009; GALLI et alii, 2009).
Indeed, although in this sector of the chain the knowledge on
active tectonics was though to be one of the best in Italy, it
appears that amongst the hundred trenches dug along the
Apennines, only one was previously located in the near field of
the 2009 epicentre (Mt. Marine fault; see in GALLI et alii, 2008).
Therefore, the preliminary results revealed a surprising
behaviour of these faults. For instance, they show that the slip of
the Paganica-San Demetrio fault may cause both 2009-like
earthquakes (i.e., Mw ~6.3; see also the 1461 event), and also
stronger ones, as in February 1703, when it ruptured together
with the Mt. Marine and Mt. Pettino faults, generating a Mw ~6.7
event.
Notwithstanding this encouraging outline, it must be stressed
that paleoseismology alone can not be considered a panacea in
earthquake geology, especially when applied without the control
of a comprehensive and robust geomorphological, stratigraphical,
chronological and structural framework of the local and regional
context. Moreover, the isolated trenching of geomorphic features
(i.e., scarps, lineaments) or the analysis of occasional, limited
outcrops may lead to hazardous mistakes; concerning both the
interpretation of the investigated deformation (e.g., gravitational
vs tectonic) and its stratigraphical and chronological constraint
20
(e.g., rejuvenating of deposits age).
In particular, great attention should be paid in assessing the
age of units in trench wall only on the basis of “blind”
radiometric dating. The measured age of samples (and especially
of bulk samples, and paleosols), which is usually analytically
correct, must absolutely be consistent with the morphostratigraphical
context of the area. Indeed, it is very common to
obtain young “contaminated” 14C ages of old deposits or
paleosols (e.g, near the ground surface), and thus to extrapolate
non-existent paleoearthquakes (and/or fault slip-rates). In this
perspective, paleoseismology should be seen as the crowning
achievement of a long-term to short-term integrated approach,
and not the starting (and often definitive) point in active tectonics
studies.
REFERENCES
CINTI F.R., CIVICO R., CUCCI L., DE MARTINI, P.M.,PANTOSTI,
D., PIERDOMINICI, S., PUCCI, S.,BRUNORI, C.A. (2009) -.
Looking for surface faulting ancestors of the L’Aquila April
6, 2009 event: preliminary paleoseismological data and
seismic hazard implications. GNGTS, 28° Convegno
Nazionale, 27-29.
FALCUCCI E., GORI S., MORO M., GALADINI F., MARZORATI S.,
LADINA C., PICCAREDA D. & FREDI P. (2009) - Evidenze di
fogliazione normale tardo-olocenica nel settore compreso fra
la conca Subequana e la Media Valle dell’Aterno. GNGTS,
28° Convegno Nazionale, 161-163.
GALLI P., GALADINI F. & PANTOSTI D. (2008) - Twenty years of
paleoseismology in Italy. Earth Sci. Rev., 88, 89-117,
doi:10.1016/j.earscirev.2008.01.001.
GALLI P. & NASO G. (2009) -. Unmasking the 1349 earthquake
source (southern Italy). Paleoseismological and
archaeoseismological indications from the Aquae Iuliae
fault. J. Structural Geology, 31, 128-149.
GALLI P., GIACCIO B., MESSINA P. & PERONACE E. (2009) -.
Paleoseismological news from L'Aquila faults. GNGTS, 28°
Convegno Nazionale, 34-37.
GILBERT G. K. (1884) - A theory of the earthquakes of the Great
Basin, with a practical application. Am. Jour. Sci., 3 rd ser.,
49-53.
GIRAUDI C. (1989) - Datazione di un evento sismico preistorico
con metodi geologici e radiometrici: piani di Aremogna e
Cinquemiglia. In E. Guidoboni (Ed.), I terremoti prima
dell'anno Mille, ING-SGA, Bologna, 53-64.
MCCALPIN, J.P. (1996) - Paleoseismology. Academic Press, San
Diego, 588 pp.

Key words: Active tectonics, Alto Ofanto, earthquakes, Irpinia,
paleoseismology, seismic hazard.
INTRODUCTION
Thirty years ago - on November 23, 1980 - the strongest
earthquake (Mw 6.9) occurred in the 20th century in the southern
Apennine rocked the villages of the Upper Ofanto Valley
(Irpinia), causing almost 3000 fatalities.
Indeed, this small region is one of the most seismically active
of Europe; for instance, Conza della Campania – one of its more
ancient settlement - has been struck at least seven times (Is>VIII
MCS; GALLI, 2010) during the past millennium, each time rising
again over its ruins. But after the 1980 earthquake, it has been
deserted, and rebuilt by its inhabitants 1 km away from its former,
pre-Roman settlement.
Many of these earthquakes are almost unknown, and some do
not still appear in the current seismic catalogue (CPTI, 2004);
others are well characterised in terms of intensity distribution, but
still lack any certain seismogenetic attribution. Only the 1980 one
has conclusive data concerning its causative seismogenic
structure, not only due to the large amount of instrumental data,
but also because of the unequivocal surface faulting phenomena
that drew the attention of some geologists on a previously
unconsidered fault system (i.e., Mt. Marzano fault, and
contiguous segments: MMFS. WESTAWAY &JACKSON, 1984).
On the basis of 1) field study on faults and fault scarps and 2)
archive research of minor earthquakes, we are currently trying to
cast light on these aspects, which are both the basic ingredients
for understanding the seismic hazard of the region.
KNOWN AND UNKNOWN EARTHQUAKES AND
FAULTS OF THE UPPER OFANTO VALLEY
_________________________
Earthquakes and fault(s) in the Upper Ofanto Valley
(Irpinia,southern Italy)
PAOLO GALLI (*) (**), TAMARA CARDUCCI (°), GIUSEPPE ESPOSITO (*), GIUSEPPE NASO (*),
EDOARDO PERONACE (**) & BRUNO QUADRIO (°°)
(*) Dipartimento della Protezione Civile, paolo.galli@protezionecivile.it
(**) CNR – IGAG, Istituto di Geologia Ambientale e Geoingegneria, Roma
(°) Dipartimento di Scienze della Terra, Università di Camerino
(°°) Dipartimento di Scienze della Terra, Università degli Studi di Pavia
21
CPTI (2004) reports two catastrophic earthquakes in the
Upper Ofanto Valley (in 1694 and 1980, both with Mw~6.9),
besides a couple of moderate events in 1853 and 1910 (Mw~5.9).
Actually, our archive researches reveal the existence of other
strong poorly known or unknown earthquakes in the same area
(Fig. 1). These are the 1466 (Mw~6.4, see in GALLI et alii, 2006),
1517, 1561, 1680 and 1692 events (Mw~5.8; CASTELLI et alii,
2008; CARDUCCI et alii, 2009) and others of lower energy.
Fig. 1 – Macroseismic epicentres of Mw>5.5 earthquakes in the Upper Ofanto
Valley (black years from CPTI, 2004; blue, other sources in this paper). The blue
lines are the surface evidences of the Mt. Marzano fault system, which was
responsible for the 1980 event (see instrumental epicentre by WESTAWAY,
1992), and, perhaps, for many others earthquakes. The dashed line envelops the
1980 aftershocks distribution, that is, reasonably, the in-depth area of the fault.
The macroseismic epicentres of all of these earthquakes fall
within the area subtended by the MMFS (see Fig. 1). Moreover,
some of the highest intensity datapoints distributions (e.g., of the
1466 and 1980 earthquakes) are very similar, both in terms of
geometry and intensity values. Others events appear to fill the gap
of the 1980 surface rupture (1853), whereas others are located at
SESSIONE 1

SESSIONE 1
the tips of the fault system. Finally, for one of the strongest
earthquake (1694, Mw 6.9), we identified the description of a
long surface faulting phenomenon in one of the historical
accounts which could match with part of the MMFS.
Therefore, considering the proximity and similarity of most of
these earthquakes, we guess that some of them could have been
generated by a single seismogenetic structure. Indeed, we do not
exclude a priori alternative sources, since we are aware to know
not enough on possible antithetic structures. These would
necessary affect the silicoclastic units of the Ofanto-Ufita valleys,
being thus not easily detectable at surface (GALLI et alii, 2006).
However, in order to overcome this impasse, we focused
firstly on the MMFS, trying to collect all the possible information
concerning the surface faulting happened in November 1980.
To do this we both interviewed dozen of peasants, shepherds
and inhabitants of the area which was crossed by the different
fault segments, and most of all those geologists who were
involved in field survey after the 1980 earthquakes. We finally
gathered many reliable, first-hand information, photographs, and
unpublished reports.
Fig. 2 – Deep gorge carved in the limestone footwall of the Mt. Marzano fault
system. The bottom is offset by one of the N340 transfer fault between the main
segments. Note the prominent rock-fault scarp.
We also had the opportunity to study the high-resolution
panchromatic airphotos taken in the days after the earthquake,
where some the surface faulting stretches are visible (in the areas
not affected by snowfall).
Then we surveyed the entire ~40-km-long fault system,
making observations, measures (structural, microtopography),
and quick paleoseismic pit analyses - with 14C dating of samples
– on the fault/fault scarp.
On the basis of all the above we obtained some preliminary
results, such as: 1) identification and 1:5000 mapping of the
several surficial segments of the MMFS (e.g. in Fig. 2); 2)
quantitative reassessment of the 1980 and previous surface
ruptures on each segment; 3) hypotheses on which (group of)
segments reasonably generated the historically documented
earthquakes.
22
ACKNOWLEDGEMENTS
We are indebted with many colleagues who share with us
their 1980 memories and photos, and in particular with F.
Carraro, S. Lambiase and R. Westaway. We wish to thank also R.
Berardi, C. Bosi, L. Carmignani, A. Cinque, P. Scandone, P.
Marsan, F. Ortolani and I. Sgrosso. We thank also D. Pantosti,
who generously provided her field maps and photos, discussing
with us some unpublished data of Piano di Pecore trench. Thanks
also to G. Di Trolio for the information on the 1980 damage
along the Acquedotto Pugliese tunnel.
REFERENCES
CARDUCCI T., GALLI P. & PERONACE E. (2009) - Terremoti
minori dell’Irpinia ed il loro ruolo nell’identificazione delle
strutture sismogenetiche maggiori. Riassunti del 28°
Convegno Nazionale GNGTS, Trieste, 16-19 Novembre
2009, 93-95.
CASTELLI V., GALLI P., CAMASSI R. & CARACCIOLO C. (2008) -
The 1561 earthquake(s) in southern Italy: new insights into a
complex seismic sequence. J. Earthquake Engineering, 12,
1054-1077.
GALLI P. (2010) – La storia sismica di Conza, in: E. Ricciardi
(ed.), Conza. Storia, arte, fede, Conza della Campania.
GALLI P., BOSI V., PISCITELLI S., GIOCOLI A. & SCIONTI V. (2006)
- Late Holocene earthquakes in southern Apennines:
paleoseismology of the Caggiano fault. Int. J. of Earth
Sciences, 95, 855-870.
WESTAWAY R. (1992) - Seismic moment summation for historical
earthquakes in Italy: tectonic implications. J. Geophys. Res.,
97, 15437-15464.
WESTAWAY R. & JACKSON J. (1984) - Surface faulting in the
Southern Italian Campania-Basilicata earthquake of 23
November 1980. Nature, 312, 436-438.

Active normal faulting and large scale gravitational deformation:
the case of the Mt. Morrone SW slopes (central Apennines, Italy)
Key words: Central Apennines, Sulmona basin, large scale
gravitational deformation, active normal faulting.
INTRODUCTION
The present work aims to add new data to improve the
comprehension of the relationship between tectonics and largescale
gravitational deformations. According to the present
literature, tectonics may play an active or passive role in the
gravitational evolution of mountain slopes. The passive role is
related to the structural setting inherited by previous, no more
active, tectonic phases. Rock movements may occur along faults
planes, being just triggered by erosional processes and/or seismic
shaking. The role of active tectonics, instead, is represented by
the morphological modifications that surface faulting produce on
slopes, determining an increase of relief energy and (of) rocks
stress. The present paper deals with the case of the Morrone
ridge, a Neogene thrust front located in the outer sector of the
central Apennine foreland fold and thrust belt (Abruzzi
Apennines), in order to define the relationship between an active
fault system potentially responsible for high-magnitude seismic
events and the occurrence of large-scale gravitational movements.
The Mt. Morrone relief delimits the eastern border of the
Sulmona basin, a tectonic depression the formation of which is
due to the activity of two parallel normal fault segments affecting
the ~23 km long Mt. Morrone western slopes (GORI et alii,
2009). The Late Pleistocene-Holocene activity of these normal
fault branches has been already documented in the past. Along
the same slope, landforms and structures, such as trenches and
small depressions, representing the surficial expression of Deep
Seated Gravitational Movement (DSGM), have been detected at
different elevations (CICCACCI et alii, 1999). The highest trench
is very long and almost continuous, bounding the higher part of
the slope for over 20 km from the Pescara river valley to the
_________________________
STEFANO GORI (*), FABRIZIO GALADINI (*), PAOLO GALLI (**), BIAGIO GIACCIO (°), PAOLO MESSINA (°),
ANDREA
SPOSATO (°), EMANUELA FALCUCCI (*) & FRANCESCO DRAMIS (°°)
(*) INGV, Sezione Milano-Pavia, gori@mi.ingv.it
(**) Protezione Civile Nazionale, paolo.galli@protezionecivile.it
(°) CNR-IGAG, paolo.messina@igag.cnr.it
(°°) Università Roma Tre, dramis@uniroma3.it
23
Pacentro village. A series of relatively shorter trenches, in the
order of 1-2 km long, affects the middle-lower part of the slope.
GEOMORPOLOGICAL AND PALEOSEISMOLOGICAL
INVESTIGATION
Geological, structural and geomorphological surveys have
been carried out along this mountain slope in order to achieve
information about the kinematic history and behaviour of these
DSGM and to define their relationship with the fault system
activity. Moreover, paleoseismological trenches have been dug
across two of the gravitational trenches, in order to detect
possible evidences and chronological constraints for the DSGM
formation and evolution.
All the data indicate that the DSGM affecting the SW slope of
the Mt. Morrone took place after the Early-Middle Pleistocene,
since slope-derived breccias, related to this chronological
interval, have been displaced by the opening of a gravitational
trench. Small displacements of colluvial units which fill the
trenches (dated at 10660-10540 cal. b.C./ 10430-9910 cal. b.C.
and 21440±120 BP) represent the effects of the gravitational
deformation activity. This probably represents the secondary
effect of the fault system activation, and indicates that the Mt.
Morrone normal fault system played an active role in the
evolution of the large-scale gravitational deformation.
REFERENCES
CICCACCI S, D’ALESSANDRO L, DRAMIS F, MICCADEI E (1999) -
Geomorphologic evolution and neotectonics of the Sulmona
intramontane basin (Abruzzi Apennines, central Italy). Z
Geomorph N F, 118 (Suppl. Bd), 27-40.
GORI S., GIACCIO B., GALADINI F., FALCUCCI E., MESSINA P.,
SPOSATO A., DRAMIS F. (2009) - Active normal faulting along
the Mt. Morrone south-western slopes (central Apennines,
Italy). Int. J. Earth Sci. DOI: 10.1007/s00531-009-0505-6.
SESSIONE 1

SESSIONE 1
Key words: Active fault, Geomorphology, neotectonic,
quaternary stratigraphy.
The recent L’Aquila earthquake (Mw 6.3) reawakened the
discussions concerning the relationships amongst the superficial
geological setting, seismogenetic structure and coseismic surficial
effects. This happened also during previous moderate
earthquakes, such as the Umbria-Marche event in 1997 (Mw 6),
when the surficial breaks were interpreted by some authors as due
to surface faulting, whereas others claimed mainly for gravitydriven
phenomena. As far as the 2009 L’Aquila earthquake, and
as for stronger events (i.e., 1980 earthquake; Mw 6.9), the whole
scientific community agreed on the tectonic genesis of the
surficial breaks recognized all along the Paganica-San Demetrio
fault system (PSDFS; e.g. in FALCUCCi et alii, 2009).
Nevertheless, in this case the problems were related to the fact
that this fault system was previously poorly known and not
reported by the database of seismogenetic structures. Indeed, in
the past, several others fault systems contiguous to the PSDFS
have been investigated in the L’Aquila region (see in GALLI et
alii, 2008 and reference therein). Many earthquake geologists
pointed their attention toward these faults after the 2009 event,
but none of these showed indication of surficial ruptures. Due to
the small distance amongst regional fault systems, the main
problem the scientific community had to face with was to unravel
the relationships between faults (i.e., segmentation), that is if they
might rupture sometime alone (generating moderate earthquake)
and sometime together with the conterminous segments
(generating high energy events).
In order to understand these fundamental issues, it is strictly
necessary to study the behavior and the time-space evolution of
the active fault system. This yields to know both the past surface
faulting events and the long term displacement history of the
structure. The first target may be achieved through
paleoseismological analyses, which usually provide information
concerning the past 40 ka. The second one needs integrated
studies of stratigraphy, geomorphology, structural geology,
pedology, etc. (Quaternary Geology s.l.), which allow also to
_________________________
(*) CNR – Istituto di Geologia Ambientale e Geoingegneria,
paolo.messina@cnr.it
Quaternary geology and seismic hazard
PAOLO MESSINA (*)
24
improve the main fault parameters.
These two approaches are often separately applied, and the
ensuing results are sometimes even rather conflicting. The
reasons for these potential disagreements relate to the different
aims that move these studies, and to the different methodologies
and forma mentis of geologists operating in the field of
paleoseismology and Quaternary geology. Nevertheless, it should
be noted that only the integration of both long-term and shortterm
study approaches brings advantages, towards a better
perceptive of the behaviour of active tectonic structures over
time.
This kind of interdisciplinary approach, which cannot be
limited to quick (e.g., geomorphologic surveys) or local (isolated
paleoseismological trenches) analyses, provides all the necessary
information for the mapping of “certain” active faults, i.e. one of
the main step toward the characterization of local and regional
seismic hazard.
In the past years, just applying this methodology, some of the
researches aimed at the neotectonics characterization of
seismically active regions have defined the succession of
depositional and erosional events, allowing defining the
chronology of the different phases. Examples come from the
Latium-Abruzzi Apennine area, where the continental succession
of several intermountain basins have been recognized, offering
also a tentative correlation amongst them (BOSI et alii, 2003).
The possibility to draw a stratigraphical and morphological
framework with accurate chronological constraints has allowed
either to define the tectonic evolution of each basin, or to propose
regional models of the tectonic evolution. Moreover, it permitted
to define the geometric and kinematics characters of several
faults, giving the boundaries of their activity during time (e.g.
figure 1).
Unfortunately, these data were not yet available for the
PSDFS, which prior to the 2009 earthquake was poorly known,
its several segments being variously linked to other fault system
by different authors (see MESSINA et alii, 2009). The weeks after
the 2009 earthquake, Quaternary investigations coupled with
paleoseismological trenching finally revealed the detailed
geometry of the causative fault and the tectonic evolution of the
area, besides the chronology of the last seismic events. This
study allows to ascertain that the PSDFS may rupture also
together with the Upper Aterno Fault System (GALADINI &
GALLI, 2000), as in 1703 when it caused a Mw 6.7 earthquake.

Fig. 1 – Tectonic evolution of the NE part of Fucino basin (AQ). 1) Dip of
tilted layers; 2) top surfaces of non-tilted terraces; 3) traces of the paleo-
Giovenco river; 4) normal fault (indentation towards the hangingwall); A)
limestone (Miocene); B) Flysch (Miocene); C) Aielli and Cupoli Complexes
(Pliocene- Lower Pleistocene); D) Pescina formation (Middle Pleistocene); E)
Casoli formation (Middle Pleistocene); G) Pervole formation (Middle
Pleistocene); H) deposits of the Upper Pleistocene-Holocene; S1…S6)
erosional and depositional surfaces; F1, F2) faults of Early-Middle Pleistocene
activity; F3) active fault. From MESSINA (1996) modified.
REFERENCES
BOSI C., GALADINI F., GIACCIO B., MESSINA P. & SPOSATO A.
(2003) - Plio-Quaternary continental deposits in the Latium-
Abruzzi Apennines: the correlation of geological events
across different intermontane basins. Il Quaternario, 16
(1Bis), 55-76.
FALCUCCI E., GORI S., PERONACE E., FUBELLI G., MORO M.,
SAROLI M., GIACCIO B., MESSINA P., NASO G., SCARDIA G.,
SPOSATO A., VOLTAGGIO M., GALLI P. & GALADINI F. (2009)
- The Paganica fault and surface coseismic ruptures caused
by the 6 April 2009 earthquake (L’Aquila, Central Italy).
Seismol. Res. Lett., 80, 940-950.
25
GALADINI F. & GALLI P. (2000) - Active tectonics in the central
Apennines (Italy) - input data for seismic hazard assessment.
Nat. Haz., 22, 225–270.
GALLI P., GALADINI F. & PANTOSTI D. (2008) - Twenty years of
paleoseismology in Italy. Earth Sci. Rev., 88, 89–117.
MESSINA P. (1996) - Tettonica mesopleistocenica dei terrazzi
nord-orientali del Fucino (Italia centrale). Il Quaternario, 9,
293–298.
MESSINA P., GALLI P., FALCUCCI E., GALADINI F., GIACCIO B.,
GORI S., PERONACE E. & SPOSATO A. (2009) - Evoluzione
geologica e tettonica quaternaria dell'area interessata dal
terremoto aquilano del 2009. Geoitalia, 28, 24-29.
SESSIONE 1

SESSIONE 1
The crustal deformation associated to the seismic cycle measured by
DInSAR techniques: a starting point for the geological analysis
Key words: crustal deformation, L'Aquila seismic sequence,
SAR interferometry, seismic cycle.
Various analysis techniques based on interferometric satellite
SAR data allow nowadays to measure sudden or slow ground
movements with accuracies up to 0.5 cm in displacement, 1
mm/yr in velocity, and with spatial resolutions up to 2.5 m. In the
area of the 2009 Abruzzi earthquake the ground deformation was
analysed for a seismic cycle interval of 18 yr, including the strain
accumulation phase, the co-seismic and the initial post-seismic
deformations.
The regional inter-seismic deformation field shows the
evidence of the tectonic processes acting in this sector of the
Apennines, but does not seem to yield elements for a detailed
seismic hazard analysis at the scale of the single seismogenic
sources. New analytical and numerical models shall be developed
to fully exploit the information content carried by these data.
The co-seismic deformation associated to the main
earthquakes of the Abruzzi sequence has been measured with
unprecedented detail thanks to the new high resolution data from
the Italian COSMO-SkyMed satellites (Figure 1). The visual
inspection and the modeling of these data allowed to extract
important information on the seismic source, on its surface
expression, and on the indirect effects of the seismic shaking on
the environment. The co-seismic deformation modeling was
based on well-established analytical simulations of elastic
dislocations, and on a new approach using numerical analysis.
The latter allows to include as constraints the topography and the
crustal heterogeneities, where known. The geophysical modeling
generates important parameters which can be used to test and
validate the geological analysis of the source.
The post-seismic deformation measured on the 2009 Abruzzi
faults has been modeled in terms of fault after-slip. Although
small, it should be taken into account when calculating the total,
per-event ground deformation, and when analysing the
cumulated geological ground deformation.
_________________________
(*) Istituto Nazionale di Geofisica e Vulcanologia - Roma,
stefano.salvi@ingv.it
Lavoro eseguito nell’ambito del progetto ASI-SIGRIS, con il contributo
finanziario dell’Agenzia Spaziale Italiana.
STEFANO SALVI (*)
26
Our research shows that the detailed analysis and the
geophysical modeling of high resolution measurements of the
present ground deformation can generate important information
to be carefully considered during the interpretation of the
geological and geomorphological evolution of high seismic
hazard regions.
Fig. Fig. 1 – Differential 1 – Differential COSMO-SkyMed interferogram showing showing the co-seismic the co-seismic
displacement field field generated generated by the by mainshock the mainshock source source dislocation. The The black black
lines lines show show the field the field evidences evidences of surface of surface breakage. breakage. The The pentagon pentagon symbol symbol is is
the mainshock the mainshock epicenter.
epicenter.

Principal slip zones in limestone: microstructural characterization
and implications for the seismic cycle
STEVEN A.F. SMITH (*), GIULIO DI TORO (* , °), ANDREA BILLI (**) & RICHARD SPIESS (°)
Key words: Earthquakes, limestone, slip zones, friction
experiments, microstructure.
INTRODUCTION
Earthquakes in central Italy and in other seismically-active
areas of central Europe often nucleate within, and propagate
through, carbonates in the upper crust. Two complementary ways
of understanding the mechanical behaviour of carbonates during
earthquake ruptures is to: 1) study exhumed faults, and; 2)
conduct laboratory experiments designed to simulate the
conditions that occur during earthquake rupture.
A variety of field and geophysical evidence suggests that
most displacement during individual earthquakes is localized to
thin Principal Slip Zones (PSZs) within the fault core. PSZs
potentially contain a record of passing earthquake ruptures and,
more generally, deformation mechanisms throughout the seismic
cycle. At present, however, there are no reliable microstructural
or geochemical indicators of seismic slip in carbonate rocks. In
addition, there is little information concerning the frictional
properties of carbonate at seismic slip speeds (i.e. 1-10m/s). In
this contribution, we present a detailed microstructural
characterization of the PSZs of active, large-displacement faults
from the Fucino basin in central Italy.
To gain insights in to fault mechanical behaviour, future work
will compare natural PSZ microstructures to those produced over
a wide range of slip speeds and normal stresses using a recentlyinstalled
rotary-shear friction apparatus at INGV, Rome.
NATURAL MICROSTRUCTURES
The PSZs we have studied are exhumed from

SESSIONE 1
Fig. 1 – Detailed map (A) and photomicrograph mosaic (B) showing 3 distinct ultracataclasite layers found adjacent to the main slip surface in one sample from
the Tre Monti fault, Fucino basin. Note the presence of: 1) a laterally-continuous, slip-surface-parallel calcite vein; 2) a sharp boundary between ultracataclasites
1 and 2.
28

Elastic properties evolution of the seismogenic Triassic Evaporites
and implications for crustal modeling
FABIO TRIPPETTA (*), CRISTIANO COLLETTINI (*), SERGIO VINCIGUERRA (**) & PHILIP G. MEREDITH (°)
Key words: Cyclic stressing, elastic moduli, evaporites,
laboratory experiments, seismic velocities.
Earthquakes up to M ~ 6 nucleate within the Triassic
Evaporites (TE) in the Northern Apennines of Italy, however this
lithology is generally considered as a ductile horizons incapable
of generating seismic rupture. TE are a sedimentary succession
made up of a sequence of alternating sulphates (anhydrites and
gypsum) and dolostones. The repeated seismic cycles lead to
deformation, increasing the level of damage of the host rocks and
hence changing their elastic moduli, which are key parameters for
petrophysical characterizations and for reliable modeling of
deformation processes. Therefore, here we focus on the elastic
properties of TE testing samples coming from outcrop and from
boreholes drilled in the central Italy. We obtained elastic
parameters from both seismic velocities measurements (Vp and
Vs) and increasing amplitude cyclic stressing experiments.
At ambient pressure, P-wave velocities are in the range 4.6-
6.6 km/s for dolostones, 4.1-6.2 km/s for anhydrites and 3.7-5.3
km/s for gypsum-dolostones. Borehole samples show higher
velocities respect to outcrop samples and the highest velocities
were registered for borehole samples coming from undeformed
areas. Cyclic loading provided highly variable unconfined
compressive strength values ranging from 10 MPa for outcrop
gypsum to ~ 200 MPa for borehole dolostones. However in all
experiments the Young's modulus and the Poisson's ratio increase
with increasing loading cycles. The increase in Young’s modulus,
and Poisson’s ratio is characterized by a non constant pattern
with increasing cycle number and it is more evident during the
first loading/unloading cycles. This behavior is likely to be
related to compaction-driven processes, in agreement with
microstructural observations that show an evident pore collapse
and increased crack damage as indicated from the
microseismicity output (Acoustic Emissions), recorded
throughout each experiment.
Calculated dynamic (velocity derived) and static
_________________________
(*) Dipartimento di Scienze della Terra, Università degli Studi di Perugia,
fabio.trippetta@unipg.it
(**) Istituto Nazionale di Geofisica e Vulcanologia, Roma
(°) Department of Earth Sciences, University College London, England
29
(deformation-test derived) elastic moduli on the same rock
samples have been then compared. Laboratory dynamic elastic
moduli are in agreement with elastic moduli used in several
models at the crustal scale however dynamic moduli are always
higher by two to three times respect to the static.
We interpret this behavior as due to frequency effects and we
suggest that static moduli need to be taken in account for
modeling slow deformation at the crustal scale.
SESSIONE 1

SESSIONE 1
The new release of the Database of Individual Seismogenic Sources,
DISS 3.1.1
PAOLA VANNOLI (*), SALVATORE BARBA (*), ROBERTO BASILI (*), PIERFRANCESCO BURRATO (*),
UMBERTO FRACASSI(*), VANJA KASTELIC (*), MARA MONICA TIBERTI(*) & GIANLUCA VALENSISE (*)
Key words: Active fault, active tectonics, DISS, seismic hazard,
seismogenic source.
The Database of Individual Seismogenic Sources (DISS) was
conceived at the end of the 1990s by a group of scientists at
Istituto Nazionale di Geofisica e Vulcanologia. The database was
designed to host data about seismogenic source models intended
to serve as geological input for ground-shaking SHA applications
and was continuously updated since then (BASILI et alii, 2008).
In 2005 there was a big turn in this process as we launched a
new version of the database (DISS 3) which augmented the
database with two innovative categories: the Composite
b)
Seismogenic Sources and the Debated Seismogenic Sources -
alongside of the native Individual Seismogenic Sources.
At this time we also made the database available online
30
through a dedicated web-dased GIS application. Its IT
infrastructure was also kept up to date and guidelines on how to
prepare new records have been distributed to potential
contributors (BASILI et alii, 2009).
During the years, DISS brought together a large amount of
published and original data on Italian seismogenic sources having
a potential for a magnitude 5.5+ earthquake and is now being
extended to the rest of the Euro-Mediterranean area.
We present highlights on the identification and
characterization of new seismogenic sources in four key-areas in
Italy, namely Lombardia-Emilia-Veneto (Southern Alps,
Northern Apennines), Adriatic Sea, Ionian Sea, and
Fig. 1 – Google-earth map of the DISS version 3.1.0 (DISS WORKING GROUP, 2009), current version available online. Polygons outline areas of significant
updates that will be illustrated at the meeting.
_________________________
(*) Istituto Nazionale di Geofisica e Vulcanologia, Roma,
paola.vannoli@ingv.it
Abruzzo/Molise (central Apennines). These new sources describe
youthful structures of the Alpine south-verging Apennine northverging
contractional systems, the external fold-and-thrust system
in the Adriatic and Ionian offshore, and the extensional domain of
the inner central Apennines. For each of these areas we illustrate
a combination of original data collected and interpreted by our
group together with reviews of published literature. We will also
outline contributions from several other scientists that

collaborated with us during the two-year term of “Project S1”
funded by the Dipartimento Protezione Civile (Agreement 2007-
2009).
The main novelties include updates of the geometric and
kinematic properties of seismogenic sources, new geological data
and numerical constraints on deformation rates, new
interpretations of faults that are thought to have generated a
number of historical earthquakes.
REFERENCES
BASILI R., VALENSISE G., VANNOLI P., BURRATO P., FRACASSI U.,
MARIANO S., TIBERTI M.M. & BOSCHI E. (2008) - The
Database of Individual Seismogenic Sources (DISS), version
3: summarizing 20 years of research on Italy's earthquake
geology. Tectonophysics, 453, 20–43,
doi:10.1016/j.tecto.2007.04.014.
BASILI R., KASTELIC V., VALENSISE G., & DISS WORKING GROUP
2009 (2009) - DISS3 tutorial series: Guidelines for compiling
records of the Database of Individual Seismogenic Sources,
version 3. Rapporti Tecnici INGV, 108, 20 pp.,
http://portale.ingv.it/produzione-scientifica/rapporti-tecniciingv/archivio/rapporti-tecnici-2009/.
DISS WORKING GROUP (2009) - Database of Individual
Seismogenic Sources (version 3.1.0): A compilation of
potential sources for earthquakes larger than M 5.5 in Italy
and surrounding areas. Available at:
http://diss.rm.ingv.it/diss.
31
SESSIONE 1

SESSIONE 1
Active tectonics in the Sannio Apennine: insights from the April-July
1990 Benevento seismic sequence
Key words: Active tectonics, Apennine chain, 1990 Benevento
earthquake, southern Italy.
The Sannio is a region of the Italian southern Apennine chain
that hosted destructive earthquakes in historical time.
Since April 1990, a low energy seismic sequence affected
again a small area of the region located N-NE of Benevento town
on the northern side of the Calore River.
The sequence, whose strongest shock (ML = 3.6) occurred
on April 22 with epicentre to NE of Benevento and hypocentral
depth located at about 15 km, lasted until July 1990. The
earthquakes caused material damage to the villages around the
epicentral area and no loss of lives.
Data from field survey on surface faulting coupled with a
reinterpretation of the available focal mechanism allow to
recognize that the area was acted upon by a NE-SW extension
coupled with a simultaneous NW-SE compression along faults
striking WNW-ESE and NNE-SSW respectively.
This resulted in both dextral and local reverse faulting as
already reported for other Apennine areas (DI BUCCI &MAZZOLI,
2003 and references therein).
Taking into account the regional geodynamic reference frame
and constraints, we suggest in agreement with DI BUCCI &
MAZZOLI (2003) that the active geodynamic setting of the 1990
seismic sequence was controlled by intraplate deformation of the
foreland of the Apennine chain, Adria, due to a NW-SE
convergence between the African and European plates.
REFERENCES
DI BUCCI D. & MAZZOLI S. (2003) - The October-November 2002
Molise seismic sequence (southern Italy): an expression of
Adria intraplate deformation. J. Geol. Soc., London, 160,
503-506.
_________________________
(*) Università degli Studi del Sannio, Facoltà di Scienze MM.FF.NN,
geo.adr@gmail.com
ADRIANO ZUPPETTA (*)
32

SESSIONE 2
Variazioni del livello del mare, eustatismo e tettonica
lungo le coste del Mediterraneo
CONVENERS
Paolo Roberto Federici (Università di Pisa)
Marta Pappalardo (Università di Pisa)
33
SESSIONE 2

SESSIONE 2
Key words: Coastal plain, late Holocene, lower Magra Valley,
northern Tyrrhenian Sea, relative sea level rise.
INTRODUCTION
Two geognostic surveys were performed, using a vibracorer,
in the plain surrounding the area of the ancient roman settlement
of Luni (lower valley of Magra River, NW Italy), today at the
border between Tuscany and Liguria and facing the northerrn
Tyrrhenian Sea. The cores were drilled during the month of
September in the successive years 2008 and 2009 and allowed to
collect several stratigraphic logs that show the progressive
evolution of the area during the late Holocene (BINI et alii, 2009).
Some of the cores were located within lagoons evolved in
their latest stages as marshes and swamps. Different
sedimentological palaeo sea level indicators of different ages
were identified in the logs. The aim of this work is to present the
sedimentological sea level indicators and to discuss, as work
hypothesis, their use to do a relative sea level rise curve for the
late Holocene in the eastern Liguria.
METHODS
Peat from paralic swamps is considered one of the most
reliable sea level indicators (PIRAZZOLI, 1991). It accumulates
where water surface discharge into the sea is retarded by beach
ridges or levees or in a lagoonal environment. A relative sea level
rise (RSLR) is assumed to be balanced by an accretion of peat
deposit while a sea level fall causes its weathering.
An abrupt marine incursion, however, erodes and disturbs
peat layers in coastal area. At the time of peat formation sea level
was slightly lower than sampling depth. If peat layers are not
_________________________
First remarks on the late Holocene relative sea level from
sedimentological palaeo sea level indicators in the lower Magra
Valley coastal plain
MONICA BINI (*), HELMUT BRÜCKNER (**), ALESSANDRO CHELLI (°) & MARTA PAPPALARDO (*)
(*) Dipartimento di Scienze della Terra, Università di Pisa,
bini@dst.unipi.it; pappalardo@dst.unipi.it
(**) Geographisches Institut, Universität zu Köln, h.brueckner@unikoeln.de
(°) Dipartimento di Scienze della Terra, Università di Parma,
achelli@unipr.it
34
available, wood fragments, plant remains or shells of marine
organisms can be used as sea level indicators (VÖTT, 2007).
The weight of the contribution to the sea level rise curve of
every dated sample has to be evaluated against its
geomorphologic and sedimentologic meaning. The height of
water column at the time of deposition of the sample should be
estimated in a realistic manner, through the modern analogues
found in neighbouring area. Nevertheless, considering the poor
number of data deriving from environments where today the
deposition of material similar to that used for the sea level rise
curve occurs directly influenced by the present day sea level, we
decide to use the uncertainty margins reported from the literature
(see BRUNETTI et alii, 1998 and VÖTT, 2007 and references
therein) discussing them in the light of the sedimentological
features of the logs considered.
Generally considering peat layers from coastal swamps,
palaeo sea level may be assumed within 50 cm below the depth of
the sample itself. If the sample derived from a thin layer of peat
(

Fig. 1 – Location map of the drilled cores.
Magra. The three cores are aligned along a N-S transect, roughly
directed from land (LUNI4) towards the sea (LUNI5).
In the core LUNI5 three potential sea level indicators have
been identified. The basal peat lying on the deposit representing
the fan of the Parmignola Stream, the creek descending towards
the sea from the hills backing the roman colony, has been dated at
about 5,840 years BP. At about 6 metres of depth, a piece of
wood deposited inside the lagoon yelded an age about 2,000
years younger than the basal peat. Finally, the sharp border
marking the passage between the lagoon and the overlying marsh
has been dated to about 2,700 years BP.
The cores LUNI4 and ORTO06 were drilled in two different
sites along the outer rim of the Seccagna area, representing the
rim of the area once occupied by the lagoon. Both the sequences
show a marsh lying directly on the deposit of the Parmignola
Stream alluvial fan. The gyttja representing the onset of the
marsh has been dated at about 2,200 year BP in ORTO06 while
the contact between the marsh and the overlying alluvial deposit
has been dated at about 300 years via a plant remain in LUNI4.
CONCLUSIONS
The sedimentological features interpreted as sea level
indicators were arranged in a relative sea level rise curve. Since
6,000 BP, the sea level was not higher than present day. The data
of the lower Magra River Valley were evaluated in comparison
with others from neighbouring areas discussing their meaning in
term of relative movement between land and sea.
35
REFERENCES
BINI M., CHELLI A., DURANTE A.M., GERVASINI L. &
PAPPALARDO M. (2009) – Geoarchaeological sea-level prozie
from a silted-up Harbour: A case study of the Roman colony
of Luni (northern Tyrrhenian Sea, Italy). Quat. Int., 206, 147-
157.
BRUNETTI A., DENEFLE M., FONTUGNE M., HATTE C. &
PIRAZZOLI P.A. (1998) – Sea-level and subsidence data from
a Late Holocene back-barrier lagoon (Valle Standiana,
Ravenna, Italy). Mar. Geol., 150, 29-37.
PIRAZZOLI P.A. (1991) – World Atlas of Holocene sea-level
changes. Elsevier Oceanogr., Ser. 58, Amsterdam, London,
New York, Tokyo.
VÖTT A. (2007) – Relative sea level changes and regional
tectonic evolution of seven coastal areas in NW Greece since
the mid-Holocene. Quat. Sci. Rev., 26, 894-919.
SESSIONE 2

SESSIONE 2
Contribute of sequence stratigraphy in the study of depositional
marine terraces: the Metaponto area example (southern Italy)
ANTONIETTA CILUMBRIELLO (*) LUISA SABATO (*) & MARCELLO TROPEANO (*)
Key words: Depositional marine terraces, sequence
stratigraphy, Southern Italy.
The hinterland of the Taranto Gulf (the Metaponto area)
represents a sector of the Bradanic Trough, that is the
Apenninic foredeep in southern Italy. It is characterized by the
occurrence of coarse-grained Quaternary deposits that represent
the outcropping and upper part of the Bradanic Trough infill.
36
These coarse-grained deposits are coastal s.l. in origin and
historically viewed as linked to a flight of marine terraces
developed during Middle and Late Pleistocene (Fig. 1).
A detailed sedimentological and stratigraphic study was
performed in a selected part of the Metaponto area, between
Cavone and Basento Rivers; the analysed successions are very
complex and record high-frequency relative sea-level changes.
Following a sequence-stratigraphic approach, several fourth-
Fig. 1 – Geological setting of the study area (from CILUMBRIELLO et alii, 2008, after BRÜCKNER, 1980, and SELLA et alii, 1988).
_________________________
(*) Dipartimento di Geologia e Geofisica, Università "Aldo Moro" di Bari,
m.tropeano@geo.uniba.it
order sequences made up of different systems tracts comprised
of higher-order sequences (either simple sequences or sets of
simple sequences) may be recognized.
Highstand Systems Tracts (HST) within fourth-order
sequences are the best developed features and mainly

Fig. 2 – Sequence stratigraphic interpretation of depositional marine tarraces in the study area (after CILUMBRIELLO 2008 and CILUMBRIELLO et alii, 2008,)
correspond to sets of simple sequences; sets are
stratigraphically organized in a downward shifting
configuration. According to chronostratigraphic data, these
fourth-order HSTs may be referred to interglacial stages 9, 7,
and 5 of the OIT/RSL curve (OIT = Oxygen Isotope Timescale;
RSL = Relative Sea-Level curve) (Fig. 2).
Within each fourth-order HST, the HST of the highest
simple sequence of each set corresponds to a coastal sigmoidal
body, the top of which is a terraced surface. Only the HSTs of
these simple sequences may be viewed as “classic” depositional
marine terraces. According to chronostratigraphic data, these
HSTs of simple sequences may be correlated to substages of
OIT/RSL curve, namely to MIS (Marine Isotope Stage) 9.5,
9.3, 9.1, 7.5, 7.3, 7.1, 5.5, 5.3, and 5.1.
Detailed facies analyses, stratigraphic correlations of the
measured sections, and sequence-stratigraphic considerations
show that the terraced marine-deposits cropping out in the
Metaponto area record high-frequency relative sea-level
changes, each of which can not be simply linked to a terraced
surface. A higher number of sea-level oscillations is locally
recorded below each terraced surface, and studies based only
on geomorphological evidences are unable to describe the
complex interaction between regional uplift and relative sealevel
changes. Sequence stratigraphy may be an useful tool to
37
better define the development of these terraced marinedeposits,
the terraced surface being genetically linked only to
the upper part of a flat topped marine succession.
REFERENCES
BRÜCKNER H. (1980) - Marine Terrassen in Süditalien. Eine
quartärmorphologische Studie über das Küstentiefland von
Metapont. Düsserdolfer Geographische Schriften 14, 225
pp.
CILUMBRIELLO A. (2008) - Stratigrafia sequenziale dei depositi
del Pleistocene medio-superiore del metapontino
nell’evoluzione del bacino di avanfossa appenninico
meridionale. PhD Thesys, Università di Bari, 105 pp.
CILUMBRIELLO A., TROPEANO M. & SABATO L. (2008) - The
Quaternary terraced marine-deposits of the Metaponto
area (Southern Italy) in a sequence-stratigraphic
perspective. Geoacta, Sp. Publ.. 1, 27-54.
SELLA M., TURCI C. & RIVA A. (1988) - Sintesi geopetrolifera
della Fossa bradanica (avanfossa della catena appenninica
meridionale). Mem. Soc. Geol. It., 41, 87-107.
SESSIONE 2

SESSIONE 2
Key words: Neogene-Quaternary sequence, radiocarbon dating,
Scarlino Plain.
INTRODUCTION
The Scarlino Plain represents the coastal sector of the Pecora
River catchment. It is a depression filled with a succession of
Neogene - Quaternary sediments up to 200 meters thick
(TANELLI, 2009). In 1998-2000 the arsenic problem in the
Scarlino Plain was firstly identified, when high As levels were
recognized in soils, sediments and in piezometers monitoring the
shallow groundwater (COSTAGLIOLA et alii, 2010). Since then
many geochemical, mineralogical and stratigraphic studies have
been carried out, by the Environmental Protection Regional
Agency of Tuscany and the Department of Earth Sciences of the
University of Florence.
These studies pointed out that the As in the Scarlino Plain is
the result of both geogenic (erosion of As-rich rocks, followed by
river transport and deposition) and anthropogenic (leaching of
As-rich waste piles, related the industrial plant located in the
Casone area in the Scarlino Plain to produce sulfuric acid)
sources.
Two boreholes (La Botte and Vetricella) were drilled in the
Scarlino Plain, in order to analyze the arsenic distribution within
the Neogene-Quaternary succession. La Botte borehole is located
in the central-distal part of the plain, whereas the Vetricella
borehole is in the proximal part of the plain, about 3,5 km north
of the first one. La Botte is 147 m long and intercepted the
Ligurian bedrock at 141 m b.s. The Vetricella borehole is 92 m
long and it is drilled exclusively within the Neogene-Quaternary
sediments; the drilling has been stopped near the bedrock
identified through geoelectrical surveys (ROSSATO et alii, 2009).
The detailed stratigraphic analysis of La Botte and Vetricella
cores identified continental sediments typical of a fluvial
environment. We recognize the alternation of coarse channel and
floodplain deposits, interlayered with mass flow deposits typical
of a foot slope. These sediments are in large part related to
paleoPecora River, and to a paleoPecora tributary, similar to the
present-day, Gora delle Ferriere creek.
_________________________
Preliminary radiocarbon datings of Late Quaternary sediments in
the Scarlino Plain (Grosseto, Italy)
(*) Dipartimento di Scienze della Terra, Università di Firenze,
francesca.dughetti@unifi.it
(**) INFN Sezione di Firenze
Lavoro eseguito nell’ambito del progetto Prin 2006 (G. Tanelli) con il
contributo finanziario del MIUR, dell’Università di Firenze e dell’ARPAT.
FRANCESCA DUGHETTI (*), LUCA ROSSATO (*), MARIAELENA FEDI (**),
G.
MARCO BENVENUTI (*) & GIUSEPPE TANELLI (*)
38
RADIOCARBON DATINGS
In this contest, some radiocarbon datings of the first 20 m of
the Late Quaternary succession in the La Botte and Vetricella
boreholes have been performed in order to calibrate the
paleogeographic reconstruction of Scarlino Plain. Furthermore
these radiocarbon datings, the first measurements of the Scarlino
Plain chronology, could help us to better define the conceptual
model concerning the As anomaly in the plain.
For the radiocarbon measurements one charcoal fragment
and six sediment samples (bulk analysis) (WATANABE et alii,
2007; CHITI et alii, 2008) have been collected.
For bulk analysis six samples of sediments were taken, two in
La Botte borehole (at 10 m b.s. and 16 m b.s. respectively) and
four in Vetricella borehole (at 4, 7, 17.5 and 20 m b.s.
respectively).
After the chemical pre-treatment of sediment samples,
conducted using the AAA method for the extraction of humus
fraction (XU &ZHENG, 2003), only for two sediment samples we
have obtained sufficient humic acids for the radiocarbon datings
(LB10 and LV20). The charcoal (LB5.5) and sediments (LB10
and LV20) radiocarbon analyses were performed performed by
Accelerator Mass Spectrometry (AMS) at the INFN-LABEC of
Florence (FEDI et al., 2007).
The samples analyzed from La Botte borehole are located,
starting from the top of the stratigraphic sequence, at 5.5 m b.s.
(charcoal sample labelled LB5.5) and at 9.5 m b.s. (labelled
LB10) respectively. The first one is related to unit a consisted of
gravels in a muddy matrix with an important organic fraction,
and the second one comes from unit b characterized by gravels
in a muddy matrix. The LV20 sample was taken at a depth of 20
m b.s. in Vetricella borehole, and it corresponds to the unit c
which consists of pelitic layers interbedded by sand and gravels
levels.
Since the samples have been taken from both the boreholes, a
spatial stratigraphic correlation can be made in order to compare
the obtained values as illustrated in Fig.1.
The calibrated ages for the LB5.5 (3904-5644 years before
present) and LB10 (8705-9527 years before present) are related
to the stratigraphic units labelled a and b respectively, both in
Vetricella and La Botte boreholes.
It is particular interesting to note that the sample LV20 has a
rather wide calibrated age range (about 3000 years), between 15-
18 Ka before present, a period that was characterized by major
climatic changes. The last glacial peak, called LGM (Last Glacial

Maximum) is in fact dated around 20 Ka b.p., while in the age
range from 15 to16 Ka there was a reversal in a post-glacial
Fig. 1 – In figure are shown the first 20 m of Quaternary sequence in La Botte
and Vetricella boreholes. The samples for radiocarbon datings and the
calibrated ages obtained by measure (years before present) are indicated in the
columns. At right of the columns are shown the average sedimentation rates.
With a, b, c are labeled the stratigraphic units.
phase (OROMBELLI et alii, 2005).
The sample LV20 belongs to a unit which consists of constant
stratigraphic thicknesses across the investigated Scarlino plain,
with a slight deepening in La Botte area (unit c). This deepening,
limited to the axial zone of the plain suggests a paleovalley
related to the post-glacial phase mentioned above. In this phase
the sea-level went back closer to the valley area thus allowing a
more uniform sediments deposition, that forms the flood plain. It
is therefore more reliable for the sample LV20 a calibrated age
close to lower limit of the dating range (15 Ka); whereas the
deposits that represent the previous glacial period are probably
related to the lower stratigraphic units.
A rough calculation of the sedimentation rate, considering the
radiocarbon ages of the measured samples and their depths (5.5
m, 10 m and 20 m b.s.), provide an average rates of 1.29 – 1.08
mm/yr (Fig. 1). These values are congruent with the mean
sedimentation rate reported for the Ombrone alluvial plain
(BISERNI &VAN GEEL, 2005).
The data discussed here represent the first geochronological
data in the Scarlino Plain and these are an important help to
understand the stratigraphy of the area above all related to the
39
glacial – postglacial phases in the coastal area of Tuscany during
the Late Quaternary.
REFERENCES
BISERNI G. & VAN GEEL B. (2005) - Reconstruction of
Holocene palaeoenvironment and sedimentation history of the
Ombrone alluvial plain (South Tuscany, Italy). Rev. Palaeobot.
Palyno., 136, 16-28.
CHITI T., NEUBERT R.E.M., JANSSENS I.A., CERTINI G.,
CURIEL YUSTE J. & SIRIGNANO C. (2008) - Radiocarbon dating
reveals different past managements of adjacent forest soils in the
Campine region, Belgium. Geoderma, 149, 137-142.
COSTAGLIOLA, P.,BENVENUTI, M.M., BENVENUTI, M.G., DI
BENEDETTO F. & LATTANZI P. (2010) - Quaternary sediment
geochemistry as a proxy for toxic element source: A case study of
arsenic in the Pecora Valley (southern Tuscany, Italy). Chem.
Geol. 270, 80-89.
FEDI M.E.,CARTOCCI A., MANETTI M. , TACCETTI F. &
MANDÒ P.A. (2007) - The 14 C AMS facility at LABEC, Florence.
Nucl. Instrum. Meth B, 259, 18-22.
OROMBELLI G., RAVAZZI C. & CITA M.B. (2005) -
Osservazioni sul significato del termine LGM (UGM)
tardoglaciale e postglaciale in ambito globale, italiano e alpino.
Il Quaternario, 18 (2), 147-155.
ROSSATO L., GABBANI G., TANELLI G. (2009) - Geoelectrical
survey in Scarlino plain (Southern Tuscany).
10.1474/epitome.03.1738. Geoitalia, VII Forum Italiano Di
Scienze Della Terra, Rimini, 9-11 settembre 2009.
TANELLI G. (2009) – La zona mineraria di Boccheggiano-
Montieri e gli impianti di Scarlino. In: Georisorse e Ambiente.
Aracne Editore, Roma (ISBN 978-88-548-2615-1), 78-93.
WATANABE T.A., NAKAMURA T.A & KAWAI T.B. (2007) -
Radiocarbon dating of sediments from large continental lakes
(Lakes Baikal, Hovsgol and Erhel). Nucl. Instrum. Meth, 259 (1),
565-570.
XU S. & ZHENG G. (2003) - Variations in radiocarbon ages of
various organic fractions in core sediments from Erhai Lake, SW
China. Geochem. J., 37, 135-144.
SESSIONE 2

SESSIONE 2
Key words: Marine terraces, Policastro Gulf, Quaternary,
Southern Apennines Thyrrhenian margin.
INTRODUCTION
The Tyrrhenian margin of the Southern Apennines is defined
by the alternation of large bays and headlands, which represent
the surface expression of a horst-and-graben structure related to
major NE-trending faults (e.g. MOUSSAT et alii, 1986). This
structure, which developed during the Quaternary, represents the
response to NW-trending stretching which governed sea-floor
spreading in the southern portion of the Tyrrhenian extensional
basin (e.g. KASTENS et alii., 1990; CAIAZZO et alii, 2006). Based
on subsurface and offshore data, the peri-Tyrrhenian grabens
were affected by Quaternary subsidence on the order of 2000-
3000 m (IPPOLITO et alii, 1973; BIGI et alii, 1983; BRANCACCIO
et alii, 1991). Since middle Pleistocene times, extension in the
northern grabens was accompanied by volcanic activity (e.g.
BROCCHINI et alii, 2001; MILIA et alii, 2003). In the late
Quaternary, large sediment supply by major fluvial basins and
volcanoes and slower subsidence, allowed the development of
coastal plains in the inner portions of the Garigliano, Campano,
and Salerno Gulf grabens. Coeval to the peri-Tyrrhenian graben
subsidence, uplift of the interposed horst blocks took place. This
is shown by the flights of marine terraces well preserved in the
carbonate headlands, which develop up to some hundreds of
metres of elevation.
In the rocky coastal belt of the Policastro gulf, several marine
terraces are preserved. In addition, coastal (with shore and fan
delta facies) and alluvial deposits and subaerial landforms are
locally present. These deposits and landforms provide constraints
to the amount and timing of vertical motions (both absolute and
relative) which affected the Policastro gulf coastal perimeter, and
allow outlining the style of the extensional tectonics which
affected the Southern Apennines Tyrrhenian margin during the
Quaternary.
_________________________
The marine terraces of the Policastro Gulf: new insights on the
evolution of the southern Apennines Tyrrhenian margin
FRANCESCA FILOCAMO (*), ALESSANDRA ASCIONE (*) & PAOLA ROMANO (*)
(*) Dipartimento di Scienze della Terra, Università degli Studi di Napoli
“Federico II”, filocamo@unina.it, ascione@unina.it, paromano@unia.it
40
Fig. 1 – The Policastro Gulf coastal belt. In the gray rectangles are given the
elevation (m a.s.l.) of the highest paleo-shorelines and their chronological
attributions: EP=Early Pleistocene, MP=Middle Pleistocene.
THE POLICASTRO GULF COASTAL BELT
The stratigraphical, geomorphological and morphostructural
study carried out in the Policastro graben coastal belt, from Mt.
Bulgheria headland (Campania) to the Lao river plain (northern
Calabria, Fig.1), has shown that both the amount and maximum
elevation of uplifted marine terraces are uneven moving along
this rocky coast. The richest successions of deposits and
landforms occur in the northwestern border of the Policastro
graben (Mt. Bulgheria headland), and in the Torre S. Nicola-Lao
river outlet sector (in which a flight of ten terrace orders is
present). In these two areas, the highest marine terraces are
located at 400 m and 240 m a.s.l. respectively.
Biostratigraphical data, and integrated paleoecological,
biostratigraphical and paleomagnetic data, constrain marine
terraces at 400 m and 280 m a.s.l. in Mt. Bulgheria area to the
early Santernian and to the early Emilian respectively (ASCIONE
&ROMANO, 1999; CAIAZZO et alii, 2006), and the 100 m a.s.l.
marine terrace in the Torre S. Nicola-Lao river sector to the early
Middle Pleistocene (MIS 19–15) based on the age of the Fornaci
S. Nicola marine succession (FILOCAMO et alii, 2009).

Other sectors of the coastal belt are characterized by a lesser
amount of terraces and by lower elevation of the highest
shorelines, e.g.: (i) in the Noce river coastal plain the highest
shore deposits are raised up to 170 m a.s.l., (ii) in the Sapri gulf
coastal belt the highest terraces are found 100 m a.s.l., and (iii) in
the Maratea coastal sector small size abrasion terraces reach 70-
75 m of elevation (FILOCAMO, 2007).
Collectively, evidences from the Policastro area are
interpreted as the result of the dyachronous (spanning from the
early Santernian to the middle Pleistocene) outline of the coastal
perimeter. The latter is related to the fragmentation of the
Tyrrhenian margin by NE-trending and NW-trending faults
bounding minor horst and graben structures.
CONCLUDING REMARKS
Data from the Policastro gulf coastal belt provide constraints
to the Quaternary evolution of this area. In addition, the
Policastro gulf coastal belt provides new insights on the evolution
of the Southern Apennines Tyrrhenian margin. In this area, in
fact, evidences relevant to unravel the style of Tyrrhenian
extensional processes, which are largely obscured by thick
alluvial covers in the western borders of the more northerly peri-
Tyrrhenian grabens, are exposed on surface.
The western border of the Policastro graben reflects the major
horst-and-graben structure of the Tyrrhenian margin of the
Southern Apennines. This block faulting may be essentially
framed in early Pleistocene times, a time span during which local
subsidence episodes (well testified in Mt. Bulgheria and in the
Noce and Lao river plains) took place. Since the Middle
Pleistocene, the uplift trend became dominant in the whole
coastal belt. This was probably accompanied by minor
differential motions, as suggested by the slight uplift of the Late
Pleistocene paleo-shorelines (ESPOSITO et alii, 2003) in the
northwestern border of the graben.
REFERENCES
ASCIONE A. & ROMANO P. (1999) - Vertical movements on the
eastern margin of the Tyrrhenian extensional basin. New data
from Mt. Bulgheria (Southern Apennines, Italy).
Tectonophysics, 315, 337-356.
BIGI G., COLI M., COSENTINO D., PAROTTO M., PRATURLON A.,
SARTORI R., SCANDONE P. & TURCO E., (Eds.) (1983) -
Structural Model of Italy. C.N.R., Progetto Finalizzato
Geodinamica, Roma.
BRANCACCIO L., CINQUE A., ROMANO P., ROSSKOPF C., RUSSO
F., SANTANGELO N. & SANTO A. (1991) - Geomorphology
and neotectonic evolution of a sector of the Tyrrhenian flank
41
of the Southern Apennines (Region of Naples, Italy). Z.
Geomorph., Suppl. -Bd. 82, 47-58.
BROCCHINI D., PRINCIPE C., CASTRADORI D., LAURENZI M.A. &
GORLA L. (2001) - Quaternary evolution of the southern
sector of the Campana Plain and early Somma-Vesuvius
activity: insight from the Trecase 1 well. Mineral. Petrol., 73,
67-91.
CAIAZZO C., ASCIONE A. & CINQUE A. (2006) - Late Tertiary-
Quaternary tectonics of the Southern Apennines (Italy): New
evidences from the Tyrrhenian slope. Tectonophysics, 421,
23-51.
ESPOSITO C., FILOCAMO F., MARCIANO R., ROMANO P.,
SANTANGELO N., SCARCIGLIA F. & TUCCIMEI P. (2003) - Late
Quaternary shorelines in southern Cilento (Mt. Bulgheria):
morphostratigraphy and U/Th chronology. Il Quaternario, 16
(1), 3-14.
FILOCAMO F. (2007) - Evoluzione quaternaria del margine
tirrenico dell’Appennino meridionale tra il Golfo di Sapri e
la foce del fiume Lao: studio stratigrafico e geomorfologico.
PhD Thesis, Università degli Studi di Napoli Federico II.
Available at http://www.fedoa.unina.it.
FILOCAMO F., ROMANO P., DI DONATO V., ESPOSITO P., MATTEI
M., PORRECA M., ROBUSTELLI G&RUSSO ERMOLLI E (2009)
- Geomorphology and tectonics of uplifted coasts: New
chronostratigraphical constraints for the Quaternary
evolution of Tyrrhenian North Calabria (southern Italy).
Geomorphology, 105 (3-4), 334-354.
IPPOLITO F., ORTOLANI F. & RUSSO M. (1973) - Struttura
marginale tirrenica dell’Appennino campano:
reinterpretazione di dati di antiche ricerche di idrocarburi.
Mem. Soc. Geol. It., 12, 227-250.
KASTENS K., MASCLE J. et al. (Eds.) (1990) - Proceedings of
Ocean Drilling Program, Scientific Results 107. Ocean
Drilling Program, College Station, TX
MILIA A., TORRENTE M.M., RUSSO M. & ZUPPETTA A. (2003) -
Tectonics and crustal structure of the Campania continental
margin: relationships with volcanism. Mineral. Petrol., 79,
33-47.
MOUSSAT E., REHAULT J.P. & FABBRI A. (1986) - Rifting et
èvolution tectono-sèdimentaire du Bassin Tyrrhènien au cours
du Neogene et du Quaternaire. Gior. di Geol., ser. 3, 48 (1/2),
41-62.
SESSIONE 2

SESSIONE 2
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SESSIONE 2

SESSIONE 2
Key words: Eustasy, MIS 5, sea level change, sea level indicator,
southern Italy.
The studies on the reconstruction of Quaternary sea level
history are based on several methodological approaches, the main
relying on the following criteria:
i) oxygen isotope ratios are used to infer continental ice
volume estimates and thus sea level history;
ii) local sea level curves are predicted on the basis of glaciohydro-isostatic
models;
iii) field data are collected by surveying the geological sea
level indicators on tectonically stable areas in order to reconstruct
the eustatic sea level fluctuations in terms of number, vertical
amount and duration. Such reconstructions are more reliable
whether stable areas include different geomorphological settings
allowing different types of sea level markers to be correlated.
The Campania sector of the southern Apennines Tyrrhenian
belt is a very favourable geological context for studying the
Quaternary sea level history. This area is characterised by coastal
geomorphological land systems varying from submerged to
uplifted rocky coasts interrupted by prograding coastal plain, and
giving rise to alternating high-energy and sheltered coastlines.
The Campania regional tectonic setting is quite
undifferentiated. With the exception of the Campanian Plain
coastal graben, which was affected by volcano-tectonic ground
movements, the pattern of the vertical displacement, emerging
from investigation on the MIS 5.5 marker, is that of a
substantially stable region during the late Quaternary. The
headlands (Sorrento Peninsula and Cilento) bounding the peri-
Tyrrhenian tectonic depressions have been stable to slightly
uplifting (average rate of 0.1/0.01 mm/y) during the last 130 ka;
in this time span the Sele plain/Salerno gulf graben underwent a
mean uplift trend of 0.1 mm/y while the northernmost Garigliano
coastal plain was stable. These rates are based on total vertical
displacements of 2/4 meters during the last 130 ka, thus of the
same order of the uncertainty affecting the determination of the
eustatic sea level elevation during the MIS 5.5 highstand.
In the last decades, several researches on the geological
_________________________
The sea level changes during the MIS 5: eustatic fluctuation data
from the southern Tyrrhenian coasts of Italy
PAOLA ROMANO (*), ALESSANDRA ASCIONE (*), FRANCESCA FILOCAMO (*) & NICOLETTA SANTANGELO (*)
(*) Dipartimento di Scienze della Terra, Università di Napoli Federico II,
paromano@unina.it, ascione@unina.it, filocamo@unina.it, nicsanta@unina.it
44
record of sea level along the southern Apennine Tyrrhenian
coasts have been carried out by the geomorphologists of the
University of Naples Federico II (BRANCACCIO et alii, 1978,
1986, 1990; CINQUE &ROMANO, 1990; BARRA et alii, 1991;
BARATTOLO et alii, 1992; ROMANO et alii, 1992; ANTONIOLI et
alii, 1994; ROMANO et alii, 1994; IANNACE et alii, 2001; RICCIO
et alii, 2001; ESPOSITO et alii, 2002; IANNACE et alii, 2003;
FERRANTI et alii, 2006; MARCIANO et alii, 2008; SANTANGELO et
alii, 2010). They were addressed to the strandlines survey and
dating and to the study of associate continental deposits as well,
the latter being also fruitful in providing chronological constraints
for the sea level markers. At this aim, U-series dating on
carbonate concretions (speleothems and carbonates formed in
supersaturated marine waters) or geochemical analyses of
pyroclastic fallout deposits were also performed. The resulting
framework consists in a detailed paleo-shoreline reconstruction of
the Campania region dating back to the Last Interglacial, and in a
rich elevation/age data set concerning the sea level fluctuations
during MIS 5, by which several relative sea level curves are
reconstructed.
By the data set it results that, with the exception of the slight
post-Eutyrrhenian offset affecting the southern Campania coasts,
the shapes of the different curves, i.e. number, amplitude and
elevation of the sea level highstands occurred during MIS 5.5,
MIS 5.3 and MIS 5.1, are comparable. This suggests that the
obtained curves reflect the eustatic behaviour of the sea level in
the MIS 5. In particular, the curves point to the occurrence of a
double peak during the MIS 5.5 (which is also evidenced by
global data), and to a fluctuating sea level position around the
present day datum during MIS 5.3 and MIS 5.1. These sea level
positions are consistent with field data from other stable coasts of
the western Mediterranean sea, e.g. the Baleari islands.
REFERENCES
ANTONIOLI, F.,CINQUE A., FERRANTI L. & ROMANO P. (1994) -
Emergerd and submerged Quaternary marine terraces of
Palinuro Cape (Southern Italy). Mem. Descr. Carta Geol.
d’It., 52, 237 -260.
BARRA D., CINQUE A., GEWELT M. & HURTGEN C. (1991) -
L’ospite caldo Sylvestra semins (Bonaduce, Masoli e
Pugliese, 1976) (Crustacea, Ostracoda): un possibile marker

dell’ultimo interglaciale dell’area mediterranea. Il
Quaternario, 4, 327-332.
BARATTOLO F., CINQUE A., D'ALESSANDRO E., GUIDA M.,
ROMANO P. & RUSSO ERMOLLI E. (1992) - Geomorfologia ed
evoluzione tettonica quaternaria dell’isola di Capri. Studi
Geologici Camerti, Volume Speciale 1992/1, 265-269.
BRANCACCIO L., CAPALDI G., CINQUE A., PECE R. & SGROSSO I.
(1978) - 230 Th- 238 U Dating of corals from a Tyrrhenian beach
in Sorrentine Peninsula (Southern Italy). Quaternaria, 20,
175-183.
BRANCACCIO L., CINQUE A., BELLUOMINI G., BRANCA M.&
DELITALA L. (1986) - Isoleucine Epimerization dating and
tectonic significance of Upper Pleistocene sea-level features
of the Sele Plain (Southern Italy). Z. Geomorph. N.F., Suppl.
Bd. 62,159-166.
BRANCACCIO L., CINQUE A., RUSSO F., BELLUOMINI G., BRANCA
M. & DELITALA L. (1990) - Segnalazione e datazione di
depositi marini tirreniani sulla costa campana. Boll. Soc.
Geol. It., 109, 259-265
CINQUE A. & ROMANO P. (1990) - Segnalazione di nuove
evidenze di antiche linee di riva in Penisola sorrentina
(Campania). Geogr. Fis. Dinam. Quat., 13, 23-36.
ESPOSITO C., FILOCAMO F., MARCIANO R., ROMANO P.,
SANTANGELO N., SCARCIGLIA F. & TUCCIMEI P. (2002) – Late
Quaternary shorelines in southern Cilento (M. Bulgheria):
morphostratigraphy and chronology. Il Quaternario, 16 (1),
11-22.
FERRANTI L., ANTONIOLI F., MAUZ B., AMOROSI A., DAI PRA G.,
MASTRONUZZI G., MONACO C., ORRU P., PAPPALARDO M.,
RADTKE U., RENDA P., ROMANO P., SANSÒ P. & VERRUBI V.
(2006) – Markers of the last interglacial sea level high stand
along the coast of Italy: Tectonic implications. Quat. Int.,
145, 30-54.
IANNACE A., ROMANO P., SANTANGELO N., SANTO A., &
TUCCIMEI P. (2001) – The OIS 5c along Licosa cape
promontory (Campania region, southern Italy):
morphostratigraphy and U/Th dating. Z. Geomorph. N.F., 45
(3), 307-319.
IANNACE A., ROMANO P. & TUCCIMEI P. (2003) – U/Th dating
and geochemistry of carbonate concretions associated with
Upper Pleistocene fossil shorelines of the Sorrento Peninsula
(Conca dei Marini, southern Italy). Il Quaternario – Volume
Speciale INQUA, Ital. J.Quat. Sci., 16 (1Bis), 49-54.
MARCIANO R., MUNNO R., PETROSINO P., SANTANGELO N.,
SANTO A. & VILLA I. (2008) - Late quaternary tephra layers
along the Cilento coastline (southern Italy). J. Volcanol.
Geoth. Res., 177, 227–243.
45
RICCIO A., RIGGIO F. & ROMANO P. (2001) – Sea level
fluctuations during Oxygen Isotope Stage 5: new data from
fossil shorelines in the Sorrento Peninsula (Southern Italy).
Z. Geomorph. N.F. 45, (1), 121-137.
ROMANO P. (1992) - La distribuzione del Pleistocene marino
lungo le coste della Campania: stato delle conoscenze e
prospettive di ricerca. Studi Geologici Camerti, Volume
Speciale 1992/1, 265-269.
ROMANO P., SANTO A. & VOLTAGGIO M. (1994) - L’evoluzione
geomorfologica della pianura del Fiume Volturno
(Campania) durante il tardo Quaternario (Pleistocene mediosuperiore-
Olocene). Il Quaternario, 7 (1), 41-56.
SANTANGELO N., CIAMPO G., DI DONATO V., ESPOSITO P.,
PETROSINO P., ROMANO P., RUSSO ERMOLLI E., SANTO A.,
TOSCANO F. & VILLA I. (2010) - Late Quaternary buried
lagoons in the northern Campania plain (southern Italy):
evolution of a coastal system under the influence of volcanotectonics
and eustatism. Ital. J. Geosci . (Boll.Soc.Geol.It.),
129 (1), 156-175.
SESSIONE 2

SESSIONE 2
Submerged shorelines off the Gallinara Island (Ligurian Sea, NW
Mediterranean)
Key words: Ligurian Sea, marine landforms, underwater
geomorphology.
INTRODUCTION
In coastal stable to slowly uplifting/subsiding areas, most of
the marine landforms produced during Middle and Late
Quaternary are presently submerged. Even though sedimentation
can rapidly obliterate coastal landforms in many underwater
contexts, along submerged promontories and coastal islands
usually the sedimentation is low and landforms inherited by past
sea levels can be identified and mapped. In this study we focus on
the submerged coastal area of the Gallinara Island, located in the
NW Mediterranean Sea (Fig.1) in order to describe its
geomorphological features, in particular those inherited by past
sea levels.
The Gallinara Island is characterized by rocky cliffs of
quartzites interbedded with strata of polygenic conglomerates
(Quarziti di Monte Bignone Unit - Creataceous). For its
coastlines have not been reported evidences of emerged paleo
shorelines, while in the coastal sector facing it (Alassio) OXILIA &
VICINO, 1984 report a shoreline attributed to MIS 5.5 located at
about 4 meters asl. In general, along the coastline comprised
between Savona and Ventimiglia, the paleo-shoreline elevations
relative to MIS 5.5 have been reported from 5 to 12 m a.s.l.
(FEDERICI &PAPPALARDO, 2006 and reference therein); the Late
Quaternary tectonic behavior of this coastal tract is thus
considered typical of stable to slowly uplifting areas
(AMBROSETTI et alii, 1987).
Surveys were carried out using scuba diving techniques in
four transects and eight spot diving surveys within the study area
(Fig.1). Aerial photos allowed to identify the presence/absence of
seagrass meadows in the shallow part of the study area.
_________________________
(*) Dip.Te.Ris., Università degli studi di Genova, alessio.rovere@unige.it
ALESSIO ROVERE (*), MATTEO VACCHI (*) & MARCO FIRPO (*)
46
RESULTS AND DISCUSSIONS
Surveys allowed to draw a geomorphological sketch map of
the study area (Fig.1). The eastern and southern parts of the
island are characterized by plunging cliffs, separated by a large
rockfall ending at 27-30 m depth. In this sector, a slope rupture is
evident both in the rockfall deposit and in the cliff at 15-20 m
depth. Several caves of structural origin (differential erosion of
strata) have been identified along these cliffs at -24/-26 m. These
caves appear to have been reworked by the sea, as their walls are
characterized by abrasion notches decreasing in amplitude
towards the closure of the cave. The other sectors of the island
show a different morphology: the cliff ends at 5-8 m depth in
rockfall deposits. In general, at 25-30m depth, the rockfall
deposits are substituted by loose sediments.
The surveys carried out in the study area allowed to identify
some evidence which could be related to former shorelines: the
slope rupture at 15-20 m depth, and the reworked caves at 27-30
m depth could in fact represent respectively the outer margin of a
marine terrace, and the effect of marine abrasion in a shallow or
coastal environment. These levels appear to be in bathymetric
analogy with those found in several stable to slowly uplifting
areas along the Italian coastlines. Nevertheless, this interpretation
calls for more reliable data for which concern: i) marine origin of
the observed landforms, and more precise depth of the sea
level(s) associated to them. It is possible that the two elements
represent different aspects of the same shoreline: while the upper
marine terrace was forming, the caves were shaped by marine
abrasion in shallow (7-10m) water. Nowadays, the caves are no
more subjected to marine abrasion. ii) Age of the ancient sea
level(s): as no direct chronological constraint is possible, due to
the absence of dateable material, hypotheses can be made on the
basis of bathymetric cross-correlations. According to the present
knowledge, the coastal part of the study area can be considered
tectonically stable, and the glacio-hydro isostatic rebound
characterizing it after LGM can be constrained within few meters
(BARD et alii, 2002). Under such conditions, any sea level
observed through a geomorphological marker can be in first
approximation compared with its eustatic value, without further
corrections for tectonic or isostatic effects. According to eustatic
curves (e.g. WAELBROECK et alii, 2002), different Marine Isotope
Stages (5.1, 5.3, 7.1, 7.3 and 7.5) peaked below MIS 5.5 and 1

Fig. 2 –Geomorphological sketch map of the underwater part of Gallinara Island and location of transects and spot diving surveys.
sea levels and near the levels described in this study. Therefore,
the shorelines identified in this study can have been shaped by
one or more sea level highstands lower than the present one. In
the case of their MIS 7 age, further studies would be needed to
identify the causes of their preservation during two entire glacial
cycles (MIS 6 and MIS 2).
REFERENCES
OXILIA M. & VICINO G. (1984) - Scoperta di un livello marino
fossilifero del quaternario ad alassio (Savona). Riv. Ing.e Int.
3-4, 85-86.
FEDERICI P. & PAPPALARDO M. (2006) - Evidence of MIS 5.5
highstand in Liguria (Italy) and its tectonic significance.
Quat. Int. 145-146, 68-77.
AMBROSETTI P., BOSI C., CARRARO F., CIARANFI N., PANIZZA M.,
PAPANI G., VEZZANI L.& ZANFERRARI A. (1987) - Neotectonic
Map of Italy, Scale 1:500 000. CNR, Rome.
BARD E., ANTONIOLI F. & SILENZI S. (2002) - Sea-level during the
penultimate interglacial period based on submerged
stalagmite from Argentarola cave (Italy). Earth and Plan. Sc.
Lett. 196 (3-4), 135-146.
WAELBROEK C., LABEYRIE L., MICHEL E., DUPLESSY J.C.,
MCMANUS J.F., LAMBECK K., BALBON E.& LABRACHERIE M.
(2002) - Sea-level and deep water temperature changes
derived from benthic foraminifera isotopic records. Quat. Sc.
Rev. 21, 295-305.
47
SESSIONE 2

SESSIONE 2
Sea level changes in the Gulf of Orosei based on continental and
marine cave deposits
Key words: Cave sediments, OSL, sea level changes,
speleothems, U/Th dating.
INTRODUCTION
The Gulf of Orosei is located in central-east Sardinia and is
composed of a long carbonate cliff interrupted by some beaches
where fluviokarstic canyons open out into the sea. From a
geological point of view this over 200 km 2 karst area, entirely
comprised in the territories of Urzulei, Dorgali and Baunei, is
composed of a Mesozoic carbonate sequence covering Palaeozoic
basements rocks, constituted of Variscan phyllites and granites.
The carbonate plateau dips toward the East and is locally covered
by Quaternary basalts and slope deposit. The Jurassic succession
starts with continental fluvio-lacustrine sediments followed by
dolostone and limestone beds reaching a total thickness of about
800 meters. The systems of faults and the general structure of this
coastal karst area, confined by underlying impermeable basement
rocks, oblige water, infiltrating in the western part of the massif,
to flow towards the east with submarine springs located along the
coast (Bue Marino, Cala Luna, Bel Torrente, Fico Cave,
Mudaloro (Utopia) and Goloritzé). The interaction between fresh
water, discharged from the continental area through karst springs,
and sea water, combined with the action of waves, has allowed
the development of large cave entrances along the coastline (DE
WAELE, 2004). These caves are ideal places for ancient
continental and marine deposits to be preserved. Bue Marino
cave is certainly the most important karst system along this coast.
This cave system, composed of more than 17 km of passages,
_________________________
(*) Dipartimento di Scienze Botaniche, Ecologiche e Geologiche,
Università di Sassari, pascucci@uniss.it
(**) Istituto Italiano di Speleologia, Università di Bologna,
jo.dewaele@unibo.it
(°) Departamento de Hidrogeologia y Quimica Analitica. Universidad de
Almeria, Spain, lsann@ual.es
LAURA SANNA (*) (°), JO DE WAELE (*)(*), GIANCARLO PASINI (**),
VINCENZO PASCUCCI (*) & STEFANO ANDREUCCI (*)
48
opens to the sea with several entrances, some of which are more
than 20 meters wide. It is in these entrance parts that large
deposits of marine and continental sediments can be observed.
The entrance parts also show clear evidences of past sea level still
stands (Lithophaga holes, dune deposits covered with flowstone,
marine sediments).
METHODS
Marine and continental deposits have been studied in detail in
the late 70’s (CAROBENE & PASINI, 1982) and their
sedimentological significance has been clarified rather well. The
succession of depositional events, instead, has not been clearly
understood, and hypotheses on the age of the sedimentological
cycles were only based on stratigraphical relationships.
Four different levels of flowstones can be distinguished:
referring to CAROBENE &PASINI (1982) they can be indicated as
follows: (i) AL1, the oldest constituted of 10-50 cm of reddish
calcite covered by a marine conglomerate made of limestone and
granite clasts with some basaltic and speleothems pieces. The
conglomerate is covered by (ii) AL2 flowstones, made of white
calcite, deposited before the sand fillings. These two AL1 and
AL2 layers are cut by tidal notches. The following (iii) AL3 is a
pale yellow flowstone deposited on top of the partially eroded
sands. All these speleothems are bored with Lithophaga holes.
AL4 flowstone (iv) represents the last generation of speleothems
and is composed of stalagmites and stalactites covering all older
sediments. AL4 lacks Lithophaga holes and, therefore, has never
been underwater.
Clastic sediments are represented by medium-coarse grained
bioclastic-rich sands, of a probable aeolian origin. Lithophaga
boreholes have been observed aswell. In some place these
deposits are covered by reddish sediments probably derived from
flood pulses of the underground river. Also a limestone breccia,
of probable cryogenic origin, occurs interlayered in between
sandstones.
In the winter of 2009 a sampling campaign has been
undertaken in order to date the various sedimentary levels in the
Sand and Fossil Galleries of Bue Marino cave. Three different
levels of flowstone and 4 levels of sandstones have been sampled

for U/Th and OSL dating respectively.
For U/Th separation in carbonates of speleothems we used the
isotopic dilution procedure with TRU-resin in chloridric and
fluoridric acid. The U-Th ratio was measured with an ICP
Multicollector Spectrometer at the University of Oslo.
Three samples blocks (~50 x 50 x 40 cm) and one opaque
PVC tube (D = 8 cm; L = 40 cm) of freshly exposed sandstone
deposits were collected for OSL dating purposes. The inner cores
of sandstone samples were chemically treated (by using
hydrochloric acid and hydrogen peroxide) to separate siliciclastic
grains from carbonate and any residual organic material, and then
sieved to between 180 and 250 μm. Initial checks for any residual
feldspar contamination were conducted. This proved negative so
a single aliquot regenerative (SAR) protocol was used for De
measurement. The pre-heat value of 260°C was experimentally
derived based on a pre-heat plateau test and a cut heat of 220°C
was applied to each aliquot before the test dose measurement.
Five regeneration points were measured during the SAR
procedure, including a recycling point which was used to check
the adequate sensitivity correction. All aliquots had recycling
values within 0.95 ± 0.06 and a dose recovery test shows an
average value of 1.0 ± 0.1. De distributions of all samples show a
single peak which is considered a good indicator of fully
bleached, undisturbed sediments. Dose rate calculations are based
on high-resolution gamma spectrometry to give natural
radionuclide concentrations. Corrections for cosmic ray, water
content and cementation contributions at the final dose rate were
calculated.
Given the high reproducibility of sample De values, the
resultant OSL ages are thought to be a reliable indication of the
age of sediment burial. OSL analyses were carried out at the
Nordic laboratory for Luminescence Dating (Denmark).
RESULTS
The preliminary U/Th data are in good agreement with those
estimated by CAROBENE & PASINI (1982). In particular the oldest
flowstone AL1 has given an age of 262+/-100 ka and is, despote
the large error, surely much older than MIS 5e, and probably
related to warm stage MIS9.
The flowstone AL3 has given an age of 84+/-14 ka, while the
broken stalagmite embedded in the sandstone was dated 128+/-20
ka. On the basis of these dates we can refer these periods of
flowstone formation to the high sea level phases of MIS 5a, MIS
5e, during relatively warm periods.
The sandstones, interlayered in between the flowstone levels
were carried into the system during relative sea level fall and low
stands related to colder stages. The older sandstones (BUE 2)
have given an OSL age of 73+/-5 ka. Other two samples of sands
(BUE 4 and 5) immediately and half a metre below the calcite
floor have given ages of 56+/-4 ka and 57+/-5 ka respectively.
49
Further U/Th and OSL analysis are being carried out to get a
more detailed view on the various phases of speleothem and
clastic sediment deposition.
CONCLUSIONS
The first chronological data on sediments in the Bue Marino
cave are shedding light on the evolution of this cave system in a
changing coastal environment during Late Pleistocene-Holocene.
These U/Th and OSL dates are still too scarce to be able to trace
a detailed scale of events, but more datings are under way.
REFERENCES
CAROBENE L. & PASINI G. (1982) - Contributo alla conoscenza
del Pleistocene superiore e dell'Olocene del Golfo di Orosei
(Sardegna orientale). Boll. Soc. Adr. Sci., 64, 5-35.
DE WAELE J., (2004) - Geomorphologic evolution of a coastal
karst: the Gulf of Orosei (Central-East Sardinia, Italy). Acta
Carsologica, 33, 37-54.
MURRAY A.S., MARTEN R., JOHNSTON A. & MARTIN P. (1987) -
Analysis for naturally occurring radionuclides at
environmental concentrations by gamma spectrometry. J.
Rad. Nucl. Chem., 115, 263–288.
SESSIONE 2

SESSIONE 2
for U/Th and OSL dating respectively.
For U/Th separation in carbonates of speleothems we used the
isotopic dilution procedure with TRU-resin in chloridric and
fluoridric acid. The U-Th ratio was measured with an ICP
Multicollector Spectrometer at the University of Oslo.
Three samples blocks (~50 x 50 x 40 cm) and one opaque
PVC tube (D = 8 cm; L = 40 cm) of freshly exposed sandstone
deposits were collected for OSL dating purposes. The inner cores
of sandstone samples were chemically treated (by using
hydrochloric acid and hydrogen peroxide) to separate siliciclastic
grains from carbonate and any residual organic material, and then
sieved to between 180 and 250 μm. Initial checks for any residual
feldspar contamination were conducted. This proved negative so
a single aliquot regenerative (SAR) protocol was used for De
measurement. The pre-heat value of 260°C was experimentally
derived based on a pre-heat plateau test and a cut heat of 220°C
was applied to each aliquot before the test dose measurement.
Five regeneration points were measured during the SAR
procedure, including a recycling point which was used to check
the adequate sensitivity correction. All aliquots had recycling
values within 0.95 ± 0.06 and a dose recovery test shows an
average value of 1.0 ± 0.1. De distributions of all samples show a
single peak which is considered a good indicator of fully
bleached, undisturbed sediments. Dose rate calculations are based
on high-resolution gamma spectrometry to give natural
radionuclide concentrations. Corrections for cosmic ray, water
content and cementation contributions at the final dose rate were
calculated.
Given the high reproducibility of sample De values, the
resultant OSL ages are thought to be a reliable indication of the
age of sediment burial. OSL analyses were carried out at the
Nordic laboratory for Luminescence Dating (Denmark).
RESULTS
The preliminary U/Th data are in good agreement with those
estimated by CAROBENE & PASINI (1982). In particular the oldest
flowstone AL1 has given an age of 262+/-100 ka and is, despote
the large error, surely much older than MIS 5e, and probably
related to warm stage MIS9.
The flowstone AL3 has given an age of 84+/-14 ka, while the
broken stalagmite embedded in the sandstone was dated 128+/-20
ka. On the basis of these dates we can refer these periods of
flowstone formation to the high sea level phases of MIS 5a, MIS
5e, during relatively warm periods.
The sandstones, interlayered in between the flowstone levels
were carried into the system during relative sea level fall and low
stands related to colder stages. The older sandstones (BUE 2)
have given an OSL age of 73+/-5 ka. Other two samples of sands
(BUE 4 and 5) immediately and half a metre below the calcite
floor have given ages of 56+/-4 ka and 57+/-5 ka respectively.
50
Further U/Th and OSL analysis are being carried out to get a
more detailed view on the various phases of speleothem and
clastic sediment deposition.
CONCLUSIONS
The first chronological data on sediments in the Bue Marino
cave are shedding light on the evolution of this cave system in a
changing coastal environment during Late Pleistocene-Holocene.
These U/Th and OSL dates are still too scarce to be able to trace
a detailed scale of events, but more datings are under way.
REFERENCES
CAROBENE L. & PASINI G. (1982) - Contributo alla conoscenza
del Pleistocene superiore e dell'Olocene del Golfo di Orosei
(Sardegna orientale). Boll. Soc. Adr. Sci., 64, 5-35.
DE WAELE J., (2004) - Geomorphologic evolution of a coastal
karst: the Gulf of Orosei (Central-East Sardinia, Italy). Acta
Carsologica, 33, 37-54.
MURRAY A.S., MARTEN R., JOHNSTON A. & MARTIN P. (1987) -
Analysis for naturally occurring radionuclides at
environmental concentrations by gamma spectrometry. J.
Rad. Nucl. Chem., 115, 263–288.

Fossil dunes and desert flora along the southern margin of Chott el
Jerid (Southern Tunisia)
Key words: Chott el Jerid, fossil dunes, fossil flora, rhizoliths,
Tunisia.
INTRODUCTION
Chott el Jerid is a large, salt-covered, depression in southern
Tunisia, located some 100 km west of Gabes and extended along
an East-West direction up to 20 km from the border with Algeria.
The dried lake is bordered to the North by the Atlas Mountains,
and to the South and West by the margin of the Grand Erg
Oriental. After major flooding events the flat expansion of Chott
el Jerid becomes an ephemeral lake, but usually it is covered by a
crust of salt and gypsum, and the ground below is soaked by a
salt brine. Dissolution of Cretaceous to Tertiary evaporite
sediments from the mountains surrounding the chott is the source
for the salt deposited in Chott el Jerid (ROBERTS &MITCHELL,
1987).
The area described in this paper is located just West of Douz,
on the southern margin of Chott el Jerid, where low-relief
“promontories” and “islets” mark the transition between the chott
saltpan and the rocky land.
These small elevations are part of a fossilized dunes field
extended over a huge area South of the chott. Spectacular
outcrops of the fossilized dunes occur along the margin of the
chott, where they form isolated ridges with eroded flanks
exposing the internal eolian cross-lamination. Further South the
fossilized dunes are laterally connected, and largely masked by a
veneer of modern dunes.
FOSSILIZED SAND DUNES
Fossilized sand dunes at the southern margin of Chott el Jerid
form 1 to 2 km-long ridges trending along 80° Azimuth direction.
Height of the ridges is about 5 m, and distance between parallel
crests is about 120-150 m. Size and shape of the fossilized
transverse dunes markedly contrasts with the small modern
barchans migrating above them, and the relative orientation
between the two dunes systems indicates a 90° rotation in the
_________________________
(*) Baker Hughes Inteq, Paolo.Sudiro@bakerhughes.com
PAOLO SUDIRO (*)
51
direction of dominant winds.
Interdunes areas are not preserved at the chott margin, where
the fossil dunes form elongated mesas with steep eroded flanks,
and depressions between the ridges are filled by the same spongy
evaporitic deposit forming the bottom of the chott.
Evidence exists of two humid episodes at about 90 and 150 ka
when the southern Tunisian chotts became permanent lakes
(CAUSSE et alii, 1989), while it is highly controversial a direct
connection to the Mediterranean at 35 ka (RICHARDS &VITA-
FINZI, 1982). High water level in Chott el Jerid during the humid
periods could explain the erosion of the fossil dunes at the chott
margin, and the missing of interdunes deposits, because the area
was then a lake shore exposed to waves erosion. Small bivalve
shells (diameter of 3-4 mm) frequently occur in the loose sand of
the toes of the eroded fossilized dunes at the chott inlets. These
shells were not probably airborne from the Mediterranean coast,
and are not included in the sand making the ancient or actual
dunes. Therefore the bivalves were living in the flooded chott,
and were left by waves and currents along its shore, indicating
that these depressed areas were once submerged.
Fig. 1 – Cross-section of a fossilized sand dune along a road cut on the
southern margin of Chott el Jerid. Height of the small cliff is about 2 m.
Several root borings dot the face of the cliff. The picture is oriented with
North to the right,and South to the left.
Quartz is the dominant component of the active dunes around
Chott el Jerid, but gypsum becomes more frequent towards the
East, indicating a local source for the eolian sedimentation
(BARCZUK & DLUZEWSKI, 2005). Fossil dunes, made, as the
SESSIONE 2

SESSIONE 2
modern ones, of very fine to fine sand that could preserve even
the finest details of the buried vegetation, have probably a similar
composition; however, the widespread occurrence of solutionredeposition
features in the fossil dunes (caliche hardpans,
solution pipes, mineralized vegetation fossils) indicates a higher
percentage of soluble minerals compared to the modern dunes.
The top surface of the fossilized dunes consists of a 20 to 50
cm-thick caliche hardpan, made of concretions, cauliflower-like
efflorescences, large lithified mud cracks extending downward in
spiky crystalline overgrowths, and mounds of fossil vegetation.
At places, wedge-like solution pipes cross the dunes, usually
running along sub-vertical fractures.
Fig. 2 – Top of a fossilized dune along the southern margin of Chott el Jerid.
The little mounds dotting the dune summit (maximum height 30 cm, diameter
about 1 m) are fossilized bushes and consist of roots, trunks, lower branches
and broken branches, all replaced by carbonate encrustations. The view is
from South looking North, i.e. from the edge of the chott towards the interior
of the salt pan.
THE FOSSILIZED DESERT FLORA
Sub-circular mounds (diameter 1 m, height 30 cm), made of
stumps, lower branches, broken branches, and roots of fossil
bushes, cover the undulated top surface of the fossilized dunes.
Trunks and larger branches have been fossilized by concentric
crystal rims that could be a replica of the annual rims of the living
plants. Roots of various sizes are also exposed along the slopes of
the eroded dunes: from long root borings crossing the full section
of the dunes, to root casts and, at places, large areas covered by
thick nets of millimetre-size rhizoliths.
Modern dead vegetation is degraded in the desert by intense
de-hydratation and seasoning, and the full range of degradation
features displayed by the modern vegetation is also preserved by
the fossil counterparts, like the mineralized fragments of
carbonized branches with scorched bark on one side and a windpolished
surface on the other one.
52
The density of the fossilized vegetation is high compared to
the one of the actual mobile dunes, where sparse bushes usually
grow in the interdunes depressions and not on top of the dunes.
However, if the ground is stabilized, also the living vegetation is
dense, especially in the depressed areas closer to the ground
water, and the morphology of the fossil vegetation indicates that
the type of bushes preserved in the fossilized dunes is similar to
the one living today in the same area. Therefore, although the
climate was probably more humid when the dunes were stabilized
and fossilized, the area was still too arid for the growth of larger
trees. The dunes were also probably stabilized before they were
colonized by the vegetation.
Fig. Fig. 3 – Close-up 3 – Close-up view view of a of cluster a cluster of broken of broken branches branches of a of fossilized a fossilized desert desert
bush bush on the on edge the edge of a fossilized of a fossilized sand sand dune.
dune.
REFERENCES
CAUSSE C., COQUE R., FONTES J-CH., GASSE F., GIBERT E., BEN
OUEZDOU H. & ZOUARI K., (1989) - Two high levels of
continental waters in the southem Tunisian chotts at about 90
and 150 ka. Geology, 17 , 922-92.
BARCZUK A. & DLUZEWSKI M. (2005) Importance of the
petrological approach in studies of the desertification in
Northern Sahara. Mineral. Soc. of Poland – Spec. Papers, 26,
137-140.
RICHARDS G. W. & VITA-FINZI C. (1982) - Marine deposits
35,000-25,000 years old in the Chott el Jerid, southern
Tunisia. Nature, 295/5844, 54-55.
ROBERTS, C. R., & MITCHELL, C. W. (1987) - Spring mounds in
southern Tunisia. In: Frostick, L. & Reid, I. (Eds), Desert
Sediments: Ancient and Modern, Geol. Soc. of London, Spec.
Pub. 35, 321-334.

Key words: Aegean Sea, coastal tectonics, geomorphological
markers, Lesvos Island, palaeo-shoreline.
INTRODUCTION
Detailed mapping of raised shorelines has been often used as
tool to quantify coastal vertical displacements (FERRANTI et alii,
2007). Along the Mediterranean coastlines, progress in
understanding the co-seismic motions of the region has been
achieved by accurate analyses of geomorphological records of
Pleistocene and Holocene displacements preserved in uplifted
palaeo-shorelines (PIRAZZOLI, 2004; FERRANTI et alii, 2007).
Many studies were carried in the Aegean Sea (PIRAZZOLI et alii,
2005; STIROS et alii, 2009), a rapidly extending areas of
continental crust characterized by the southern Aegean moving at
a rate of about 35 mm/yr relatively to Eurasia. The northern part
of the Aegean area is strongly influenced by the North Anatolian
Trough (NAT) fault system characterized by a principal dextral
strike-slip displacement and, in the adjacent area, by mainly
synthetic and antithetic shear extensional structures and rarely
constructional structures (SOULAKELLIS et alii, 2006). This study
was carried out in Lesvos Island (NE Aegean Sea) the third
largest Greek island covering an area of about and 1,630 km2 and
bordered by about 370 kilometers of coastline. It lies south of the
North Anatolic Fault and presents a fault pattern reflecting three
different neotectonic phases, determined for the wider North
Aegean area. For our study, great importance is assumed by the
last phase, started in the Pleistocene, that created E-W normal
faults and re-activated pre-existing structures. The geology of the
Island presents, in the eastern part, the basement composed of
Alpidic and pre-Alpidic rocks, instead the western part is covered
by post-Alpine formations, mainly represented by Miocene
volcanic rocks (SOULAKELLIS et alii, 2006).
A detailed mapping of paleo-shorelines of the island was
carried out, including both erosional and depositional sea level
markers. The field mapping were not focused only to the on land
part of the coast areas but several underwater transects were
_________________________
Spatial distribution of the paleo-shorelines in Lesvos Island.
Evidence of differential coastal uplift in the area?
MATTEO VACCHI (*), ALESSIO ROVERE (*), NICKOLAS ZOUROS (**) & MARCO FIRPO (*)
(*) Dip.Te.Ris., University of Genova (Italy), matteo.vacchi@unige.it
(**) Department of Geography, University of Aegean (Greece)
53
carried out mapping the submerged geomorphology until about –
15 m.
RESULTS AND DISCUSSION
The sea levels markers found in the study area mainly
consisted in beachrock outcrops, shore platforms and tidal
notches (Fig 2a). Several beachrock resulted to be composed by
multiple generations. Their altitude varied between – 5 to + 2 m
respect the present sea level. Debates about the use of beachrocks
as sea level indicators are present in literature (BERNIER &
DALONGEVILLE, 1999; KELLETTAT, 2006; VOUSDOUKAS et alii,
2007). In this study we considered beachrocks as markers of past
sea level mainly because of their altimetric correlation with other
erosional markers. As an example a 5 km long raised shore
platform was mapped in the area of Agios Fokas-Vrisa its internal
margin being at + 1,2 ± 0,3 m asl (fig.1). In the same area, a
beackrock deposit has been found at nearly the same altitude.
Fig. 1-
The uplifted shore platform of Agios Fokas (internal margin at + 1.2
± 0.3 m asl).
Along the limestone rocky coastlines of the island series of
tidal notches were observed and mapped. In particular the south
eastern part showed three generations of notches with the highest
located at about 11 m above the sea level. In the northern part
only one generation, at present sea level, was observed. The
preliminary analysis of the mapped geomorphological indicators,
SESSIONE 2

SESSIONE 2
Fig. 2 – Spatial distribution (a) and relative elevation on the present sea level (b) of the geomorphological markers in Lesvos island.
not yet supported by chronological dating, evidenced strong
differences on the altimetric distribution of the paleo-shorelines
along the Lesvos coastlines (fig.2b).
These preliminary results provide suggestive evidence that the
south eastern part of the Island is subjected to important uplift
phenomena as highlighted by the several displaced sea level
markers mapped along this coastal area. On the contrary, the
central, the eastern and the north-western part of the Island,
despite the high tectonic activity characterizing the region did not
present any evidences of raised shorelines. This spatial
distribution of the paleo-shorelines could become crucial if
related with the active tectonics of the area. In fact, Lesvos island
is located in a complex area subjected to the parallel activity of
both strike slip and normal faults resulting in a transestensive
tectonics (ROUMELIOTI et alii, 2010). Radiometric dating is being
carried out on beachrock cements and on other deposits found
upon raised shore platforms, and will likely allow to quantify
rates of uplift, providing new data about the neotectonic behavior
of this part of the Aegean Sea.
REFERENCES
BERNIER P. & DALONGEVILLE R. (1996). Mediterranean coastal
changes in beach-rock cementation. Z. Geomorph. N.F.,
Supp. 102, 185-198.
FERRANTI L., MONACO C., ANTONIOLI F., MASCHIO L., KERSHAW
S. & VERRUBBI V. (2007). The contribution of regional uplift
and coseismic slip to the verticalcrustal motion in the
Messina Straits, southern Italy: Evidence from raised Late
54
Holocene shorelines. J. Geoph. Res., 112, B06401,
doi:10.1029/2006JB004473
KELLETTAT D. (2006). Beachrock as Sea-Level Indicator?
Remarks from a Geomorphological Point of View. J. Coast,
Res. 22, 6: 1558-1564.
PIRAZZOLI P.A. (2005). A review of possible eustatic,isostatic
and tectonic contributions in eight late-Holocene relative
sea-level histories from the Mediterranean area. Quat. Sci.
Rev. 24 1989–2001
PIRAZZOLI P.A., STIROS S.C., FONTUGNE M. & ARNOLD M.
(2004). Holocene and Quaternary uplift in the central part of
the southern coast of the Corinth Gulf (Greece). Mar. Geol.
212, 35-44
SOULAKELLIS N.A., NOVAK I.D., ZOUROS N., LOWMAN P. &
YATES J. (2006). Fusing Landsat-5/TM Imagery and Shaded
Relief Maps in Tectonic and Geomorphic Mapping: Lesvos
Island, Greece. Phot. Eng & Rem. Sens. 72, 6: 693-700.
STIROS S.C., PIRAZZOLI P.A. & FONTUGNE M. (2009). New
evidence of Holocene coastal uplift in the Strophades Islets
(W Hellenic Arc, Greece). Mar. Geol., 267, 207–211.
VOUSDOUKAS M.I., VELEGRAKIS A.F. & PLOMARITIS T.A. (2007).
Beachrock occurrence, characteristics, formation
mechanisms and impacts. Earth Sc. Rev., 85, 23-46.

SESSIONE 3
Modellazione geologica tridimensionale: ricostruzione
di strutture crostali e sub-crostali e loro applicazioni
CONVENERS
Chiara D'Ambrogi (Servizio Geologico d'Italia Roma)
Davide Scrocca (CNR Roma)
Giovanni Toscani (Università di Pavia)
55
SESSIONE 3

SESSIONE 3
Key words: Finite-element models, inherited fault systems, Italy,
seismogenic faults.
In the world there is an ongoing effort for the realization of
seismic hazard maps in which seismogenic fault systems play a
primary role. For regions poorly known from a seismotectonic
point of view, however, these maps have to include those fault
systems, derived from the literature, that are compatible with the
current stress field.
On the other hand, there are cases where severe earthquakes
occur on seismogenic faults that are mis-oriented with respect to
the active stress field, e.g.: the San Andreas fault, in California
(CHÉRY et alii, 2004); the Alpine fault, in New Zealand (WARR
&COX, 2001; LIU &BIRD, 2002); the Castle Mountain fault, in
Alaska (BUNDS, 2001); and the Molise-Gondola shear zone, in
Italy (hereinafter MGsz, DI BUCCI et alii, 2006). This occurrence
poses a problem of uncorrect hazard estimation (e.g., escape
tectonics in Los Angeles; WALLS et alii, 1998).
The MGsz appears as a ~15 km-wide and ~180 km-long
corridor, running W-E at the latitude 41.6°N from the Adriatic
foreland off-shore to the core of the Apennines fold-and-thrust
belt. The MGsz is an inherited structure: the oldest evidence for
its activity dates back to the Jurassic. Its Meso-Cenozoic
evolution records a long history of subsequent tectonic phases
(e.g., Mesozoic extension or Cenozoic shortening) during which
the MGsz slipped both as right- and as left-lateral. The algebraic
sum of strike-slip displacements estimated for the off-shore part
of the MGsz leads to ~15 km of right-lateral offset (DE’
DOMINICIS &MAZZOLDI, 1987).
The MGsz is presently active and seismogenic, as
demonstrated by the Mw 6.8, 1627 Gargano earthquake and by
the Mw 5.8-5.7, 2002 Molise earthquakes (CPTI WORKING
GROUP, 2004). The stress drop associated with these earthquakes
_________________________
Low-friction shear zones: the Molise-Gondola case study
PAMELA ANGELONI (*), SALVATORE BARBA (**), MICHELE CARAFA (**) & DANIELA DI BUCCI (*)
(*) Dipartimento della Protezione Civile,
pamela.angeloni@protezionecivile.it; daniela.dibucci@protezionecivile.it
(**) Istituto Nazionale di Geofisica e Vulcanologia, barba@ingv.it;
carafa@ingv.it
This research has benefited from funding provided by the Italian Presidenza
del Consiglio dei Ministri – Dipartimento della Protezione Civile (DPC).
Scientific papers funded by DPC do not represent its official opinion and
policies.
56
is low (CALDERONI et alii, 2010). The horizontal slip rate based
on VHR seismic profiles on the off-shore part of the MGsz,
referred to the past 240 ka, ranges between 0.08-0.78 mm/a. (DI
BUCCI et alii, 2009). For the exposed part of the same shear zone,
TONDI et alii (2005) estimated a Late Pleistocene and Holocene
slip rate of 0.7-0.8 mm/a. Finally, from a GPS network straddling
the entire shear zone, FERRANTI et alii (2008) obtained a slip rate
of 2 mm/a.
The E-W strike of the shear zone, however, is not perfectly
oriented with respect to the regional stress field, that shows a
NW-SE sriking σhMax (MONTONE et alii, 2004).
The present-day MGsz activity suggests us that it behaves as a
weak shear zone, i.e. that the friction coefficient μ is sufficiently
low, according to the Mohr-Coulomb criterion (BEELER et alii,
2000).
This work is aimed at quantifying the μ_eff value for the
Fig. 1 – Study area and grid used in our finite-element models (major fault
systems simplified and redrawn from DISS WORKING GROUP, 2009).
MGsz and verifying that the seismic moment is balanced. To do
this, we implemented a set of finite-element numerical models
(Fig. 1). These three-dimensional models are referred to the
entire lithosphere and encompass several major shear zones. The
computation has been carried out with SHELLS software (BIRD

&KONG, 1994), and verified through a comparison with GPS
data for the horizontal velocities (DEVOTI et alii, 2007), focal
mechanisms for the tectonic regime (DEL GAUDIO et alii, 2004)
and break-out data for the σhMax orientation (MONTONE et alii,
2004).
We chose to use a finite-element numerical modeling because
direct observation on the fault gauge is possible only for a limited
part of the shear zone, which is mainly buried or submerged.
Moreover, analyses based on the instrumental seismicity are not
possible, due to the limited number of recorded data.
Results from our modeling show that: (i) the MGsz is
significantly weaker than the average of the considered Italian
faults; (ii) the μ_eff value for the MGsz is = 0.1; and (iii) with the
latter value the moment rate is balanced.
REFERENCES
BEELER N.M., SIMPSON R.W., HICKMAN S.H. & LOCKNER D.A.
(2000) - Pore fluid pressure, apparent friction, and Coulomb
failure. J. Geophys. Res., 105 (B11), 25,533-25,542.
BIRD P. & KONG X. (1994) - Computer simulations of California
tectonics confirm very low strength of major faults. Geol.
Soc. Am. Bull., 106 (2), 159-174.
BUNDS M.P. (2001). - Fault strength and transpressional
tectonics along the Castle Mountain strike-slip fault, southern
Alaska. Geol. Soc. Am. Bull., 113, 908-919.
CALDERONI G., ROVELLI A., MILANA G. & VALENSISE G. (2010) -
Do Strike-Slip Faults of Molise, Central–Southern Italy,
Really Release a High Stress?. Bull. Seismol. Soc. Am., 100
(1), 307-324; doi: 10.1785/0120090046
CHÉRY J., ZOBACK M.D. & HICKMAN S. (2004) - A mechanical
model of the San Andreas fault and SAFOD Pilot Hole stress
measurements. Geophys. Res. Lett., 31 (L15S13),
doi:10.1029/2004GL019521
CPTI WORKING GROUP (2004) - Catalogo Parametrico dei
Terremoti Italiani. Version 2004 (CPTI04), INGV, Bologna.
http://emidius.mi.ingv.it/CPTI04/
DE’ DOMINICIS A. & MAZZOLDI G. (1987) - Interpretazione
geologico-strutturale del margine orientale della Piattaforma
apula. Mem. Soc. Geol. It., 38, 163-176.
DEL GAUDIO V., PIERRI P., FREPOLI A., CALCAGNILE G., VENISTI
N. & CIMINI G.B. (2007) - A critical revision of the seismicity
of Northern Apulia (Adriatic microplate — Southern Italy)
and implications for the identification of seismogenic
structures. Tectonophysics, 436, 9-35.
57
DEVOTI R., RIGUZZI F., CUFFARO M. & DOGLIONI C. (2008) - New
GPS constraints on the kinematics of the Apennines
subduction. Earth and Planetary Science Letters, 273, 163-
174 doi: 10.1016/j.epsl.2008.06.031
DI BUCCI D., RAVAGLIA A., SENO S., TOSCANI G., FRACASSI U. &
VALENSISE G. (2006) - Seismotectonics of the southern
Appenines and Adriatic foreland: Insights on active regional
E-W shear zones from anologue modelling. Tectonics 25,
TC4015, doi: 10.1029/2005TC001898
DI BUCCI D., RIDENTE D., FRACASSI U., TRINCARDI F. &
VALENSISE G. (2009) - Marine palaeoseismology from very
high resolution seismic imaging the Gondola Fault Zone
(Adriatic foreland). Terra Nova, 21, 393-400.
DISS WORKING GROUP (2009) - Database of Individual
Seismogenic Sources (DISS), Version 3.1.0: A compilation of
potential sources for earthquakes larger than M 5.5 in Italy
and surrounding areas. http://diss.rm.ingv.it/diss/, © INGV
2009.
FERRANTI L., OLDOW J.S., D’ARGENIO B., CATALANO R., LEWIS
D., MARSELLA E., AVELLONE G., MASCHIO L., PAPPONE G.,
PEPE F. & SULLI A. (2008) - Active deformation in Southern
Italy, Sicily and southern Sardinia from GPS velocities of the
Peri-Tyrrhenian Geodetic Array (PTGA). Boll. Soc. Geol. It.
(Ital. J. Geosci.), 127, 1-18.
LIU Z. & BIRD P. (2002) - Finite element modeling of
neotectonics in New Zealand. J. Geophys. Res., 107 (B12),
2328, doi:10.1029/2001JB001075
MONTONE P., MARIUCCI M.T., PONDRELLI S. & AMATO A. (2004)
- An improved stress map for Italy and surronding regions
(central Mediterranean). J. Geophys. Res., 109 (B10410),
doi: 10.1029/2003JB002703
TONDI E., PICCARDI L., CACON S., KONTNY B. & CELLO G.
(2005) - Strumental and time contraints for dextral shear
along the seismogenic Mattinata Fault (Gargano, Southern
Italy). J. Geodyn., 40, 134-152.
WALLS C., ROCKWELL T., MUELLER K., BOCK Y., WILLIAMS S.,
PFANNER J., DOLAN J. & FANG P. (1998) - Escape tectonics in
the Los Angeles metropolitan region and implications for
seismic risk. Nature, 394, 356-360.
WARR L.N. & COX S. (2001) - Clay mineral transformations and
weakening mechanisms along the Alpine Fault, New Zealand.
Geol. Soc. London, Special Publications, 186, 85-101.
SESSIONE 3

SESSIONE 3
Three dimensional modelling in mineral exploration: a case study
from the El Creston porphyry-moly deposit (Sonora, Mexico)
Key words: 3D modeling and visualization, Mexico, porphyrymoly
deposits, Sonorian basin-and-range, subsurface
exploration.
The surface and subsurface exploration in mining involves
at least geological mapping and intense drilling, along with
geochemical assays, remote-sensing, geophysics and
geotechnics. The data collected are handled in specific software
in order to reconstruct consistent three-dimensional (3D)
models that include the ore, lithological and alteration shells,
and all the relevant structures. Especially in the case of deep
erosion and/or tectonic activity, it is possible to observe
different portion of the magmatic-hydrothermal system, from
the deep roots to the periphery. The use of the modelling and
visualization techniques in 3D and the 3D restoration is
effective in mining exploration and provides remarkable helps
for correctly understand and correlate large datasets, and
propose coherent interpretations.
The El Creston is a porphyry-moly deposit with proven and
probable mineral reserve of 146,705,000 tonnes grading
0.077% Mo, plus copper, minor zinc and silver as main byproducts.
The project is now moving to full feasibility, along
with the follow-up of the exploration program, aimed to extend
the proven reserve. The deposit is related with the intrusion of a
quartz-monzonitic to monzogranitic porphyry stock (55Ma),
intruding a metamorphosed Proterozoic sequence. The gross of
the deposit is hosted in the “Creston” meta-granite (1.73Ga)
and in a hydrothermal breccia (54Ma); the feeder of the deposit
is identified as a quartz-eyes bearing porphyry granite,
representing the late stages of the quartz-monzonitic intrusion.
The mineralized system underwent a complex tectonic history,
including extensional faulting and uplift from Miocene to
Quaternary. The most relevant structures are low-angle normal
faults (dipping N35/30°) with horizontal displacement of 450 to
250 mts; late high-angle faults (E-W and NW-SE trending)
weakly dissect all the previous structures.
_________________________
(*) Dipartimento di Scienze della Terra, Universitá di Siena.
aque@unisi.it.
RICCARDO AQUÉ (*)
58
This is a good example for demonstrate the utility if the
modelling techniques and structural geology in the exploration
phases, from fieldwork follow-up, to drill hole plan and target
prediction.
The existing surface and subsurface data allow an accurate
reconstruction of the subsurface geology; the existing 145 core
logs and the geological survey data have been used for
extensive geological and grade modelling. The initial (current)
model has been restored, in order to better imagine the shape of
the original (pre-deformation) mineralized system, identify
additional targets and estimate the erosion play.
This contribution aims to stress the importance of 3D
modelling in many fields of the geosciences.

Key words: 3D geological modelling, geometrical coherence,
kinemetics analysis.
The use of three-dimensional (3D) modelling and
visualization techniques is an effective tool that helps in the
understanding of the geometry and evolution of the geological
structures. These techniques are routinely used in the oil & gas
and in the mine industries, where significant investments are
accompanied by careful planning and monitoring through
digital modelling. With the increasing need of understand threedimensional
coherence of large and multidisciplinary datasets,
the 3D modelling practice has been extended to field-based
investigations and serves as a predictive tool in areas with poor
sub-surface data. In the latter case, the study of analogue
outcrops is used to predict the 3D behaviour of subsurface
structures. The ability of modelling structures with strong
geometrical coherency between surface and subsurface data in
a geologically viable way, and in the true 3D space, is enhanced
by the 3D kinematical balancing exercise (DEE et alii, 2005).
This is normally achieved by using specific algorithms, (EGAN
et alii., 1997; BUDDIN et alii., 1997; MORETTI, 2008) currently
available in some software. We use the software MOVE®
(MVE inc) to handle cross-sections, map and well data, and
create viable 3D models.
Different modelling techniques are used for reconstruct the
current (deformed) architectural geometry in tectonically
complex areas. We tailored workflows for geological modelling
that include the use of georeferred field data, interpreted
geological maps and cross-sections; when available, subsurface
data like well logs and seismic images are used for better
constrain the model. Surfaces representing lithological
boundary and faults have been obtained in different ways,
either by interpolation of the starting data (field measurements,
best constrained map traces of the structures), or starting from
reference surfaces (used as a proxy for subsequent morphing by
using structural thickness and attitude constraints. Subsequent
balancing methods in both cross-section and 3D are used for
_________________________
3D modeling and cross-section restoration as tools for imaging
geological structures
(*) Dipartimento di Scienze della Terra, Universitá di Siena,
tavarnelli@unisi.it
(°) Dipartimento di Scienze Geologiche, Universitá della Basilicata,
Potenza
RICCARDO AQUÉ (*), ROCCO NOVELLINO (*), FRANCESCO BUCCI (*),
GIACOMO PROSSER (°) & ENRICO TAVARNELLI (*)
59
constrain the geological model with a trial-and error procedure.
Our experience demonstrates the effectiveness of the 3D
modelling techniques in different tectonic settings. Here we are
presenting map-scale examples of models obtained in areas of
the inner and the central zones of the Apennines, respectively in
areas where the post-collisional extension is prevalent, and
areas where the effects of the contraction does.
1) The first example is a 3D model of the NE margin of the
Larderello-Travale geothermal field (southern Tuscany),
showing the geometry of Pliocene-Quaternary normal faults
that bound the western edge of the Pomarance-Anqua basin
(upper Miocene to Pleistocene; BOSSIO et alii, 1993). These
faults are reflecting a regional trend characterizing the
Larderello geothermal field, cross-cut all the local tectonostratigraphic
pile, down to the current brittle-ductile transition,
and are believed to play a strong control on the circulation of
the geothermal fluids (BELLANI et alii, 2004).
The modelled faults have been imaged using the
stratigraphic cut-offs resulting from cross-sections; the
geometry of the faulted units is balanced consistently with the
geometry of the modelled faults and assuming the tectonic
transport perpendicular to the main faults.
2) The second example model is a transect of the Umbria-
Marche Apennines, where map-scale structures belonging to a
linked fold-and-thrust belt (TAVARNELLI, 1996) have been
modelled in a balanced 3D model, obtained from 5 balanced
cross-sections. The sequential back stripping of the
compressive deformation (i.e., restoring sequentially the
stratigraphic tops to the depositional position) allowed
reconstructing the pre-compressive geometry of the precursor
sedimentary basins. The position of early extensional ramps is
closely related to the nucleation of thrust fault, as commonly
observed in cases of positive structural inversion (GILLCRIST et
alii, 1997). The forward modelling of the structures allowed a
quasi-quantitative estimation of the finite strain caused by
faulting and folding.
3) The third example is the model of a faulted anticline in
the Val d’Agri basin (southern Apennines), where normal faults
nucleated at the steep flanks of an upright fold (the Monte
Corno anticline), affecting the tectonic units pile, on which the
Lagonegro I (platform carbonates to shales, Carnian to
Cretaceous in age) is the deepest tectonic unit outcropping in
the study area. The projection of field data along local
structural axis allowed reconstructing the shape of the fold, and
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SESSIONE 3
constraining the interpretation of its faulted portions. Starting
from a reference surface (the top of the Calcari con selce fm.),
we reconstructed the local stratigraphic sequence by using
structural thickness constraints. The post-compressive normal
faults pattern is derived from the inferred map-traces and
imaged in cross-section.
We stress the need of 3D geometrical coherence between
geological maps and related cross-sections, and the utility of
the 3D modelling and visualization techniques in achieve best
results and geometrically consistent linked structures.
REFERENCES
BELLANI S., BROGI A., LAZZAROTTO A., LIOTTA D. & RANALLI
G. (2004) - Heat flow, deep temperatures and extensional
structures in the Larderello Geothermal Field (Italy):
constraints on geothermal fluid flow. J. Volcanol. Geoth.
Res., 132, 15-29.
BOSSIO A., COSTANTINI A., LAZZAROTTO A., LIOTTA D.,
MAZZANTI R., MAZZEI R., SALVATORINI G. & SANDRELLI F.
(1993) - Rassegna delle conoscenze sulla stratigrafia del
neoautoctono toscano. Mem. Soc. Geol. It., 49, 17-98.
BUDDIN T.S., KANE S.L., WILLIAMS G.D. & EGAN S.S. (1997) -
A sensitivity analysis of 3-dimensional restoration
techniques using vertical and inclined shear constructions.
Tectonophysics, 269, 33–50.
DEE S., FREEMAN B., YIELDING G., ROBERTS A., BRETAN, P.
(2005) - Best practice in structural geological analysis.
First Break, 23, 49-54.
EGAN S.S., KANE S., BUDDIN T.S., WILLIAMS G.D. &
HODGETTS D. (1999) - Computer modelling and
visualisation of the structural deformation caused by
movement along geological faults. Comput. Geosci., 25 (3),
283-297.
GILLCRIST, R., COWARD, M.&MUJER, J. (1987) – Structural
inversion and its controls: examples from the Alpine
foreland and the French alps. Geodin. Acta, 1, 5-34.
MORETTI I. (2008) - Working in complex areas: New
restoration workflow based on quality control, 2D and 3D
restorations. Mar. Petrol. Geol., 25 (3), 205-218.
TAVARNELLI, E. (1996) – Thethyan heritage in the
development of the Neogene Umbria-Marche fold-andthrust
belt, Italy: a 3D approach. Terra Nova, 8, 470-478.
60

Sedimentological and structural analysis of a “tight reservoir” in the
Hassi Terfa field (North Algerian Sahara)
Key words: Burial, correlation, diagenesis, fracture, Hassi Terfa,
reservoir, saharian-platform.
The first sedimentary deposits overlying the saharian platform
noted for its flatness are of paleozoic age.
The burial associated with diagenesis phenomena compacted
several geological levels, especially in the Ordovician. The
Hassi-Terfa field, which is one of the satellite structures
surrounding the giant Hassi Messaoud field, is mostly
characteristic. It is being located in the triassic petroleum
province.
The ordovician system contains a compact formation
called “the Hamra quarzites”. It is also a hydrocarbon reservoir
but with rather bad petrophysical properties. Statistical analysis
of porosity and permeability factors shows a typical bimodal
distribution. This is rightly due to being fractures. The mapping
of isopermeability factor of this reservoir indicates a distribution
largely depending on the fractured zones caused by different
steps of deformation along the geological time.
A significant correlation between the isopermeability and
isofracturation maps is clearly shown .This reservoir which
produces hydrocarbons by natural fracturation can be ranged as a
“fracturated reservoir”. Therefore, it is a need to look after areas
highly fracturated for all new wells projected to drilling .Thus
substantial increased hydrocarbons are extracted.
_________________________
(*) Fields Départment, Hydrocarbon & Chemistry Faculty, University of
Boumerdes – Algeria, assesamar@yahoo.fr, k_loumi@yahoo.fr
AMAR ASSESS (*) & KHALED LOUMI (*)
61
SESSIONE 3

SESSIONE 3
3D reconstruction of the structural setting, reservoir modeling and
simulation of an off-shore area from available seismic reflection data
interpretation: evidences and constraints in the research of potential
structures for geological storage of CO2
MAURO BUTTINELLI (*), GIUSEPPE VICO (**), ELIO BIANCHI (**), DAVIDE SCROCCA (°),
LORENZO PETRACCHINI (°) & FEDORA QUATTROCCHI (*)
Key words: CO2 storage, reservoir , simulation, tridimensional.
A re-interpretation of available seismic reflection surveys
dataset in an off-shore study area has been performed to focus on
its structural setting and to identify potential geological structures
for CO2 injection.
The stratigraphic succession of this area is constrained by a
deep well, and is characterized by a sedimentary succession of
terrigenous marine units resting above a marly-sandy-calcarenitic
succession, which is tectonically superimposed above calcareous
units and evaporites.
Seismic reflection data interpretation show that this area was
affected by several deformational stages, which caused firstly the
formation of compressional (thrusts, back-thrusts and fold
structures) and then extensional features (horst, graben and halfgraben
structures, bordered by normal faults).
This tectonic stages isolated volumes or rocks that could be
considered as structural traps potentially suitable for geological
storage of CO2. Both compressional (anticlines and thrust-related
anticlines) and positive extensional structures (horst) could be
targets of this research.
The marly-sandy-calcarenitic succession (and the terrigenous
marine units above it) can be considered as cap-rock, whereas
calcareous fractured formations (hosting a regional deep aquifer)
can be considered as reservoirs.
The original raster seismic reflection data have been
transformed into SEG-Y vectorial data format. The SEG-Y files
were loaded in a digital database and a tri-dimensional
reconstruction of the structural setting of the area has been
accomplished via dedicated softwares. The interpretation was
carried out through manual picking of the relevant seismic
horizons and discontinuities. Principal surfaces of top cap-rock
and top reservoir units have been computed taking into account
normal faults and thrusts surfaces geometry, also reconstructed.
The reconstruction of top reservoir surface have been checked via
_________________________
(*) Istituto Nazionale di Geofisica e Vulcanologia (INGV), sezione Roma1,
UF geochimica dei fludi, stoccaggio geologico e geotermia
mauro.buttinelli@ingv.it
(**) Independent Energy Solutions S.r.l.
(°) CNR-IGAG c/o Università degli Studi di Roma “La Sapienza”
62
cross correlation between units signals on seismic lines (in ms
two way time) and the analogue measured thickness in the well
stratigraphy (in meters).
This workflow allowed to identify and map a positive
reservoir trap structure completely surrounded by cap-rock
lithologies.
A depth conversion from time (twt ms) to depth (meters
below sea level) of all the computed surfaces have been then
performed by construction of isopachs maps for each seismic
units, even referring to the geological literature on rocks seismic
velocities.
This methodology led to the reconstruction of a reliable tridimensional
geometry of the reservoir potentially suitable for
CO2 injection. Moreover, this process also allowed the
calculation of the trap volume. After this process, a modelling
and simulation of the CO2 behaviour in the reservoir after
injection have been performed, considering the fluid flux through
the pore, volume of the reservoir, the injected gas composition
and the petrophysical properties of the reservoir rocks.

3D model reconstruction of mineralizations in Alpine context.
Examples of geomatics approach on the talc mineralization mine in
Germanasca Valley and the Balangero asbestos mine (Western Alps)
PAOLA CADOPPI (*), GIOVANNI CAMANNI (*), ANTONIO DAMIANO (**), ERMES FUSETTI (°), FRANCO MONTICELLI (°°),
LUIGI PEROTTI (*) & GIANLUIGI PERRONE (*)
Key words: 3D modelling, digital elevation models, geomatics,
structural geology, Western Alps.
INTRODUCTION
This work represents a multi-disciplinary approach where
geological, structural and stratigraphic logs data were combined
in a GIS environment, to obtain a 3D reconstruction and 3D
geometrical model of the mineralizations hosted in different
Alpine structural contexts. Two cases regarding talc (Germanasca
valley) and asbestos mineralizations (Lower Lanzo valley) in the
inner Western Alps were considered.
In the Germanasca valley, the talc mineralization horizon,
currently exploited by the Luzenac Val Chisone S.p.A, is hosted
in the poly-metamorphic basement of the Dora-Maira Unit
(SANDRONE et alii, 1993 with references therein), a continental
crust unit belonging to the Penninic Domain of the Western Alps.
The mineralization horizon geometry is particularly complex as it
is folded by at least four ductile deformation phases. Moreover,
the talc horizon is dissected by brittle faults with different
orientation that may have displaced the mineralization. In the
Lanzo valley the asbestos mineralization have been intensively
exploited up to the end of the last century, particularly near the
Balangero village, where one of the biggest asbestos mine in the
world is present. In this area the asbestos mineralization are
associated mostly to E-W striking semi-brittle to brittle faults,
which dissect the serpentinites of the Lanzo Ultramafic Complex
(BALESTRO et alii, 2009 with references therein).
METHODOLOGY
The Geomatics methods and techniques have been essential
_________________________
(*) Dipartimento Scienze della Terra, Università di Torino,
paola.cadoppi@unito.it
(**) SEA Consulting s.r.l
(°) A.R.P.A. Piemonte
(°°) Rio Tinto Minerals, Luzenac Val Chisone S.p.A.
63
for the study of the Western Alps landscape and the
reconstruction of the whole geological/geomorphological aspects,
multitemporal and multispatial ones.
Two research lines have been started: the first one includes
analysis based on the comparison of digital elevation models
(DEMs) derived from digitized historical records, specifically
topographical maps to define changes in the mine exploitation;
the second one is devoted to using a link between GIS tools and
3D environment.
Fig. 1 – Original Surface. Digital Elevation Model derived from hystorical
map of Balangero mine zone.
dump
Fig. 2 – Current Situation.- Digital Elevation Model derived from the recent
official Cartography of Balangero mine.
In the first step a quantitative analysis was performed with the
aim of identifying changes in the mining exploitation. This
analysis was based on the comparison of digital elevation models
(DEMs) derived from historical records, specifically maps and
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SESSIONE 3
Fig. 3 – Left - multitemporal survey with geology draped on the recent DEM available. Right - location of hystorical geognostic surveys and galleries versus
present topographic surface. Many boreholes are now "suspended."
terrestrial surveys. The DEMs were generated by means of a GIS
workstation, with semi-automatic and automatic procedures
(D’AGATA &ZANUTTA, 2007). The results can indicate the terrain
modifications due to the mine activities (fig.1 and 2)
In the second case cartographic geological and structural data
collected in the field and managed by Geographic Information
Systems (GIS) technology can be used for 3D reconstruction of
complex geological bodies. Using a link between GIS tools and
3D environment, stratigraphical and tectonic surfaces can be
reconstructed taking into account any geometrical constraint
derived from field observations (ZANCHI et alii, 2009).
Geometric features and related attributes are collected into
GIS-geodatabase and used for the 3D modelling by following
steps: (1) topographic data was used for digital elevation model;
(2) stratigraphic, structural and tectonic boundaries, and linear
features was used as 2D polylines; (3) boreholes data was used to
constrain the geological bodies.
The data was imported into 3D environment, the following
steps should be performed: (1) reconstruction of the topographic
surface; (2) 3D mapping of the linear geological boundaries and
linear features; (3) definition of geometrical constraints from
borehole data; (4) construction of a network of cross-sections
based on field observations and geometrical constraints; (5)
creation of 3D surfaces, closed volumes and grids from the
constructed objects.
Two examples of the reconstruction of complex geological
bodies from the Italian Western Alps are presented here. The
methodology demonstrates that 3D modelling has allows the
checking of the geometrical consistency of the interpretative 2D
sections and of the field geology, through a 3D visualisation of
geometrical models (fig. 3).
64
REFERENCES
BALESTRO G., CADOPPI P., PICCARDO G.B., POLINO R.,
SPAGNOLO G., TALLONE S., FIORASO G., LUCCHESI S. &
FORNO M.G. (2009) � Note illustrative della Carta Geologica
d’Italia alla scala 1:50.000 – Foglio 155 Torino Ovest.
ISPRA – Istituto Superiore Protezione Ricerca Ambientale.,
146 pp.
D’AGATA C. & ZANUTTA A. (2007) �Reconstruction
of the recent
changes of a debris-covered glacier (Brenva Glacier, Mont
Blanc Massif, Italy) using indirect sources: Methods, results
and validation. Global Planet. Change, 56, 57-68.
SANDRONE R., CADOPPI P., SACCHI R. & VIALON P. (1993) � The
Dora-Maira Massif. In: von Raumer J.F. & Neubauer F.
(Eds.) - Pre-Mesozoic Geology in the Alps. Springer-Verlag,
Berlin, 317-325.
ZANCHI A., SALVI F., ZANCHETTA S., STERLACCHINI S. &
GUERRA G. (2009) �3D
reconstruction of complex geological
bodies: Examples from the Alps. Comput. Geosci., 35, 49-69.

Mapping the anthropic backfill thickness of the historical center of
Rome (Italy) by using kriging with external drift
GIANCARLO CIOTOLI (*), FRANCESCO STIGLIANO (*), FABRIZIO MARCONI (*), MASSIMILIANO MOSCATELLI (*),
GIAN PAOLO CAVINATO (*),GIUSEPPE CAVUOTO (*), ANGELO CORAZZA(**), MARCO MANCINI (*), ALESSANDRO
PAGLIAROLI (*), FRANCESCO PENNICA (*) & ROBERTO VALLONE (*)
Key words: Backfill surface, digital terrain model,
external drift, geostatistics.
INTRODUCTION
The role played by anthropic backfilling units with
poor geotechnical characteristics to induce seismic
amplification and differential settlements has been
demonstrated by studying the distribution of the
numerous damages that occur in urban environments.
As a matter of fact, the historical centre of Rome is
characterized by the presence of a complex drainage
network filled up by recent alluvial deposits and
subsequently hidden by the anthropic cover which
accumulated during the centuries of urban
development. In this work geostatistical interpolation
techniques by using different kriging methods were
employed and compared in order to determine the best
spatial predictor of the anthropic backfill bottom
surface in the historical center of Rome (Italy). A
bottom surface map was than generated and the
thickness map was calculated by subtracting this new
map to the Digital Terrain Model (DTM).
RESULTS
A set of about 1000 measurements of anthropic
backfill lower boundary (in meters a.s.l.) obtained from
boreholes irregularly distributed all over the study area
was used for the prediction. Data used in this work was
archived in the UrbiSIT database, developed by IGAG
for the Dipartimento della Protezione Civile (i.e. Italian
Civil Protection National Sevice).
The application of kriging methods assume that the
spatial variation of the study variable is too irregular to
be modelled by a continuous mathematical function,
and its spatial variation could be better predicted by a
_________________________
(*)CNR-IGAG, Istituto di Geologia Ambientale e Geoingegneria,
francesco.stigliano@igag.cnr.it
(**)Dipartimento della Protezione Civile Nazionale
Lavoro eseguito nell’ambito del progetto UrbiSIT, con il contributo
finanziario del Dipartimento della Protezione Civile Nazionale
65
probabilistic surface.
Variography have been used to describe the way in
which similar observation values are clustered in space,
in accordance with Tobler’s first law of geography,
giving the measure of the dissimilarity of data pairs as
the spatial separation between them increases. In
particular, ordinary kriging (OK) and universal kriging
(UK) have been applied, preliminarily. Furthermore,
mixed methods are also used and compared in
exploiting the ability of regression to relate the target
variable to other spatially distributed variables (i.e
kriging with external drift, KED). The KED is a
particular case of UK that allows the prediction of a
variable Z, note only at a limited set of points in the
study area, through another variable S, exhaustively
known in the same area. Variable Z is modeled with a
random function Z(x) and S as a deterministic variable
S(x). The KED method thus consists in incorporating
into the kriging system additional universality
conditions about one or several ED variables measured
exhaustively in the study spatial domain. The variable
S(x) need to be known at all locations xi of the samples
of Z(xi), as well as at the node of the prediction grid.
As a good correlation still exists between the
backfill basal surface morphology and the present day
topography of the historical center, DTM data at the
spatial resolution of 20x20m were used as external drift
variable for kriging interpolation. The root mean
square error (RMSE) was computed from the
validation sample (observed data) and predicted values.
The collected data have been interpolated by using a
50x50m spatial grid to produce the final map. The
study of spatial variability by modeling the
experimental variograms highlights an anisotropic
behaviour of the data in the N320-330 direction with a
major and minor axes of about 3000 m and 1500,
respectively (anisotropy ratio, R=2). This anisotropic
behavior generally agree with the main morphological
features of the area. The experimental variograms have
been modeled by using a spherical model with a nugget
of 45, a sill of 250 and a range of about 3000 m (γ=
45+250 sph (3000). The model was used in the kriging
algorithm in order to estimate backfill bottom values at
unsampled location.
SESSIONE 3

SESSIONE 3
a b c
Figure 1. Scatteplots of cross-validation results obtained by using different interpolation methods. Ordinary Kriging (a) provides a regression
coefficient (r 2 ) of 0.851, Universal Kriging (b) a regression coefficient (r 2 ) of 0.702, and Ordinary Kriging with external drift (c) a regression coefficient
(r 2 ) of 0.952.
Estimated surface obtained by using OK and UK
provides cross-validation results with a regression
coefficient (r 2 ) of 0.851 and 0.702, respectively. By
adding into the ordinary kriging system the additional
condition provided by the external drift variable (i.e.,
DTM), the estimation of the backfill-bottom surface
has been improved, in fact the cross-validation gives a
regression coefficient (r 2 ) of 0.952 (Fig. 1). A further
attempt by using DTM as covariate in the cokriging
(CoK) algorithm provides a good regression coefficient
(0.902), however the CoK is a time consuming
procedure with respect to the KED because it needs to
adjust the variograms of the variable, of the covariate
and of the cross-variate.
In the presented case study, kriging with an external
drift seems to give the most coherent results in
accordance with cross-validation statistics. If there is a
correlation between backfill basal surface morphology
and topography, it seems logical that the inclusion of
topographic information should improve the estimates
(Fig. 2). Furthermore, KED has the advantage of
requiring a less demanding variogram analysis than
cokriging. The application of a numerical technique
based on the theory of Intrinsic Random Functions of
order k (IRF-k), for the optimum spatial interpolation
could be the next step of this research. This technique
should better improve the construction of geostatistical
generalized estimators composed by two
functions: one random portion, while the second
portion is deterministic containing the spatial trend of
the non-stationary parameter.
Figure 2. Map of the backfill-bottom surface (above) of the historical centre
of Rome obtained by using ordinary kriging with external drift (KED).
Below the map of the backfill thickness is shown, the map has been
obtained by subtracting the grid of the backfill bottom surface from the
DTM.
66

3D reconstruction of the periadriatic portion of the Apennines foldand-thrust-belt
(Marche –Abruzzi onshore)
Key words: Anticlines, fold-and-thrust-belt, seismic lines.
INTRODUCTION
The more external part of the Apennines fold and thrust belt is
located in the Periadriatic basin and is mostly buried under a synand
post- orogenic, Plio-Pleistocene, siliciclastic sequence.
The structural setting of this sector of the fold-and-thrust belt
is the results of the combination of extremely superficial thrustrelated
anticlines and their respective deeper ramps. The formers
mainly affect the siliciclastic foredeep deposits and the
synorogenic sequences (Pliocene-Pleistocene), whereas the
second ones, constituting the deeper thrust system, crosscut the
Triassic-Miocene carbonates and the overlying Messinian-
Pliocene siliciclastic sediments. The result is a belt characterized
by deeper ramps in the carbonate sequence, long flats developed
at their top, and shallower ramps and related anticlines involving
the Plio-Pleistocene siliciclastic sequence. This geometric
organization influences the sequence of thrust-system propagation
and characterises the evolution of syn-tectonic basins
(CENTAMORE et alii., 1992; ORI et alii., 1991). Moreover,
spacing and location of thrust ramps seems to be controlled by
pre-existing discontinuities that affect the foreland ramp (normal
faults).
The present study has the aim to build a 3D model of this
portion of the chain, using the interpretation of our available 2D
seismic dataset (Fig.1) and collecting together a considerable
amount of data.
STRUCTURAL SETTING
The reconstruction of this sector of the Apennines allows to
_________________________
ALESSIA CONTI (*), PIERO CASERO (**), SABINA BIGI (*), LIVIO RUGGIERO (*),
RICCARDO RECANATI (°) & LORENZO LIPPARINI (°)
(*) Dipartimento di Scienze della Terra, Università “La Sapienza”, Roma.
sabina.bigi@uniroma1.it
(**) caseropiero@libero.it
(°) Medoilgas Italia S.p.A., llipparini@medoilgas.it
67
correlate and follow in the third dimension the main thrust fronts
recognized using seismic lines interpretation and already known
in literature (ARGNANI et alii, 1991; CENTAMORE et alii, 1992;
ORI et alii, 1992). The 3D model comprises the area in the
footwall of the Teramo Thrust (BIGI et alii, 1999; BIGI et alii,
2009) which tectonically translated eastward the Messinian
domain onto the younger Pliocene domain. To the east of this
thrust, seismic lines interpretation pointed out the occurrence of
two main N-S thrust-related-anticlines buried below the
siliciclastic Plio-Pleistocene deposits: the inner trend, located
close to the outcropping front of the chain (in the western portion
of the basin) and the coastal trend, located close to the present
coast line. Since the activity of those structures starts during the
upper part of Lower Pliocene, they subdivide the basin in several
Fig. 1 – Location map of the study area
depocenters: the inner one, which shows the shape of a wide
syncline and the outer one, bounded to the east by the Costiera
structure (ORI et alii., 1991). More eastward, a wedge-shape
Lower Pliocene - Pleistocene sequence is recognized,
corresponding to the new foredeep basin deposits.
The main structure reconstructed in the 3D model (Fig .
2) are
the Nereto - Bellante thrust and the younger and deeper
Villadegna - Costiera thrust. The former reaches the maximum
offset and structural elevation in the northern sector (between
Teramo and Ascoli Piceno), whereas the Villadegna structure is
more evident in the southern area and shows a regional northward
axial plunging, evidenced in the 3D model.
SESSIONE 3

SESSIONE 3
Fig. 2 – 3D MOVE recostruction of the principal structural trends and main horizons pointed out by seismic interpretation.
The geometry of the thrust and related growth folds suggests a
deformation mechanism of those structures, characterized by two
main steps. In the first part of thrust evolution, the main anticline
becomes active as a wedge thrust. It shows a fore-thrust ramp,
that cuts the pre-Messinian footwall succession and is linked to a
deep detachment level (Permo-Triassic deposits). During this
stage the growing anticline partially controlled the foredeep
sedimentation, acting as a structural high inside the foredeep; the
development of a backthrust located at the top of the carbonate
succession is also possible. At the tip point of the forethrust,
when it reaches the top of Apulian platform in the footwall, a new
flat develops, involving the siliciclastic deposits of sedimentary
sequences. These flats evolve at the thrust front with the growing
anticlines (Bellante - Nereto and Costiera structures) that control
the depocenters location of Pliocene-Pleistocene foredeep
deposits.
REFERENCES
ARGNANI A., ARTONI A., ORI G.G. & ROVERI M. (1991) -
L’avanfossa centro-adriatica: stili strutturali e
sedimentazione. Studi Geolog. Camerti. vol. spec., 1991/1,
371-381.
ARTONI A. & CASERO P. (1997) - Sequential balancing of growth
structures, the late Tertiary example from the central
Apennines. Bull. Soc. Gèol. France, 168, 35-49.
CASERO P. (2004) - Structural setting of petroleum exploration
plays in Italy. Spec. Vol. of the Italian Geological Society for
the IGC 32 Florence 2004, 189-199.
CASNEDI R. & SERAFINI G. (1994) – Interpretazione geologica
della sezione sismica nella valle del Vomano (Abruzzo). Atti
Tic. Sc. Terra, serie speciale, 2, 45-49.
BIGI S., CALAMITA F., CELLO G., CENTAMORE E., DEIANA G.,
PALTRINIERI W., PIERANTONI P.P. & RIDOLFI M. (1999) -
Tectonics and sedimentation within a Messinian foredeep in
the Central Apennines, Italy. J. Petroleum Geol., 22, 5-18.
68
BIGI S., MILLI S., CORRADO S., CASERO P., ALDEGA L., BOTTI F.,
MOSCATELLI M., STANZIONE O., FALCINI F., MARINI M. &
CANNATA D. (2009) - Stratigraphy, structural setting and
burial history of the Messinian Laga basin in the context of
Apennine foreland basin system. J. Of Mediterranean Earth
Sciences, 1, 61-84.
CENTAMORE E., ADAMOLI L., BERTI D., BIGI G., CASNEDI R.,
CANTALAMESSA G., FUMANTI F., MORELLI C., MICARELLI
A.,RIDOLFI M., SALVUCCI R., CON LA COLLABORAZIONE DI
CHIOCCHINI M., MANCINELLI A., POTETTI M. & CHIOCCHINI
U. (1992) – Carta geologica dei bacini della Laga e del
Cellino e dei rilievi carbonatici circostanti (Marche
meridionali, Lazio nord orientale, Abruzzo settentrionale).
S.E.L.C.A., Firenze.
ORI G.G., SERAFINI G., VISENTIN C., RICCI LUCCHI F., CASNEDI
R., COLALONGO M.L. & MOSNA S. (1991) - The Pliocene-
Pleistocene Adriatic Foredeep (Marche and Abruzzo, Italy):
an integrated approach to surface and subsurface geology. In
Agip EAPG (eds), 3 rd E.A.P.G. Conference. Adriatic
Foredeep Field Trip, Guide Book, 85 pp.
PATACCA E., SCANDONE P., BELLATALLA M., PERILLI N. &
SANTINI U. (1991) - La zona di giunzione tra l’arco
appenninico settentrionale e l’arco appenninico meridionale
nell’Abruzzo e nel Molise. Studi Geolog. Camerti. vol. spec,
1991/2, 417-441.

Key words: 3D modelling, seismic hazard assessment.
In the frame of S1 - Seismological Project funded by the
Italian Civil Protection Department 3D modelling and
visualization techniques have coupled and supported the
traditional methods for the seismic hazard assessment.
Great amount of data, both geological and geophysical, are
produced and collected in the S1 Project “Definition of the
seismic potential in Italy for the evaluation of the seismic
hazard”; they are characterized by different distribution and
different degree of detail, although national wide datasets are
prevailing.
Analysis and comparison of geological and geophysical
datasets describing crustal and sub-crustal structures have been
performed in a 3D environment addressing the inconsistencies in
the original datasets and defining areas where more details are
needed.
The main original datasets are: geological data from seismic
profiles for specific areas (i.e.: Po Plain, central Adriatic offshore,
Marche-Abruzzi on-shore), the Database of seismogenic
sources (DISS WORKING GROUP, 2009), the Catalogue of the
Italian Seismicity (CSI, CASTELLO et alii, 2006), the depth model
for the Mohorovicic discontinuity for the Italian region and
surrounding seas, the cellular model for the lithosphereasthenosphere
system.
The integration of these multi-scale datasets has pointed out
critical areas with major differences between them; further
analyses have been performed to distinguish discrepancies
deriving from the techniques for data acquisition, rather than
from different interpretations of original datasets (Fig. 2) or
produced by the interpolation algorithms chosen in the 3D
modelling software.
This procedure allows to verify the model consistency related
to the available data and to rebuild or update the model owing to
information updating.
_________________________
3D modelling of multi-scale geological and geophysical data:
data integration and model validation
(*) ISPRA, Servizio Geologico d’Italia/Dipartimento Difesa del Suolo.,
chiara.dambrogi@isprambiente.it; mariapia.congi@isprambiente.it
This research has benefited from funding provided by the Italian Presidenza
del Consiglio dei Ministri - Dipartimento della Protezione Civile (DPC).
Scientific papers funded by DPC do not represent its official opinion and
policies.
CHIARA D’AMBROGI (*) & MARIA PIA CONGI (*)
69
Two main type of elaborations and data integration have been
carried out in the Project: 3D models of crustal structures,
including seismogenic sources and their geological constraints;
3D model of the lithosphere-astenosphere system for the Italian
region.
The 3D model of the crustal structures combines geometric
data deriving from Database of seismogenic sources (DISS) with
geological constraints, regional or national wide, and earthquake
locations (CSI).
The resulting 3D objects are: surfaces representing the
geometry of each Individual seismogenic Source, surfaces
wrapping an unspecified number of Individual Sources and
defining Composite seismogenic Sources, points defining the
earthquake location parameters and their related magnitude,
surfaces representing key horizons (e.g.: base of Pliocene
deposits) representing national wide datasets or regional 3D
models (Fig.1). These 3D crustal models are essential as input for
further 3D structural analyses supporting seismic hazard
assessment, such as the evaluation of the slip rates.
Fig. 1 – 3D crustal model for the Po Plain integrating geological cross
sections, earthquake locations, composite seismogenic sources (CS) and the
base of Pliocene deposits.
The 3D model for the lithosphere-asthenosphere system
includes three surfaces representing the Moho discontinuity,
distinguished in European, Tyrrhenian and Adriatic, and volumes,
defined by different thickness (h), Vs, Vp and Density values, and
describing the main characteristics of the lithosphereasthenosphere
system.
SESSIONE 3

SESSIONE 3
Fig. 2 – Geological cross section from 3D model of the lithosphere-astenosphere system. Area with major differences between datasets is outlined. The
highlighted model inconsistency (Adriatic Moho overriding Tyrrhenian Moho) has been corrected in the following elaborations.
The final result is a 3D imagery of seismogenic structures and
earthquake locations for the entire Italian region coupled with a
preliminary 3D elaboration of the structural model for the
lithosphere-asthenosphere system.
The comparison within these datasets highlights the existing,
both geometrical and parametrical, inconsistencies in the defined
models supporting the definition of a more comprehensive model
(Fig. 2).
REFERENCES
CASTELLO B., SELVAGGI G., CHIARABBA C. & AMATO A. (2006) -
CSI - Catalogo della sismicità italiana (1981-2002), version
1.1”, INGV-CNT.
http://legacy.ingv.it/CSI/versione_inglese/index_eng.htm
DISS WORKING GROUP (2009) - Database of Individual
Seismogenic Sources (DISS), version 3.1.0: A compilation of
potential sources for earthquakes larger than M 5.5 in Italy
and surroundings areas. http://diss.rm.ingv.it/diss/, © INGV
2009 – Istituto Nazionale di Geofisica e Vulcanologia.
70

Keywords: Energy, mapping, technologies
With increasing need for resource security (energy, raw
materials, water), waste management, sequestration along with a
more sensitive management of the environment geologists need to
be able to deliver better predictive sub-surface models where
both precision and accuracy are understood.
As uncertainty in geological interpretations can be large and is
often unconstrained by hard data a single interpretation may not
be adequate to characterise and understand the relationship
between surface and subsurface geology.
These models need to be accessible to stakeholders and end
users, not just to geologists.
Traditional paper and pencil representations of the surface
and subsurface accompanied by descriptive geo-histories are no
longer represent appropriate deliverables for these evolving needs
where the end user requires a digital model that can be visualised
and manipulated as input for work by other discipline groups.
By looking at geology from a consumer point of view we can
adopt and adapt best practice from a wide range of technologies
to develop professional workflows, training and the necessary
tools to meet this new paradigm.
This contribution illustrates one approach to how we might
address this for the 21 st century and integrate the needs of a range
of end user communities.
_________________________
Mapping in 4 dimensions - raising the game in geology
for the 21 st century
(*) MVE Midland Valley Exploration Ltd. alan@mve.com
ALAN GIBBS (*)
71
SESSIONE 3

SESSIONE 3
Three-dimensional geological and geomechanical modeling of the
Northern Apennine front in the Po Plain
MICHELE LIVANI (*), LUIGI VADACCA (*), DAVIDE SCROCCA (*), EUGENIO CARMINATI (**),
ELIO BIANCHI (°) & ROBERT NEWMAN (°°)
Key words: 3D model, geomechanics, Po Plain, thrust system.
ABSTRACT
In this work we built a three-dimensional geometrical model
of a sector of the Ferrara-Romagna fold and thrust system buried
under the Plio-Pleistocene sediments of the Po Plain in order to
model numerically the active stress field of the region.
The geometrical model was built using the commercial
software Petrel 2009 (Schlumberger). The input data include:
1. the Digital Elevation Model (DEM) of the topography
surface;
2. the grid of the Plio-Pleistocene base;
3. the grid of the Cretaceous top, realized by digitizing the map
published by CASERO et alii (1990);
4. the composite seismogenic sources of the Database of
Seismogenic Sources (DISS) version 3.1.0;
5. some geological sections reported in the literature
(BOCCALETTI et alii, 2003; FANTONI &FRANCIOSI, 2009;
PIERI &GROPPI, 1981).
Once collected, these data were imported into Petrel, using
the following procedure. Originally, the DEM, grid horizons and
DISS seismogenic sources have been imported as points defined
by three coordinate values (Easting, Northing and depth). Later,
these data were converted from points to surfaces. The geological
sections have been imported to control the geometry of horizons
and faults. Both faults and horizons were adjusted to make them
coherent with the sections.
The main tectonic elements in the model consist of a set of
ramps that converge downward to the main detachment likely
located within the Upper Triassic units.
_________________________
(*) Istituto di Geologia Ambientale e Geoingegneria, CNR, Roma,
geo.2003@libero.it
(**) Dipartimento di Scienze della Terra, Universita` degli Studi di Roma
‘‘La Sapienza’’
(°) Independent Resources plc, Roma
(°°) Schlumberger, Bracknell, UK
This research has benefited from funding provided by the Italian Presidenza
del Consiglio dei Ministri – Dipartimento della Protezione Civile (DPC)
and by Independent Resources plc. Scientific papers funded by DPC do not
represent its official opinion and policies.
72
Fig. 1 – 3D structural model built in Petrel 2009. The main surface
corresponds to the top Cretaceous (modified after CASERO et alii, 1990),
rectangles are the main seismogenic sources (DISS 3.1.0), and dots are
ipocentres according to the CSI 1.1 catalogue.
Afterwards this geometry was imported in Visage for the
numerical modelling.
A 3D model has been realised to simulate the present-day
stress field of the Northern Apennines frontal thrust system. An
elasto-plastic rheology was adopted for the modelling using the
Mohr-Coulomb failure criterion. Geomechanical properties for
each formation and faults comprised Young’s modulus, Poisson’s
ratio, density, frictional angle, cohesion and they were assumed
on the basis of published geological data.
The models were performed in three steps with different
boundary conditions. In the first step we simulated the lithostatic
stress (Sv), obtaining a model in equilibrium with gravity. The
side boundaries were constrained horizontally. Afterwards, loads
were added to simulate a regional stress state comprising the
tectonic loading component (SH and Sh). However, to evaluate
the validity of the results, the model solutions were compared
with the map of the active stress field and with the data of
seismicity in the same area. In the last step of the simulation
(tectonic phase) we forced the models with a 1 meter
displacement (applied onto the SW lateral boundary) directed
toward NE, simulating the shortening occurring in the region in
1000 years, according the present-day plate kinematics of the
Northern Apennines region. The tectonic displacement was
applied by 0.1 step increments to evaluate the change of the
mechanical properties along the principal tectonic features.

Fig. 2 – Orientation and magnitude (in kPa) of the major stress axes
predicted by the mechanical model. Map view. Notice the rotation of the
stress axes, that is controlled by the rheological behaviour of the materials
and by the occurrence of faults.
ACKNOWLEDGEMENTS
Schlumberger is grateful acknowledged for making available the
Petrel and Visage softwares. Chiara D’Ambrogi kindly provided
some of the digital data. Rob Marsden, John Fuller, Roberto
Bencini and Alessandro Romi are also thanked for fruitful
discussion.
REFERENCES
BOCCALETTI M., BONINI M., CORTI G., GASPERINI P., MARTELLI
L., PICCARDI L., TANINI C. & VANNUCCI G. (2003) - Carta
sismotettonica della regione Emilia-Romagna. Scala
1:250.000. Regione Emilia-Romagna.
CASERO P., RIGAMONTI A. & IOCCA M. (1990) - Paleogeographic
relationships during cretaceous between the Northern
Adriatic area and the eastern Southern Alps. Mem. Soc.
Geol. It., 45, 807-814.
FANTONI R. & FRANCIOSI R. (2008) - Geological framework of
Po Plain and Adriatic foreland system. In: Proceedings of the
70 th EAGE Conference and Exhibition, Rome.
FANTONI R. & FRANCIOSI R. (2009) - Mesozoic extension and
Cenozoic compression in Po Plain and Adriatic foreland.
Rendiconti online Soc. Geol. It., 9, 28-31.
PIERI M. & GROPPI G. (1981) - Subsurface geological structure of
the Po Plain, Italy. Progetto finalizzato Geodinamica-
Sottoprogetto 5, Modello strutturale, C.N.R., 414, Rome.
73
SESSIONE 3

SESSIONE 3
Key words: Algeria, fracturing, oil field.
The field of Hassi Messaoud is located 850 km south east of
Algiers, 300 km from the Tunisian border and 80 km east of
Ouargla. It has an area of 4200 km 2 . It is considered the largest
field of the Triassic Province. By its size and its reserve is the
largest oil field in Algeria.
From a geological perspective, the field of Hassi Messaoud is
in the center of the Triassic Province in the south east of Algeria.
The field of Hassi Messaoud is divided into production areas
bounded by faults sometimes. We chose the Zone 4 field of
Hassi Messaoud, because it shows a marked by intense tectonic
development of faults and fractures. These fractures contribute
differently to the productivity of the reservoir and this sometimes
in the same lithologic levels.
The majority of fractures have a preferred direction NE-SW
which is subparallel to the direction of the breakout so many of
them are closed (SH = NW-SE). The fractures are perpendicular
to them are infrequent but are open.
The well tests indicate that the reservoir behaves
heterogeneous environment, as well found in a fault zone have
better petrophysical parameters. However, the wells located away
from major accidents are more frequent secondary permeabilities
and higher who are in contact with open fractures. Thus fractures
may play a positive role (secondary porosity and permeability) or
negative (barrier permeability by silicification tectonics) in
productivity; they can also be the source of major problems such
as breakthrough of water or gas. Our study focuses on the
analysis and modeling of petrophysical parameters and fracturing.
For this we have combined several approaches using imaging
sides the well test and onventional logging. All acquisitions were
processed using multiple software PETREL namely, the
Interactive Petrophysics and Sapphire. We have reached a 3D
geological model with the distribution of secondary porosity and
permeability.
_________________________
Analysis and modeling of the fracturing of the oil field area 4 of
Hassi Messaoud (Algeria)
(*) Faculty of Hydrocarbon-University of Boumerdes, Algeria,
k_loumi@yahoo.fr
KHALED LOUMI (*) & MOHAMED KELKOULI (*)
74

Long-term geological slip rates of the Emilia thrust front (Northern
Apennines) from 3D modelling of key buried horizons
FRANCESCO E. MAESANO (*), CHARA D’AMBROGI (*), PIERFRANCESCO BURRATO (**) & GIOVANNI TOSCANI (°)
Key words: 3D modelling, Emilian Arc, Northern Apennines, slip
rates.
INTRODUCTION
The Northern Apennines fold and thrust belt (NA) developed
during the Neogene and Quaternary in the framework of the
African and European plates convergence. GPS studies show that
plate convergence at the Italian latitude is going on with rates
ranging between 3 and 8 mm/a (e.g. NOCQUET &CALAIS, 2004;
SERPELLONI et alii, 2007).
The outermost thrust front of the NA belt are buried below the
Plio-Quaternary marine and continental deposits infilling the Po
Plain basin or are partially exposed along its southern margin,
and are organized in three complex arcs that from west to east
are: the Monferrato, the Emilian, and the Ferrara-Romagna arcs.
The buried compressional structures were extensively studied by
seismic exploration lines and deep well logs. These subsurface
data show a system of N to NE-verging blind thrusts and folds
that controlled the deposition of the syntectonic sedimentary
wedges, with the Plio-Quaternary sequence locally up to 7-8 km
thick. The fast sedimentation (BARTOLINI et alii, 1996) hid the
growing structures, and as a consequence there are few direct
surface evidences of the possible ongoing activity of the thrusts.
One of the few and most notably exception to this general rule is
the San Colombano Hill, that is an outcropping anticline located
at the leading edge of the Emilian Arc, involving upper Pliocene
and lower Pleistocene sediments and cored by Miocene deposits.
Present-day activity of the frontal thrusts of the NA is testified
by historical and instrumental seismicity, the latter characterized
by contractional focal mechanisms (PONDRELLI et alii, 2006), and
by the influence on the drainage network (BURRATO et alii, 2003)
75
and faulting and folding of recent sediments. The historical and
instrumental Italian seismic catalogues show that the southern Po
Plain is affected by low to moderate seismicity, with Mmax up to
5.8 (CPTI WORKING GROUP, 2004; CASTELLO et alii, 2006; DISS
WORKING GROUP, 2009). The borehole breakouts and the focal
mechanisms both show Shmax oriented perpendicular to the trend
of the buried thrust fronts (MONTONE et alii, 2004).
GPS studies constrain a weak SW-NE shortening across the
Po Plain, with rates of less than 1 mm/a (SERPELLONI et alii,
2005). The shortening is accomplished in the frame of a CCW
relative rotation of the Adriatic promontory respect to Eurasia,
with a pole of rotation located in the western Alps (CALAIS et alii,
2002). As a consequence the rates of convergence are expected to
diminish westward in agreement with the observed lowering of
the seismic moment release.
3D MODELING OF THE CENTRAL EMILIAN ARC
In this study we present a 3D reconstruction of the central
portion of the Emilian Arc along a 50 km long, NNE-oriented
swath, running from the outcropping thrust wedge to the south
and including the outermost buried anticlines of the NA to the
north (Fig. 1). The study section was chosen because of available
public subsurface data, it is located in between the two regional
sections published by TOSCANI et alii (2006), and it is
perpendicular to the main trend of the buried structures. The main
goal of this study is to calculate long-term (Pliocene-Holocene)
geological slip rates of the thrust underlying the buried fold.
We follow a similar approach as that used by SCROCCA et alii
(2007). We reconstructed in 3D the subsurface geometry of pre-
_________________________
(*) ISPRA, Servizio Geologico d’Italia/Dipartimento Difesa del Suolo,
framae80@gmail.com , chiara.dambrogi@isprambiente.it
(**) Istituto Nazionale di Geofisica e Vulcanologia,
pierfrancesco.burrato@ingv.it
(°) Dipartimento di Scienze della Terra, Università di Pavia,
toscani@dst.unipv.it
This research has benefited from funding provided by the Italian Presidenza
del Consiglio dei Ministri - Dipartimento della Protezione Civile (DPC).
Scientific papers funded by DPC do not represent its official opinion and
policies. Fig. 1 – 3D model of the studied area.
SESSIONE 3

SESSIONE 3
and syn-tectonic strata, using for the deep portion of the model
structural surfaces derived from interpreted cross-sections
(TOSCANI et alii, 2006), constrained by the stratigraphy of deep
oil well logs. The shallow portion of the model was derived by
the stratigraphic data used for the reconstruction of the regional
aquifers (REGIONE EMILIA ROMAGNA & ENI-AGIP, 1998;
REGIONE LOMBARDIA &ENI, 2002).
After the model building a decompaction workflow was
applied to the 3D model in order to remove the effects of rock
volume change due to porosity reduction through time allowing
the better definition of the slip rates. The horizons backstripping
allows the underlying rocks to vertically decompact, as a result of
the removal of the overburden.
Using algorithms supplied by the software package Move
(MVE, Ltd) we restored the effects of compaction history for the
acquifer horizons dated to 0.45 My, 0.65 My, 0.8 My and for the
top of Pliocene and Messinian. The decompaction was performed
with the 3DMove Decompaction tool, using the flexural isostasy
setting and assuming a sub-aerial load for the two uppermost
aquifers (0.45 My, and 0.65 My) and a submarine load for the
deepest aquifer (0.8 My) and the underlying Pleistocene (1.8 My)
and Pliocene deposits (5.3 My).
We performed the slip rate calculations for the unfaulted
horizons using two methods, that gave comparable results: 1) an
elastic half-space dislocation modelling of surface deformation,
and 2) a trishear fault propagation modelling (Trishear algorithm
in 2DMove). To better describe the evolution of main thrust we
calculated the slip rate also on the faulted horizons (top Pliocene
and top Messinian); the calculation was extended to the whole 3D
model to verify the lateral variation along the thrust. The
Separation tool in 3DMove was used to measure the heave, throw
and slip between fault cutoffs.
REFERENCES
BARTOLINI C., CAPUTO R. & PIERI M. (1996) – Pliocene-
Quaternary sedimentation in the Northern Apennine
Foredeep and related denudation. Geol. Mag., 133 (3), 255-
273.
BURRATO P., CIUCCI F. & VALENSISE G. (2003) – An inventory of
river anomalies in the Po Plain, Northern Italy: evidences for
active blind thrust faulting. Ann. Geophys., 46 (5), 865-882.
CALAIS E., NOCQUET J. M., JOUANNE F. & TARDY M. (2002) –
Current strain regime in the western Alps from continuous
Global Positioning System measurements, 1996-2001.
Geology, 7, 651-654.
CASTELLO B., SELVAGGI G., CHIARABBA C. & AMATO A. (2006) –
CSI Catalogo della sismicità italiana 1981-2002, versione
1.1. INGVCNT, Roma http://www.ingv.it/CSI/.
76
CPTI WORKING GROUP (2004) – Catalogo Parametrico dei
Terremoti Italiani, version 2004 (CPTI04). INGV, Milan,
available from http://emidius.mi.ingv.it/CPTI04/.
DISS WORKING GROUP (2009) – Database of Individual
Seismogenic Sources (DISS), Version 3.1.0: A compilation of
potential sources for earthquakes larger than M 5.5 in Italy
and surrounding areas. http://diss.rm.ingv.it/diss/, © INGV
2009.
MONTONE P., MARIUCCI M.T., PONDRELLI S. & AMATO A. (2004)
- An improved stress map for Italy and surrounding regions
(central Mediterranean). J. Geophys. Res., 109, doi:
10.1029/2003JB002703.
NOCQUET J. M. & CALAIS E. (2004) – Crustal velocity field of
western Europe from permanent GPS array solutions, 1996-
2001. Geophys. J. Int., 154, 72-88.
PONDRELLI S., SALIMBENI S., EKSTRÖM G., MORELLI A.,
GASPERINI P. & VANNUCCI G. (2006) – The Italian CMT
dataset from 1977 to the present. Phys. Earth Planet. Int., 159
(3-4), 286-303, doi:10.1016/j.pepi.2006.07.008.
REGIONE EMILIA-ROMAGNA & ENI-AGIP (1998) – Riserve
idriche sotterranee nella Regione Emilia-Romagna. A cura di
G. Di Dio. S.EL.C.A., Firenze.
REGIONE LOMBARDIA & ENI (2002) – Geologia degli Acquiferi
Padani della Regione Lombardia. A cura di C. Carcano & A.
Piccin .S.EL.C.A., Firenze.
SCROCCA D., CARMINATI E., DOGLIONI C. & MARCANTONI D.
(2007) – Slab retreat and active shortening along the centralnorthern
Apennines. In: Lacombe O., Lavé J., Roure F. &
Verges J. (Eds.), Thrust belts and Foreland Basins: from fold
kinematics to hydrocarbon systems.. Springer, 471–487.
SERPELLONI E., ANZIDEI M., BALDI P., CASULA G. & GALVANI A.
(2005) – Crustal velocity and strain-rate fields in Italy and
surrounding regions: new results from the analysis of
permanent and non-permanent GPS networks. Geophys. J.
Int., 161, 861-880, doi: 10.1111/j.1365-246x.2005.02618.x,
1-20.
SERPELLONI E., VANNUCCI G., PONDRELLI S., ARGNANI A.,
CASULA G., ANZIDEI M., BALDI P. & GASPERINI P. (2007) –
Kinematics of the Western Africa-Eurasia plate boundary
from focal mechanisms and GPS data. Geophys. J. Int., 169,
1180-1200, doi: 10.1111/j.1365-246X.2007.03367.x.
TOSCANI G., SENO S., FANTONI R. & ROGLEDI S. (2006) -
Geometry and timing of deformation inside a structural arc:
the case of the western Emilian folds (Northern Apennine
front, Italy). Boll. Soc. Geol. It., 125 (2006), 59-65.

Analogue experiments and numerical modeling exploring the
relationship between volcanoes and thrusting
DOMENICO MONTANARI (*), GIACOMO CORTI (**) & ALEXANDER SIMAKIN (°)
Key words: Analogue modelling, granite emplacement,
numerical modelling, structural geology.
INTRODUCTION
Although magma emplacement in compressional settings is
now generally accepted and described in different natural
examples (e.g., TIBALDI, 2008; GONZALEZ et alii, 2009 and
references therein), the modalities of interaction between
volcanic edifices and contractional structures still remain in part
to be defined. Analogue modeling studies have shown a strong
interaction between magma uprising and contractional
deformation, with active thrust systems representing a
preferential pathway for ascending magma (e.g., GALLAND et
alii, 2007; MONTANARI et alii, 2010). Magma migration and
emplacement, in turn, have shown to be able to control the
architecture of thrust systems: the effects of both migration of the
low-viscosity fluids that may act as a basal detachment for the
compressive structures (e.g., GALLAND et alii, 2007), and the
load of volcanic edifices (when magma reaches the surface) may
reorient the local stress/strain fields (e.g., MARQUES &COBBOLD,
2002), resulting in the final arcuature of the thrust systems in
front of the volcanoes or migrating magma. In this study, we
present the results of both analogue and numerical modeling that
provide further insights into the relations between volcanoes and
thrust faults. The models implement previous experimental works
by accounting for the presence of an upper crustal active magma
chamber below a volcano, introducing a strong rheological
heterogeneity able to exert a strong potential control in
stress/strain localization during deformation. Results indicate that
the presence of a volume of low-viscosity magma is able to
strongly influence the structural pattern, acting as a strain
attractor for the compressional deformation.
ANALOGUE MODELLING
The experiments were performed at the TML of the C.N.R.-
IGG, with an apparatus to model pure shear and simple shear
_________________________
(*) Centro di Eccellenza per la Geotermia di Larderello,
domenico.montanari@gmail.com
(**) Istituto di Geoscienze e Georisorse, CNR, giacomo.corti@unifi.it
(°) Institute Experimental Mineralogy RAS, simakin@iem.ac.ru
77
deformation. The models were made of a single pack of quartzsand,
simulating the brittle upper crust, containing a central
elliptic rheological heterogeneity (magma chamber), reproduced
by a low viscosity mixture of silicone and oleic acid (for material
properties see MONTANARI et alii, 2010). The analogue magma
chamber has the shape of an ellipsoid and was present by the
beginning of deformation. Comparative tests included the
presence of a surface conic volcanic edifice (made of quartzsand)
above the magma chamber in order to evaluate its effect on
the pattern of deformation.
Geometrical, rheological, kinematical and dynamical
similarity ensured scaling to the natural process under
investigation (MONTANARI et alii, 2010), with a length ratio of
l*~1.10 -5 (1 cm in the model represents ~1 km in nature) and a
velocity ratio of v*~6.5.10 -3 (the ~2 cm/h of model shortening
correspond to a natural shortening rate of ~27 mm/yr).
Shortening results in arcuate contractional structures, which
curve towards the low-viscosity magma (Fig. 1). The main thrust
is thus “captured” by the low-viscosity silicone, which is
shortened and uplifted creating a structural relief and a small
collapsed structure at the top.
In the presence of a magma chamber, the inclusion of a
volcano at surface has no influence on the resulting structural
pattern and the main thrust is still characterized by an arcuature
towards the low-viscosity magma (Fig. 1).
NUMERICAL MODELLING
Sand-box analogue results presented above can be
rationalized with simple numerical simulations. For the
calculation it was used FEM code designed for the modeling of
the deformations of liquid inclusion in the non-isothermal
Maxwell solid with strain and temperature dependent viscosity
(SIMAKIN & GHASSEMI, 2010). Stress distribution around
chamber can be approximately evaluated in two 2D sections
(vertical and horizontal) through its center; as in the analogue
modeling, chamber has shape of the ellipsoid with short vertical
axis. In the vertical section two configurations (with and without
volcanic load) have been considered.
During compression, the roof layer experiences uplift, as
observed in the analogue models. In the case without volcanic
cone, uplift is characterized by a smooth gauss-like shape.
Conversely, in the presence of a volcano, a combination of
overall uplift and subsidence under volcanic edifice produces
discontinuities in the displacement field at the cone edges.
SESSIONE 3

SESSIONE 3
Taking into account particular mechanical properties (e.g. values
of the internal friction angle and cohesion for sand model or
rocks for Mohr-Coulomb criteria) failure analysis based on the
calculated stress state was performed. Maximum shear stress is
concentrated on the boundary of the magma chamber and
extended in butterfly–like fashion with axis of symmetry
coinciding with principal stresses directions. 3D failure pattern
revealed in analogue study in general follows these 2D hints.
Thrust fault trajectory near the buried magma chamber is
expected to follow zones with increased shear stress (“wings”
from Fig. 1) and pass slightly outside chamber contour
projection.
DISCUSSION OF THE RESULTS
The modelling results (Fig.1) support the idea that magma
chambers acting as long-lived weakness zone within the
otherwise strong upper crust play a major role in the structural
pattern resulting from shortening. As highlighted by the above
numerical investigations, the magma chamber induces stress
concentration and focuses compressional deformation thus acting
as a “strain attractor” for the advancing thrust front. As a result,
the compressive structures curve towards (and not away from)
the advancing thrusts, giving rise to an opposite arcuature of
structures with respect to that resulting (Fig.1) from previous
works (e.g., MARQUES &COBBOLD, 2002; GALLAND et alii,
Fig. 1 – Influence of an upper crustal magma chamber on deformation and
comparison with previous findings.
2007). In our analogue models the effect of a superimposed
volcanic edifice is insignificant in presence of an upper crustal
magma chamber, as no detectable differences in terms of general
architecture of the thrust systems are observed in models with or
without the volcano. This implies that the effect of volcano
78
loading on the structural pattern is –for the adopted boundary
conditions- subordinated to the stress concentration induced by
the magma chamber, thus possibly limiting findings of the
previous volcano load models (e.g., MARQUES & COBBOLD,
2002) to the cases of inactive volcano (with solidified or absent
magma chamber) or volcanoes with very deep (lower crustal or
subcrustal) magma chambers. Volcanic edifices developed
coevally and interacting with compressional structures as in the
Andean chain (e.g., TIBALDI, 2008; GONZALEZ et alii, 2009) or in
several other places in the world (e.g, TIBALDI et alii, 2010), may
be excellent candidates for testing the above results. As in the
models, complex faults patterns at these edifices may be the
result of the role of strain attractors played by shallow magma
chambers on the advancing thrust front, in addition to other
possible parameters such as volcanic load (MARQUES &
COBBOLD, 2002) or magma migration (GALLAND et alii, 2007).
REFERENCES
GALLAND, O., DE BREMOND D’ARS, J., COBBOLD, P.R., &
HALLOT, E. (2007) - Rise and emplacement of magma during
horizontal shortening of the brittle crust: Insights from
experimental modelling. J. Geoph. Res., 112, B06402,
DOI:10.1029/2006JB004604.
GONZALEZ G., CEMBRANO J., ARON F., VELOSO E.E., & SHYU
J.B.H. (2009) - Coeval compressional deformation and
volcanism in the central Andes, case studies from northern
Chile (23_S–24_S). Tectonics, 28, TC6003,
DOI:10.1029/2009TC002538, 2009.
MARQUES F.O., & COBBOLD P.R. (2002) - Topography as a
major factor in the development of arcuate thrust belts:
insights from sandbox experiments. Tectonophysics, 348,247-
268.
MONTANARI D., CORTI G., SANI F., DEL VENTISETTE C., BONINI
M., & MORATTI G. (2010) - Experimental investigation on
granite emplacement during shortening. Tectonophysics, 484,
147–155.
SIMAKIN A.G., & GHASSEMI A. (2010) - The role of magma
chamber-fault interaction in caldera forming eruptions. B.
Volcanol., 72, 85–101.
TIBALDI A. (2008) - Contractional tectonics and magma paths in
volcanoes. J. Volcanol. Geoth. Res., 176, 291-301.
TIBALDI A., F.A. PASQUARÈ, & D.TORMEY, (2010) - Volcanism
in reverse and strike-slip fault settings. In: New Frontiers in
Integrated Solid Earth Sciences, Editors: S. Cloetingh, J.
Negendank, Springer-Verlag, 315-348, DOI: 10.1007/978-90-
481-2737-5.

A FEM numerical modelling of the polyphase inversion tectonics in
Central Apennines (Italy)
Key words: Central Apennines, numerical modelling,
polyphase inversion tectonics.
INTRODUZIONE
The Central Apennines is an arcuate fold and thrust belt,
characterized by NNE-SSW oblique thrust ramps like the
Olevano-Antrodoco-Sibillini and the Sangro-Volturno, strongly
influenced by the Mesozoic paleomargin architecture (e.g.,
SATOLLI & CALAMITA, 2008 and references therein). These
oblique thrust ramps sign the separation of the Central
Apennines with the Northern Apennines and the southern
Apennines respectively (BOCCALETTI et alii, 2005).
In the Central Apennines, the relationships between thrusts
and normal faults along the Olevano-Antrodoco-Sibillini
oblique thrust ramp allowed us to recognize a tectonic history
characterized by Neogene positive and Quaternary negative
inversion tectonics.
The reconstructed 3D geological inversion tectonics model
has been tested through numerical modelling which can
evaluate well- or mis- oriented pre-existing faults respect to the
new compressive and extensional tectonic phases that interested
the Apennine chain during the Neogene-Quaternary time.
GEOLOGICAL AND NUMERICAL MODELLING
The Central Apennines arcuate chain is characterized by
NW-SE trending thrusts and related folds branching to the SE
along the NNE-SSW Olevano-Antrodoco-Sibillini and Sangro-
Volturno oblique thrust ramps. An inversion tectonics model
has been reconstructed, in which NNE-SSW cross-structures
have been interpreted as pre-thrusting normal faults that
undergone reactivation during Messinian-Pliocene positive
inversion, while NW-SE faults represent pre-thrusting normal
faults displaced by thrusts, according to shortcut trajectories
and subsequently reactivated as normal faults during quaternary
negative inversion tectonics (CALAMITA et alii, 2009a and b)
(Fig. 1).
This 3D geological inversion tectonics model has been
_________________________
ANTONIO PASCULLI (*), ALESSANDRA DI DOMENICA (*) & FERNANDO CALAMITA (*)
(*) Dipartimento di Scienze della Terra, Università “G. d’Annunzio”,
Chieti-Pescara, calamita@unich.it
79
tested through the slip tendency analysis (MORRIS et alii, 1996;
COLLETTINI & TRIPPETTA, 2007) which shows if the preexistent
faults are well oriented or misoriented respect to the
Neogene compressive and Quaternary extensional field stress.
The 3D geological model has been tested according to a
numerical modelling with the aim to reproduce the whole
deformation pattern also in correspondence of the hangingwall
and footwall blocks of the faults.
A double layer has been selected to simulate the system: a
brittle upper crust (10-15 km thick) and a middle-lower crust
whose behaviour is assumed to be ductile (BONCIO et alii,
2004).
The first step of the numerical modelling is to define the
boundary conditions for the whole system.
The surface extension of the fault system is considered of
20-30 km (PIZZI &GALADINI, 2009 and references therein).
The Norico-Bathoniano (50 My) rifting process has been
reconstructed for the Southern Alps by BERRA &CARMINATI
(2009). During Cretaceous and Miocene times these structures
have been reactivated as normal or trascurrent faults also
Fig. 1 – 3D polyphase inversion tectonics model (not in scale): I) prethrusting
normal faults; II and III) Neogene positive inversion tectonics
through reactivation of the NNE-SSW trending normal faults and shortcut of
the NW-SE trending normal faults; III) quaternary negative inversion
tectonics of the NW-SE trending normal faults. Light grey represents the
sedimentary cover (5-9 km thick). White and black lines represent active and
inactive structures, respectively.
during the development of foredeep basins. During the
Messinian the Monti Sibillini area was involved in the orogenic
phase (1-2 My long) (CALAMITA et alii, 1991). The
reactivaction of NW-SE trending normal faults started in the
early Pleistocene (1-1.2 Ma) as documented by the sediments
SESSIONE 3

SESSIONE 3
that fill quaternary tectonic depressions (CALAMITA et alii,
2000 and references therein).
The crustal volume is assumed to be a continuum that
undergone stress and strain in geological time, as a
consequence it will deform as a fluid and the dynamic equation
that describe this behaviour is assumed to be the Navier-Stokes
equation:
∂ p 1 ∂ ⎛ ∂ v j ⎞ 2
Dvi
− + ? ⎜ ⎟ + ? ∇ vi
+ ?Xi
= ?
∂ x i 3 ∂ x ⎜
i x ⎟
⎝ ∂ j ⎠
Dt
where: p is the pressure; ? is the viscosity; vi and vj are the
2
velocity components; ∇ is the Laplacian; ? is the material
density; X is the body force per unit mass and Dvi/Dt is the
(Lagrangian) total time derivative of the velocity vi.
The interaction between the two layer of the modelled
volume could be described through the viscous-elastic Maxwell
body of which generic equation is:
s&
s
e & = +
2μ
2?
M
where: μM and ?M are the Maxwell rigidity and viscosity,
respectively, s is the stress; e& is the strain rate and s& is the
time derivative of the stress (RANALLI, 1995).
The brittle strength of the fault surface is described by the
Mohr-Coulomb’s law (for faults of neo-formation):
t = c + μf(s n – Pf)
and by the Amonton’s law (for reactivated faults):
t = μs(s n – Pf)
where: t is the shear stress; c is the coesion; μf is the friction
internal coefficient; s n is the normal stress; Pf is the pore fluid
pressure and μs is the friction coefficient of BYERLEE (1978).
This complex system of equations that describes the
geological model will be implemented through an appropriate
Finite Element Method, FEM, technique. The movement of
hangingwall and footwall blocks of the faults before and after
the rupture will be then numerically estimated. Through this
approach we expect to acquire more elements in order to test
the proposed geological inversion tectonics model and to
evaluate the reciprocal influence of each structures on the other.
These observations have implications in the definition of the
tectonic evolution of the Apennine chain and in the seismic
hazard assessment.
M
REFERENCES
BERRA F. & CARMINATI E. (2009) – Subsidence history from a
backstripping analysis of the Permo-Mesozoic succession
of the Central Southern Alps (Northern Italy). Basin
Research, doi: 10.1111/j.1365-2117.2009.00453.x.
BOCCALETTI M., CALAMITA F. & VIANDANTE M.G. (2005) – La
Neo-Catena litosferica appenninica nata a partire dal
Pliocene inferiore come espressione della convergenza
Africa-Europa. Boll. Soc. Geol. It, 124, 87-105.
BONCIO P., LAVECCHIA G. & PACE B. (2004) – Defining a
model of 3D seismogenic sources for Seismic Hazard
Assessment applications: the case of central Apennines
(Italy). J. Seismol., 8, 407-425.
80
BYERLEE J.D. (1978) – Friction of rocks. Pure Appl. Geophys.,
116, 615-626.
CALAMITA F., CELLO G., INVERNIZZI C. & PALTRINIERI W.
(1991) – Stile deformativo e cronologia della deformazione
lungo la traversa M. S. Vicino-Polverigi (Appennino
marchigiano esterno). Studi Geol. Camerti, vol. spec.,
1990, 69-86.
CALAMITA F., COLTORTI M., PICCININI D., PIERANTONI P.P.,
PIZZI A., RIPEPE M., SCISCIANI V. & TURCO E. (2000) –
Quaternari faults and seismicity in the Umbro-Marchean
Apennines (Central Italy): evidence from the 1997
Colfiorito earthquake. J.Geodyn., 29, 245-264.
CALAMITA F., ESESTIME P., PALTRINIERI W., SCISCIANI V. &
TAVARNELLI E. (2009a) – Structural inheritance of pre- and
syn- orogenic normal faults on the arcuate geometry of
Pliocene-Quaternary thrusts: examples from the Central
and Southern Apennine Chain. Ital. J. Geosci. (Boll. Soc.
Geol. It.), 128/2, 381-394.
CALAMITA F., PIZZI A., SCISCIANI V., SATOLLI S. & POMPOSO
G. (2009b) – Assetto tettonico e sismicità nell’Appennino
centrale. Riassunti del 28° Convegno GNGTS.
COLLETTINI C. & TRIPPETTA F. (2007) - A slip tendency
analysis to test mechanical and structural control on
aftershocks rupture planes. Earth Plan. Sci. Lett., 255, 402-
413.
MORRIS A., FERRIL A. & HENDERSON D. B. (1996) - Slip
tendency analysis and fault reactivation. Geology, 24 (3),
275-278.
PIZZI A. & GALADINI F. (2009) – Pre-existing cross-structures
and active fault segmentation in the northern-central
Apennines (Italy). Tectonophysics, 476, 304-319.
SATOLLI S. & CALAMITA F. (2008) – Differences and
similarities between the Central and Southern Apennines
(Italy): examining the Gran Sasso vs. the Matese-Frosolone
salients using paleomagnetic, geological and structural
data. J. Geophysical Res., 113, B10101. doi:
10.1029/2008JB005699.
RANALLI G. (1995) – Rheology of the Earth. Chapman e Hall,
second edition, 413 pp.

Key words: Cingoli anticline, cross section balancing, move
software, 3D modelling.
INTRODUCTION
The definition of the fracture system network in a carbonate
fault-related fold has relevant implications for fluid flow in the
subsurface. Quantitative characterization of fault and fracture
patterns has several industrial applications, such as modelling of
hydrocarbon migration, trapping, sealing, and production as well
as geothermal energy production, CO2 storage or pollutant
dispersion studies.
During the last years systematic studies have been carried out
in order to develop techniques for predicting fault and fracture
distribution in carbonate reservoir. Several approaches have been
developed to this aim: stochastic, geometrical/kinematical, which
includes restoration and forward modelling, curvature analysis,
and lately geomechanic modelling. Many of these techniques
require, as input data, a 3D-model of the fold. In order to
construct this model, it may be helpful to build a series of
balanced geological cross sections.
In this work, we study a fold anticline located in the foothills
of the Umbria-Marche Apennines, i.e., the Cingoli anticline. By
integrating the available literature data and those directly
collected in the field, a set of geological cross-sections across this
structure has been built to develop a viable and geometrically
correct 3D geological model of the most important structural
horizons. This model will be used as a base for future analysis of
the fracture patterns involving lithologically and mechanically
different formations by means of geomechanical models.
_________________________
3D-Modelling of the Cingoli Anticline
LORENZO PETRACCHINI (*) (**),DAVIDE SCROCCA (**), CHIARA D’AMBROGI (°),
MARCO ANTONELLINI (*) & ANDREA BILLI (**)
(*) Dipartimento di Scienze della Terra e Geoambientali, Università Alma Mater
Studiorum di Bologna
lorenzo.petracchini2@unibo.it, lorenzo.petracchini@igag.cnr.it ,
m.antonellini@unibo.it
(**) IGAG- CNR, davide.scrocca@igag.cnr.it
(°) ISPRA, Servizio Geologico d’Italia/Dipartimento Difesa del Suolo,
chiara.dambrogi@isprambiente.it
This work has been supported by Independent Energy Solutions S.r.l..
81
GEOLOGICAL SETTING AND TECTONIC EVOLUTION
The Cingoli anticline is located a few kilometres to the East of
the Umbria-Marche fold and thrust belt in the central Apennines.
It is formed by the typical pelagic Umbria-Marche sequence
overlaying the shallow water carbonate of the Calcare Massiccio
Fm, which is outcropping in the core of the fold. The anticline
has a NW-SE axial trend in its northern portion whereas, in the
South, it turns to a N-S orientation. The anticline is confined to
the West by the Apiro-San Severino thrust, which brings the
Aliforni syncline above the western limb of the Cingoli structure.
The northern and the southern terminations of the Cingoli
anticline are characterized by E-W transpressive sinistral highangle
faults and by N20° dextral transpessive faults respectively
(DEIANA et alii, 2002).
The frontal thrust is buried by Lower Pliocene deposits, which
lay unconformably upon the carbonate sequence and the pre-
Pliocene sediments. The eastern limb of the Cingoli anticline is
characterized by a back-thrust of Upper Messinian-lower
Pliocene age, considered by CALAMITA et alii (1990) a
reactivation of a synsedimetary fault.
The anticline is characterized by Apennine-oriented and
transverse faults. The latter break the anticline structure and they
usually have a vertical displacement but weak or null horizontal
offset (CIANCETTI &NANNI, 1989).
Finally, the Cingoli area is cut by pre-orogenic faults related
both to the early Jurassic rifting (N-S) and to the Miocene prethrusting
normal faults. These pre-thrusting tectonic elements
represent fundamental features for the tectonic evolution of the
area.
The compressive deformation started after the deposition of
the Gessoso-solfifera Fm (Messinian), and it was followed by
subsidence leading to the deposition of transgressive lower
Pliocene clay deposits. After this period the area was deformed
within the Apennine fold and thrust belt (DEIANA et alii,2002;
CIANCETTI &NANNI, 1989).
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SESSIONE 3
Fig. 1 – 3D dataset visualization in Move©.
DATA, GEOLOGICAL CROSS SECTIONS AND 3D
MODELLING
Several datasets, related to both surface and subsurface
geology, have been collected and integrated. All available data
have been geo-referenced. The data include the following:
� Geological map at 1:10000 scale (CARG Project);
� C.T.R. 1:10000;
� Attitude set provided by the Regione Marche –
Servizio Ambiente e Paesaggio
P.F. Informazioni Territoriali ed Ambientali e
Beni Paesaggistici;
� Satellite images downloaded from
http://maps.google.it/;
� Structural maps;
� DEM of the 291/292/301/302 geological sheets with
a 40m cell resolution – gently provided by ISPRA;
� Public and proprietary seismic reflection profiles.
In addition, we conducted detailed structural surveys in
relevant areas along the cross section traces.
All data have been integrated in 3D Move (© Midland Valley
Exploration), a 3D modelling software able to build geological
cross sections, restore volume and to perform forward modelling.
Through the data collected and those extrapolated from the
literature several geological cross sections, parallel to the tectonic
transport direction, have been constructed in 3D Move.
All surface data (attitude of the strata, top formation outcrops,
faults, etc.) and the geological cross sections have been used to
build a consistent 3D model of the Scaglia, Fucoidi and Calcare
Massiccio Formations.
This model has been useful to analyse the fracture sets with
respect to structural position in the fold. The analysis of the
fractures suggests that the fracture pattern and orientation is
strictly connected to flexural slip in the two limbs of the
anticline.
82
ACKNOWLEDGEMENTS
Midland Valley Exploration is grateful acknowledged for
making available the Move software (ASI – academic Software
Initiative).
We are kindly grateful to ISPRA and to Regione Marche -
Servizio Ambiente e Paesaggio, P.F. Informazioni Territoriali ed
Ambientali e Beni Paesaggistici for providing useful dataset.
We also thank Roberto Bencini, Giuseppe Vico and Elio
Bianchi for the useful discussions.
REFERENCES
CALAMITA F., CELLO G., INVERNIZZI C. & PALTRINIERI W. (1990)
– Stile strutturale e cronologia della deformazione lungo la
traversa M.S. Vicino – Polverii (Appenino marchigiano
esterno). Studi Geologici Camerti, Vol. Spec., 1990, 69-86.
CIANCETTI G. & NANNI T. (1989) – Note sulla geologia
dell’anticlinale di Monte Acuto di Cingoli (Marche). Boll.
Soc. Geol. It., 108, 553-564.
DEIANA G., CELLO G., CHIOCCHINI M., GALDENI S., MAZZOLI S.,
PISTOLESI E., POTETTI M., ROMANO A., TURCO E. & PRINCIPI
M. (2002) – Tectonic evolution of the external zones of the
Umbria-Marche Apennines in the Monte San Vicino-Cingoli
area. Boll. Soc. Geol. It., vol. spec. 1, 229-238.

Key words: Integration, Petrel, seismic to simulation, static
model, uncertainty.
PETREL EXPLAINED
Petrel can be defined as an integrated software platform
aimed to realize the entire workflow commonly referred as
"seismic to simulation" in the oil & gas jargon.
This means that Petrel can act as a supporting tool to take
decisions, interpret results, quantify reserves and take in account
risks and uncertainties in all the phases in which oil & gas
companies are involved, in respect of understanding the reservoir,
modeling the subsurface and the presence and flow of fluids and
eventually rank and evaluate the economic feasibility of the
prospects.
Fig. 1 – The integrated 3D canvas of Petrel.
There are at least four points worth to mention to understand
this approach:
_________________________
Petrel as an open and unified platform to accurately model the
subsurface and its uncertainties, beyond the oil industry
(*) Schlumberger Italiana, aromi@slb.com
(Petrel, ECLIPSE, VISAGE, Petromod are mark of Schlumberger)
http://www.slb.com
ALESSANDRO ROMI (*)
83
- the first one is the seamless integration: Petrel provides a
unique common multi-domain workspace which increases
collaboration at all the levels, at any scale of study. At the same
time, this reduces data redundancy and accelerates the outcome of
any project, also because the intuitive and consistent interface
looks the same for every process. Integration is not ending within
Petrel but keeps on linking dynamic and geo-mechanic simulation
(ECLIPSE and VISAGE), petroleum systems analysis
(Petromod ) and further more;
- the second one is the "openness": Petrel is based on a
"software development platform" which allows virtually anyone
to add any piece of functionality at any time to extend Petrel
capabilities and accomplish any specific workflow. This is true
for oil & gas companies, for universities performing research
projects and for competitors using Petrel as a platform to leverage
their product;
- the third one is that Petrel is enabled for uncertainty
analysis: since a model is just a simplification of the reality and
interpretations are always subjective, Petrel is dealing with this
inevitable uncertainty by using an "engine" capable to produce
multiple and equi-probable realizations of the base case model, at
any step of the workflow. In a "reserve estimation" language, this
means more predictability and quantitative approach for the risk
analysis;
- the fourth one is the "leading-edge" technology: patented
algorithms, innovative solutions, industry-recognized
technologies are the result of the enormous R&D investment
inside Petrel. This effort helps to increase the accuracy in
characterizing and modeling even complex reservoirs, mainly
now that "easy oil" has gone.
THE DIFFERENT FLAVORS OF PETREL
This is not the whole story: Petrel is targeting not only the
"conventional oil" industry.
There are either emerging and promising sectors like the
unconventional oil & gas and the CO2 sequestration and storage,
and others with a long story but nowadays getting more and more
attention like the geothermal industry, the gas storage business
and, not least, the academic world.
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SESSIONE 3
All of them represent suitable subjects more than likely to
welcome Petrel approach and take advantage of all the
capabilities described above, whenever the purpose is to model
the subsurface, regardless of the business context.
Petrel seamless integration with other software suites
dedicated to specific tasks (like ECLIPSE** and VISAGE**) and
the capability to be extendable with customized functionalities
offer a complete solution to a large range of industry challenges.
Fig. 2 – Petrel is an open and extendable solution.
THE SCOPE OF WORK
This presentation is aimed to demonstrate, first of all, what
Petrel is and its strength of representing a single and unified
application to produce reliable shared earth models, as
recognized inside the oil & gas community.
But it is also willing to show how Petrel, alone or coupled
with other ad-hoc applications, can be the ideal tool also outside
the conventional oilfield environment and how is virtually open
to any input in very different environments or contexts.
Indeed, this is the natural consequence of focusing on
innovation from the very beginning.
As a proof of fact, relevant case histories and examples will
be shown to describe the application of Petrel in various industry
and academic benchmarks.
84

Key words: CO2 sequestration, magnesite, serpentine.
INTRODUCTION
Anthropogenic greenhouse gas emissions may be offset by
sequestering carbon dioxide (CO2) through the carbonation of
magnesium silicate minerals (i.e., Mg2SiO4 olivine,
Mg3Si2O5(OH)4 serpentine, CaSiO3 wollastonite) to form
magnesium carbonate minerals (i.e., MgCO3 magnesite,
MgCa(CO3)2 dolomite, CaCO calcite, FeCO siderite,
NaAl(CO)(OH) dawsonite). This technology attempts to mimic
natural low-temperature alteration (carbonation) of widespread
silicate rocks (i.e., peridotite, serpentinite, basalt) that trap safely
CO2 over geological times. Southern Tuscany presents more than
3 Gt of magnesite - equivalent to 1,6 Gt of trapped CO2 – that
have been formed in the past thought the carbonation of
serpentinite (BOSCHI et alii, 2009). In addition, extensive
outcrops of unaltered serpentinites (Ligurian Units) as well as
deeper occurrences are found at the base of, or embedded in,
dominantly argillitic units, largely consisting of low-permeability
shales and marls. Considering the outcropping rocks, exposed in
Tuscany over an area of about 230 km 2 , a mineralogical
sequestration up to 100 Gt of CO2 is theoretically possible -
equivalent of about 200 years of Italian GHG emissions. Even
assuming a lower performance of mineralogical GHG
sequestration in Tuscan ophiolite, it is clear that the potentiality
of this technology is very interesting. Here, we present a 3D
geological reconstruction of a continuous serpentinite layer,
buried under 300 m of argillitic formations, at Gabbro (Southern
Tuscany). This reconstruction is the first important step to count
realistically the potentiality of an in situ CO2 sequestration in
Tuscany.
We selected the study area from all the lithologic and
stratigraphic wells data extracted from The Italian National
Geothermal Database, managed at our Institute
(http://geothopica.igg.cnr.it/). The database contains data for
3193 wells and 586 thermal springs for the whole Italian
territory, and, in particular, 770 wells from Tuscany.
_________________________
3D geological reconstruction of serpentinite bodies in Tuscany:
insights for in-situ CO2 sequestration
(*) CNR - Istituto di Geoscienze e Georisorse, e.trumpy@igg.cnr.it,
c.boschi@igg.cnr.it, a.dini@igg.cnr.it
EUGENIO TRUMPY (*), CHIARA BOSCHI (*) & ANDREA DINI (*)
85
GEOLOGICAL SETTING
In the study area, the Ligurian Units are represented by a
complex stacking sequence, made up by several tectonic units
that include ophiolites, sedimentary covers (cherts, limestones
and shales), and turbiditic sediments. The main exposed
ophiolitic bodies, dominated by serpentinites with minor gabbros
and basalts, form an ENE trending, discontinuous outcrop
alignment (from Bolgheri to Casole d'Elsa). The Ligurian units
lie tectonically above a stack formed by units of continental
affinity (Tuscan units). The latter (Tuscan Nappe and the
Palaeozoic–Triassic metamorphic basement) crop out extensively
to the south of the study area, while in the Gabbro area they are
buried at a depth of about 1300–1500 m below the sea level, as
indicated by the geothermal exploratory wells. Owing to this
geological setting, ophiolities in the Gabbro area are buried at
several hundred meters depth and are potentially exploitable for
in-situ CO2 sequestration.
Wells containing ophiolites were selected from the database,
and lithological, stratigraphical, as well as temperature data were
retrieved. The result of these queries provided a map showing the
most suitable place that follow the main requirements to have
efficient and safe carbonation: temperature around 150 °C,
moderate depth and argillitic envelope. Some wells provide these
requirements displaying serpentinite/gabbros/basalt embedded in
argillitic units at a ranging depth from 150 m to 400 m, and a
temperature of about 80°-170 °C. The peculiarity of the study
area (Fig. 1) is the proximity to the Larderello Geothermal field
with its anomalous heat flow that allows reaching significant
temperature also at relatively shallow depth, enhancing
spontaneously the reaction of carbonation in presence of CO2.
3D GEOLOGICAL RECONSTRUCTION
The data from the selected wells have been used as input data
for the 3D geological reconstruction, that has been performed
using a 3D geological modeling software, “3DGeomodeler”. This
software was developed by BRGM and Australian Intrepid
Geophysics. Input data could be geological maps, geological
cross-sections, borehole, as well as geophysical data (i.e.
gravimetric and magnetic data). 3DGeomodeler uses the implicit
surfaces to model the geological surfaces; this method is based
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SESSIONE 3
Fig. 1 – Study area map.
on the potential field theory, where a set of smoothly curving,
sub-parallel geological surfaces in 3D spaces con be seen to be
analogous to a set of iso-potential surfaces of a scalar (potential)
field (MC INERNEY et alii, 2005). Once the geological model is
ready the result block diagram can be visualized, as horizontal
slices or vertical cross-sections.
CONSIDERATIONS AND DISCUSSIONS
Our resulting 3D geological model highlights the presence of
well-confined serpentinite bodies with lateral continuity that are
potentially exploitable for in-situ CO2 sequestration. Our ongoing
research will continue with a detailed petrographic and
structural studies of ophiolites exposed at surfaces and cored by
exploratory wells in order to evaluate the permeability of these
rocks.
REFERENCES
BOSCHI C., DINI A., DALLAI L., GIANELLI G. & RUGGIERI G.,
(2009) - Enhanced CO2-mineral sequestration by cyclic
hydraulic fracturing and Si-rich fluids infiltration into
serpentinites at Malentrata (Tuscany, Italy). Chem. Geol.,
265, 209–226 - DOI:10.1016/J.CHEMGEO.2009.03.016.
MC INERNEY P., GUILLEN A., COURRIOUX G., CALCAGNO P. &
LEES T. (2005) - Building 3D Geological Models Directly
from the Data ? A new approach applied to Broken Hill,
Australia. Digital Mapping Techniques.
86

SESSIONE 4
Processi tettonici, magmatici e metamorfici nella
crosta continentale profonda e nel mantello
sub-continentale del sistema Africa-Europa
CONVENERS
Eugenio Piluso (Università della Calabria)
Giovanna Rizzo (Università della Basilicata)
87
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SESSIONE 4
Peridotite xenoliths from Ethiopia: inferences on mantle processes
from Plume to Rift settings
Key words: CFB, mantle dynamics, mantle plume, mantle
xenoliths, metasomatism, rift.
A comprehensive petrological study has been carried out on
Ethiopian mantle xenoliths entrained in Neogene-Quaternary
alkaline lavas both overlying the Continental Flood Basalt (CFB)
area (Dedessa River – Wollega Region, Injibara – Gojam
Region) and from southern Main Ethiopian Rift (MER – Mega,
Sidamo Region) in order to investigate the mantle evolution from
plume to rift settings.
Mantle xenoliths from the plateau area (Injibara, Dedessa
River) range in composition from spinel lherzolite to harzburgite
and olivine websterite, showing P-T equilibration conditions in
the range 1.3–0.9GPa/1050–950°C.
These xenoliths show flat chondrite(ch)-normalized bulk-rock
REE patterns, with only few LREE-enriched samples (LaN/YbN
up to 7) in the most refractory lithotypes. Clinopyroxene (cpx)
REE patterns are mostly LREE depleted (LaN/YbN down to 0.2)
or enriched (LaN/YbN up to 4.4). Sr-Nd isotopes on separated cpx
mainly show compositions ( 87 Sr/ 86 Sr < 0.7030; 143 Nd/ 144 Nd >
0.5132) approaching the Depleted Mantle end-member, or
displaced ( 87 Sr/ 86 Sr 0.7033-0.7034; 143 Nd/ 144 Nd 0.5129-0.5128)
toward the Enriched Mantle components which characterise the
Afar plume signature and the related Ethiopian Oligocene CFBs;
3 He/ 4 He ratios in olivines range from 6.6 to 8.9 R/Ra, slightly
higher than those from other African mantle xenolith occurrences.
These characteristics suggest that most xenoliths reflect
complex asthenospere/lithosphere interactions due to
refertilisation processes by mafic subalkaline melts that infiltrated
and reacted with the pristine peridotite parageneses ultimately
leading to the formation of olivine-websterite domains (Fig. 1a
and b).
On the other hand, mantle xenoliths from southern MER
(Mega) consist of spinel lherzolite to harzburgites showing
various degree of deformation and recrystallization, coupled with
a wider range of P-T equilibration conditions, from 1.6±0.4
GPa/1040±80°C to 1.0±0.2 GPa/930±80°C. Bulk rock REE
patterns show generally flat HREE ranging from 0.1 x ch in
_________________________
LUIGI BECCALUVA (*), GIANLUCA BIANCHINI (**), ROBERT MARK ELLAM (°), CLAUDIO NATALI (*),
ALESSANDRO SANTATO (*), FRANCA SIENA (*) & FIN STUART (°)
(*) Dipartimento di Scienze della Terra, Università di Ferrara,
bcc@unife.it
(**) Istituto di Geoscienze e Georisorse - CNR, Sezione di Pisa
(°) Scottish Universities Environmental Research Centre, East Kilbride,
Glasgow, UK
88
harzburgites up to 2 x ch in fertile lherzolites, and are variably
enriched in LREE, with LaN/YbN up to 42 in the most refractory
lithologies.
The constituent clinopyroxenes have flat HREE distribution
and LaN/YbN between 0.1 and 55, in general agreement with the
respective bulk rock chemistry. Sr-Nd-Pb on separeted
clinopyroxenes are 87 Sr/ 86 Sr 0.7022-0.7031, 143 Nd/ 144 Nd 0.5130-
0.5138, 206 Pb/ 204 Pb 18.38-19.34 for lherzolites, and 87 Sr/ 86 Sr
0.7027-0.7033, 143 Nd/ 144 Nd 0.5128-0.5130, 206 Pb/ 204 Pb 18.46-
18.52 for harzburgites, thus spanning in composition between the
DM and HIMU mantle end-members; the helium isotopic
composition varies between 7.1 to 8.0 R/Ra, closely comparable
with the xenoliths from the plateau area.
Regional comparison shows that HIMU-like alkali-silicate
melt(s) were among the most effective metasomatising agent(s) in
mantle sections beneath southern MER (Fig. 1c) as well as along
the Arabian rifted continental margins and the whole East
African Rift System (EARS).
The decidedly different types of metasomatic agents recorded
in Ethiopian mantle xenoliths from the CFB area and the Rift
systems, clearly reflect distinct tectonomagmatic settings, i.e. the
plume-related subalkaline magmatism (Fig. 1a and b) and the riftrelated
alkaline volcanism which extends far beyond the influence
of the Afar plume (Fig. 1c).
REFERENCES
BECCALUVA L., BIANCHINI G., NATALI C. & SIENA F. (2009) -
Continental Flood Basalts and Mantle Plumes: a Case Study
of the Northern Ethiopian Plateau. J. Petrol., 50, 1377-1403.

CONGRESSO SGI - ABSTRACTS
Fig. 1 – Schematic cross-sections illustrating the tectonomagmatic evolution of the Afro-Arabian system from Oligocene to Present. In (a) the Afar plume impinged
the Afro-Arabian lithosphere generating the Oligocene Northern Ethiopia-Yemen CFBs from a thermally and compositionally zoned plume head (modified after
BECCALUVA et alii, 2009). Lithospheric mantle sections were widely rifertilized by plume-related melts (similar to LT and HT1 tholeiites) as evidenced by mantle
xenoliths exhumed by alkaline quaternary lavas at Injibara and Dedessa River. In (b) is shown the Neogene-Quaternary evolution characterised by a generalized
extensional regime and ultimately leading to the development of MER and the oceanic opening of the Red Sea and Gulf of Aden. This is accompanied by the gradual
vanishing of the Afar plume head testified by the alkaline-transitional affinity of both Miocene shield volcanoes on the Northern Ethiopian Plateau, and the Neogene-
Quaternary transitional to alkaline volcanism of the Afro-Arabian rift system. In (c) is shown an E-W section across the southernmost part of the present day MER.
Pliocene-Quaternary alkaline lavas at the eastern border of MER entrained lithospheric 2 mantle xenoliths which were metasomatised by HIMU-like alkali-silicate
melts: this reflects the prevalent geochemical signature of the metasomatising agents of the Afro-Arabian rift system as well as of the Northern African Plate.
89
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SESSIONE 4
Geodynamic control on orogenic and anorogenic magmatic cycles in
the Cenozoic evolution of the Western Mediterranean
LUIGI BECCALUVA (*), GIANLUCA BIANCHINI (**), CLAUDIO NATALI (*) & FRANCA SIENA (*)
Key words: Anorogenic magmas, Cenozoic Mediterranean
volcanism, mantle dynamics, orogenic magmas, roll-back
subduction.
The genetic relationships between orogenic and anorogenic
magmatic cycles have been investigated in two Cenozoic case
studies of the Western Mediterranean area: 1) in Sardinia the
orogenic magmatism (38 – 12 Ma) is followed by the anorogenic
volcanism, mostly since about 6 Ma; 2) in Southern Spain the
anorogenic volcanism follows the orogenic cycle (20 – 6 Ma)
after a gap of 0 – 4 Ma in the Calatrava and Tallante districts.
For both regions the older orogenic magmatism appears to be
related to a single subduction process of the Ionian oceanic
lithosphere, which developed diachronously since Middle-Late
Eocene, beneath the Paleo-European-Iberian continental margin,
and migrated southeastwards with time up to the present position
in the Eolian-Calabrian Arc and the Betic-Alboran regions (Fig
1A).
Relics of subducted lithosphere are geophysically recorded as
nearly-vertical single bodies down to 500 km, flattening for
several hundreds kilometres under the Tyrrhenian-Sardinia and
Southern Iberian margin, respectively.
These relics of subducted slabs, which pond over large areas
of the Mantle Transition Zone, appear to play a significant role
also in the genesis of the younger anorogenic magmas, whose
major volcanic fields lay above the frontal part of the subducted
slab where convective instabilities and upward mantle flow
components are geophysically recorded and supported by
laboratory and 3D numerical models.
Consequently, convective instabilities, generated as a dynamic
response at the periphery of a retreated subducted slab and
involving localized mantle upwellings and rising of hotter
metasomatising agents, could have been fundamental factors in
triggering partial melting in the overlying upper
mantle/lithosphere.
Due to effective slab roll-back and inter-arc extension in both
Eolian-Tyrrhenian and Betic-Alboran regions, the magma sources
of the previous orogenic cycles are completely replaced by
_________________________
(*) Dipartimento di Scienze della Terra, Università di Ferrara,
bcc@unife.it
(**) Istituto di Geoscienze e Georisorse-CNR, Sezione di Pisa
90
“fresh” mantle diapirs from which anorogenic magmas will be
generated.
The widespread HIMU signature of the Mediterranean
anorogenic magmatism, particularly evident in the Calatrava
volcanism, is in agreement with the model above, since the
HIMU mantle end-member is classically interpreted as the result
of long-term recycling of oceanic basalts/gabbros (or their
eclogitic equivalents) within the mantle via ancient (Pre-
Paleozoic) subduction.
Similarly, the geochemical component EMI, strongly
represented in the Sardinian anorogenic lavas, would require the
involvement of lower crust lithologies within the mantle sources,
resulting from either ancient subduction or delamination of
previously thickened continental crust.
In this model, the on-going subduction processes of the
Mediterranean chains do not provide chemical “ingredients” to
the mantle sources of the anorogenic magmas, but represent
fundamental factors that trigger magma-genesis remobilizing old,
deep and very fertile mantle domains (Fig. 1B and C) .

CONGRESSO SGI - ABSTRACTS
Fig. 1 – (A) Tectonomagmatic sketch map of the Western Mediterranean. Lithospheric cross-sections beneath the Betic-Alboran region (B) and the Eolian-Calabrian
arc (C). Legend: 1 - Lithosphere. 2 - Balearic and Tyrrhenian interarc basins. 3 - Late Eocene-Miocene orogenic volcanism and related mantle sections. 4 - Late
Miocene-Quaternary anorogenic volcanism and related mantle sections. 5 - Inferred boundary of the subduction system and related orogenic volcanism at different
ages; open triangles refer to slab detachments/windows. 6 - Compressional thrust front of the Alps, Betic Cordillera and Apennines-Maghrebian Chain. 7 - Mantle
peridotite massifs of Ronda and Beni Bousera. 8 - Fluid components rising to the lithosphere and metasomatising anorogenic magma sources. 9 - Mantle flow
components and convective instabilities triggered at the front and edges of the subducted slabs.
2
91
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SESSIONE 4
Crustal structure of Tolfa domes complex (northern Latium – Italy)
inferred from receiver functions analysis: an interplay between
tectonics and magmatism
MAURO BUTTINELLI(*) (°),IRENE BIANCHI (*), MARIO ANSELMI (*),
(*
CLAUDIO CHIARABBA )&DONATELLA DE RITA (°)
Key words: Domes complex, northern Latium, receiver functions
analysis.
The Tolfa-Cerite volcanic district developed along the
Tyrrhenian passive margin of central Italy, as part of magmatic
processes started during the middle Pliocene and still poorly
known, since the absence of information on the deep crustal
structure and geometry of the intrusive bodies.
After the onset of extension in the Tyrrhenian domain (Late
Miocene), the emplacement of the Tolfa and Ceriti intrusive
bodies occurred in a general back-arc regime, at a low stretching
rate. Lithospheric discontinuities and normal faults, located at the
edge of Mio-Pliocene basins, were used as preferential pathways
for the rising of magmatic masses from the mantle to the surface.
We used teleseismic recordings at the TOLF and MAON
broad band station of the INGV seismic network (located
between the Argentario promontory and Tolfa-Ceriti dome
complexes) to image the main seismic velocity discontinuities by
receiver function analysis (RF's). The analysis of data recorded at
a temporary seismic network, deployed around the Tolfa domes
complex, allows us to achieve a pseudo-3D model of the crustal
structure beneath the intrusive complex.
The analysis of these data show the Moho at a depth of 23 km
and an unexpected velocity decrease between 12 and 18 km
underneath the Tolfa domes complex, consistent with a slight
dropdown of the Vp/Vs ratio, and imputable to the regional
thermal anomaly induced by the opening of the Tyrrhenian sea.
Above this low Vs layer, we find some interesting features
corresponding to:
- a low Vs shallow and 2 km thick layer of Liguride and Plio-
Pleistocene units (z = 0-2 km of depth)
- a high Vs 4-5 km thick anisotropic layer of limestones (z =
2-7 km of depth)
- a very high Vs (3.8 km/s) 4 km thick layer probably
_________________________
(*) Istituto Nazionale di Geofisica e Vulcanologia (INGV), sezione Roma1,
UF geochimica dei fludi, stoccaggio geologico e geotermia,
mauro.buttinelli@ingv.it
(°) Università degli Studi Roma3, Dipartimento di Scienze Geologiche
92
corresponding to the metamorphic basement.
The analysis of the geometry of the velocity changes between
these layers (from the surface to the bottom of metamorphic
basement), also yield evidence of crustal block tilting, due to the
development of the eastern continental passive margin of the
Tyrrhenian sea.
Comparison of RF’s Tolfa domes complex models with
MAON station data also led to important considerations
confirming the initial evolutive phase of the Tyrrhenian sea
opening, in association with the first occurrences of intrusive
magmatism in these areas.

Key words: Calabrian Peloritani Orogen, Mediterranean
geodynamics, PT pseudosection, tectono-metamorphic
evolution.
GEOLOGICAL SCENARIO
The Calabrian orogenic segment is mostly constituted by
remnants of the original southern European Hercynian chain
reworked during the Alpine-Apennine orogeny, which locally
generated exclusive Alpine metamorphic complexes as well as
weakly to pervasively overprinted basement blocks. This
evolution led to the formation of a composite terrane (i.e.
Calabride Composite Terrane - CCT) constituted by basement
rocks presently merged in several Hercynian or possibly older
sub-terranes, locally overprinted by the different stages of the
Alpine metamorphic cycle (PEZZINO et alii, 2008).
In this scenario, several questions are still debated about the
geodynamic history of this southern Alpine sector chain such as
the unclear correlation between Northern- and Southern-
Calabride Composite Terranes. The former is characterised by
Europe- and Africa-verging tectonic transport and by the
presence of Alpine ophiolitic units, while the latter by an
exclusive Africa-verging tectonic transport and by the absence of
ophiolitic units. Furthermore, up to now, available data have not
allowed any reliable correlation among the various tectonic units
which compose the Southern Calabride Composite Terrane
(SCCT), as revealed by the PT trajectories of the constituting
tectono-metamorphic units. The present contribution has the aim
to compare the tectono-metamorphic evolution of the Serre and
Aspromonte Massifs, presently juxtaposed within the present-day
framework of the SCCT.
GEOLOGICAL FRAMEWORK
The SCCT is constituted by the Serre and Aspromonte
_________________________
The composite framework of the southern sector of the
Calabria Peloritani Orogen
ROSOLINO CIRRINCIONE (*), ELOISA DE VUONO (**), EUGENIO FAZIO (*), PATRIZIA FIANNACCA (*),
GAETANO ORTOLANO (*), ANTONINO PEZZINO (*) & ROSALDA PUNTURO (*)
(*) Dipartimento di Scienze Geologiche, Università degli studi di Catania,
ortolano@unict.it
(**) Dipartimento di Scienze della Terra, Università degli studi della
Calabria
93
Massifs and by the Peloritani range in Sicily.The Serre Massif
occupies the northern sector of the SCCT and represents a nearly
complete preserved Hercynian crustal section, consisting of lower
crustal granulites, middle crustal granitoids and upper crustal
paragneisses and phyllites.
According to ACQUAFREDDA et alii, (2006, 2008) and ANGÌ et
alii, (2010), the Serre Massif experienced a multistage
metamorphism consisting of an orogenic cycle waning at the time
of the emplacement of late- to post-tectonic granitoids, which was
responsible in turn for a quasi-static thermal metamorphic
overprint. By contrast, according to CIRRINCIONE et alii (2008),
the adjoining Aspromonte Massif is characterised by an Alpine
derived nappe-pile structure composed by the superposition of
three tectonic units characterised by different tectonometamorphic
histories. The deepest one (i.e. Madonna di Polsi
Unit) is the result of one single Alpine metamorphic cycle,
characterised by an early HP/LT stage, evolving to a late
mylonitic shearing event. The overlying unit (i.e. Aspromonte-
Peloritani Unit) is composed by Hercynian basement rocks in
which mineralogical assemblages were locally overgrown by the
same late Alpine mylonitic shearing parageneses as identified in
the deepest unit. Finally, according to GRAEßNER &SCHENK
(1999), the uppermost unit (i.e. Stilo Unit) of the tectonic pile is
exclusively characterised by a Hercynian HT/LP metamorphism
producing a sequence of metamorphic zones from chlorite to
sillimanite–muscovite, passing through the biotite-garnet and
staurolite–andalusite isograds.
GEOLOGICAL MODELLING PERSPECTIVES
The integrated presentation of inferred petrological and
microstructural PT estimates here presented, suggests a first
proposal of geology review based on a geodynamic model where
the Southern Calabride Composite Terrane is characterised by the
presence of both mono- and poly-orogenic chain sectors presently
framed within the same belt. According to PEZZINO et alii,
(2008), the Alpine geodynamic evolution of the Aspromonte
Massif can be defined indeed as the result of a prograde crustal
thickening phase beneath the European plate, which was followed
by an Africa-verging late-Alpine exhumation along a deep-seated
mylonitic shear zone, responsible for both the mylonitic overprint
affecting the early-Alpine rocks of the deepest unit as well as for
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SESSIONE 4
the local Alpine reworking of the Hercynian basement rocks.
Conversely, the Serre Massif seems to have been unaffected by
the Alpine-Apennine reworking, except for its final exhumation
stages. The Serre Massif is indeed the result of a single Hercynian
type metamorphic cycle, characterised by a multistage orogenic
evolution consisting of a prograde thickening stage, followed by a
late-Hercynian retrograde shearing evolution, which produced the
mylonitic rocks partly recovered by the subsequent late- to posttectonic
intrusion of the granitoid bodies, which gave rise to a
quasi-static thermal metamorphic overprint. This integrated data
presentation can be framed within a new geodynamic scenario
where the SCCT is the result of the juxtaposition of an internal
(i.e. the Serre Massif) and an external (i.e. the Aspromonte
Massif) sectors belonging to the southern European Alpine
margin along deep seated transcurrent faults which probably
played a key role, since Oligocene, in shaping the present-day
framework of this Alpine sector chain.
REFERENCES
ACQUAFREDDA P., FORNELLI A., PAGLIONICO A. & PICCARRETA
G. (2006) - Petrological evidence for crustal thickening and
extension in the Serre granulite terrane (Calabria, southern
Italy). Geol. Mag.,143 (2), 145-163.
ACQUAFREDDA P., FORNELLI A., PICARRETA G. & PASCAZIO A.,
(2008) - Multi-stage dehydrationdecompression in the
metagabbros from the lower crust rocks of the Serre
(southern Calabria, Italy). Geol. Mag.,145 (3), 397–411.
ANGÌ G., CIRRINCIONE R., FAZIO E., FIANNACCA P., ORTOLANO
G. & PEZZINO A., (2010) - Metamorphic evolution of
preserved Hercynian crustal section in the Serre Massif
(Calabria-Peloritani Orogen, southern Italy). Lithos,115 (1-
4), 237-262.
CIRRINCIONE R., ORTOLANO G., PEZZINO A. & PUNTURO R.,
(2008) - Poly-orogenic multi-stage metamorphic evolution
inferred via P–T pseudosections: an example from
Aspromonte Massif basement rocks (Southern Calabria,
Italy). Lithos,103, 466–502.
GRAEßNER T. & SCHENK, V., (1999) - Low-pressure
metamorphism of Palaeozoic pelites in the Aspromonte,
southern Calabria. Constraints for the thermal evolution in
the Calabrian cross-section during the Hercynian orogeny.J.
Met. Geol., 17, 157-172.
PEZZINO A., ANGÌ G., FAZIO E., FIANNACCA P., LO GIUDICE A.,
ORTOLANO G., PUNTURO R., CIRRINCIONE R. &
DEVUONO E.,
(2008) - Alpine metamorphism in the Aspromonte Massif:
implications for a new framework for the southern sector of
the Calabria-Peloritani Orogen (Italy). Int. Geol. Rev., 50,
423–441.
94

Nature of the upper mantle and metasomatic processes on Eastern
Anti-Atlas Moroccan
Key words: Alkaline complex, Moroccan, Mössbauer
spectroscopy, nephelinites, upper mantle.
The Pleistocenic anorogenic Jbel Saghro alkaline complex
was emplaced close to the eastern edge of the Moroccan Anti-
Atlas. Within the northern part, two types of nephelinite were
recognized (IBHI et alii, 2002): the first one (olivine-rich
nephelinite) constitutes the main volcanic mass the South-atlasicfault,
where the volcanism had been active at least during 2 Ma,
between 9.6 and 7.5 +/- 0.1 Ma (BERRAHMA et alii, 1993). The
second group outcrops in the North (Foum El Kouss). It is
represented by pyroxene nephelinites which are younger since the
measured ages are of 2.9 +/- 0.1 Ma, and bears carbonatitic
xenoliths and metasomatised peridotite xenoliths (IBHI &NACHIT,
1999).
Considering the small volume of erupted magmas, the Jbel
Saghro volcanism is similar to that of ‘low-volcanicity rifts’
characterised by fissure-fed volcanic activity with small eruptive
volumes of relatively undifferentiated magmas, and a wide range
of chemical compositions from tholeiitic to extremely alkaline
(BARBERI et alii, 1982, BECCALUVA et alii, 1998).
According to Hart’s textural nomenclature of peridotites, the
peridotite xenoliths contained in the nephelinites of Jbel Saghro
are all porphyroclastic with a granuloblastic tendency.
They have a modal composition relatively homogenous which
situates them in Streckeisen's classification near the limit of the
field of lherzolites and that of harzburgites. Two main enclave
types have been determined by their petrography:
- The first one does not contain any trace of destabilisation. It
is characterized by an assemblage of minerals in equilibrium and
with composition typical of mantle lherzolites : olivine (Fo90 -
Fo91), orthopyroxene (En90 - En92), diopside (Ca46 – 59 Fe05 -
07 Mg43 - 47) and spinelle (Mg/(Mg+Fe) = 0.82 and Cr/(Cr+Al)
= 0.10), which can be considered as primary.
- The second one, which occurs only in pyroxene nephelinites,
is characterized by the presence of millimetric and pale-green
reactional aggregates which are scattered throughout the sample
and filled by a microgranular mineral assemblage. These
_________________________
ABDERRAHMANE IBHI (*), HASSANE NACHIT (*), AHMED AIT TOUCHNT (*), EL HASSAN ABIA (*),
CARMELA VACCARO (**) & ELENA MARROCCHINO (**)
(*) 1LPMM, Ibn Zohr University, Agadir, Morocco,
ibhiabderrahmane@yahoo.fr
(**) Dipartimento di Scienze della Terra - Università di Ferrara
Lavoro eseguito con il contributo finanziario CNRST-CNRI
95
aggregates are interconnected by a microveinlet network. The
microgranular mineral assemblage consists of green diopside
(containing up to 0.67 wt. % Al2O3 and 2.2 wt. % Cr2O3) rich in
fluid inclusions of CO2, olivine (Fo90 - Fo91), chromite
(Cr/(Cr+Al) = 0.72 to 0.79) and interstitial anorthoclase (Ab52 -
56, Or41 - 45, An01 - 02). The scanning electronic microscope
reveals the presence of apatite phases in these aggregates, but too
small to be analysed by electron microprobe.
The use of a correction equation based on a calibration of
analyses with an electron microprobe in relation to those carried
out with Mössbauer spectroscopy gives more precise evaluation
of Fe3+ in spinels (IBHI et alii, 1999). In fact, it allows a
calculation of the oxygen fugacity in peridotitic xenoliths. The
obtained results show that the peridotites of the Foum El Kouss
massif crystallised under oxygen fugacity which were higher
(log(fO2) – log(fO2)FMQ averaging 0.18 to 0.25).
The aggregates are formed by a secondary mineralogical
paragenesis. Their dispersion and their relation with the primary
minerals suggest that they are the product of a reaction between
the lattes and a carbonatic fluid which has penetrated through the
enclaves.
All the analysed xenoliths are enriched in LREE relative to
HREE and have U-shaped REE patterns, with strongly depleted
middle REE. Since NAVON &STOLPER (1987), U-shaped REE
patterns are generally attributed to chromatographic effects
resulting from interstitial percolation of small melt fractions
through LREE-depleted peridotites. However, the Foum El Kouss
(North of the South-atlasic-fault) xenoliths display more complex
distributions of trace elements, are enriched in LILE (Rb, Ba, Th,
LREE and Sr) and shows negative anomalies of HFSE (Nb, Ta,
Zr and Hf). Such trace-element distribution is generally attributed
to carbonate melt metasomatism (RUDNICK et alii, 1993). The
variation observed across the South-atlasic-fault confirms that
this fault system represent a major lithospheric discontinuity.
REFERENCES
BECCALUVA L., SIENA F., COLTORTI M., DI GRANDE A., LO
GIUDICE A., MACCIOTTA G., TASSINARI R. & VACCARO C.
(1998) - Nephelinitic to tholeiitic magma generation in a
transtensional tectonic setting:an integrated model for the
iblean volcanism, Sicily J. Petrol., 39, 1547-1576.
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SESSIONE 4
BERRAHMA M., DELALOYE M., FAURE-MURET A. & RACHDI H.
(1993) - Premières données géochronologiques sur le
volcanisme alcalin du Jbel Saghro, Anti-Atlas, Maroc. J. Afr.
Earth Sci., 17 (3), 333-341.
IBHI A., NACHIT H., BERRAHMA M., ABIA H. & HERNANDEZ J.
(1998) - Quantification et bilan de matiere de la reaction
clinopyroxene-spinelle lors de la formation du plagioclase
dans les lherzolites a spinelle Estudias Geai., 54, 173-179.
IBHI A. & NACHIT H. (1999) - Découverte d'une association
d'enclaves carbonatite-lherzolite dans le volcanisme Plio-
Quaternaire de Foum El Kouss (Jbel Saghro): mise en
évidence d'un manteau carbonaté à l'aplomb de l'Anti-Atlas
oriental marocain. Géol. Méditerranéenne, 36, (1/2) 19-28.
IBHI A., KHATIB D. & HERNANDEZ J. (1999) - Evaluation du Fe 3+
dans les spinelles pour l'obtention de la fugacité d'oxygène
des nodules ultrabasiques. Ann. Chim. Sci. Mat., 24, 487-
492.
IBHI A., NACHIT H., ABIA EL H. & HERNANDEZ J. (2002) -
Intervention des ségrégats carbonatitiques dans la
pétrogenèse des néphélinites à pyroxène de Jbel Saghro
(Anti-Atlas, Maroc). Bull. Soc. Géol. France, 173, 37-43.
NAVON O. & STOLPER E. (1987) - Geochemical consequence of
melt percolation : The upper mantle as a chromatographic
column, J. Geol., 95, 285-307.
RUDNICK R.L., MCDONOUGH W.F. & CHAPPEL B.W. (1993) -
Carbonatite metasomatism in the Northern Tanzania mantle :
Petrographic and geochemical characteristics, Earth Planet.
Sc. Lett., 114, 463-475.
FEKKAKA A., POUCLET A. & BENHARREFC M. (2003) - The
Middle Neoproterozoic Sidi Flah Group (Anti-Atlas,
Morocco): synrift deposition in a Pan-African
continent/ocean transition zone. J. Afr. Earth Sci., 37 (1-2),
73-87.
96

Relations between grain size and Th-Pb ages of monazite: examples
from high-grade metapelitic gneiss from the Ulten Zone, eastern Alps
Key words: HP metamorphism, monazite LA-ICP-MS dating,
Ulten Zone, Variscan.
INTRODUCTION
Recent studies indicate that monazite is a well suited mineral
for dating amphibolite–facies and higher-grade metamorphic
events of metapelites (KRENN &FINGER, 2007; LANGONE et alii,
2010). Monazite, similarly to zircon, can record multiple
geologic events within single grains. Moreover, different
generations of monazite can be crystallised in response to
changes of the pressure-temperature conditions. In the latter case,
textural and chemical criteria are needed to distinguish earlystage
monazite from peak and late-stage monazite. Generally,
much effort is spent to locate monazite included in other host
minerals (e.g. garnet, micas). Enclosed monazite is believed to
yield older ages compared to the age obtained from matrix
monazite thanks to the armouring effect of host minerals.
However, the assumption of a complete shielding by
porphyroclasts/blasts is debated (MARTIN et alii, 2007). Shielded
monazite is frequently associated with microcracks/microveins
thus allowing mass exchange between host interiors and the
surroundings. As a consequence, an unequivocal correlation
between monazite textural site and ages is difficult (e.g. MARTIN
et alii, 2007).
Another textural criterion that is usually neglected during the
petrographic observation preliminary to the radiometric study is
monazite dimensions. Within the same textural site (e.g. within
the matrix or included in garnet), monazite grain size may vary
considerably. This observation suggests that different generations
of monazite can coexist within the same textural site.
This hypothesis has been tested in a garnet-kyanite paragneiss
from the Variscan Ulten Zone (UZ), which contains monazite in
different textural sites and with highly variable grain size.
Monazite grains have been detected and characterised, in terms of
microstructural position, at the SEM. Chemical analyses and Xray
elemental (Th, Ca, Y, La and Ce) mapping have been
_________________________
ANTONIO LANGONE (*), ROBERTO BRAGA (*), HANS-JOACHIM MASSONNE (**) & MASSIMO TIEPOLO (°)
(*) Dipartimento di Scienze della Terra e Geologico-Ambientali
dell’Università di Bologna, antonio.langone@unibo.it; r.braga@unibo.it
(**) Institut für Mineralogie und Kristallchemie, Universität Stuttgart,
h-j.massonne@imi.uni-stuttgart.de
(°) C.N.R - I.G.G. U.O di Pavia, tiepolo@crystal.unipv.it
97
performed by electron microprobe (EMP). On selected monazite
grains, in situ U-Th-Pb dating by LA-ICP-MS directly in thin
section has also been carried out.
GEOLOGICAL SETTING AND PETROGRAPHY
The Ulten Zone (UZ) is a high-grade basement now in the
uppermost position of the Upper Austroalpine edifice of the
eastern Alps (Trentino Alto-Adige). It represents a portion of
Variscan deep crust that has well recorded the metamorphic
evolution related to the collision between Laurussia and
Gondwana. The UZ mainly consists of high-grade garnet-kyanite
paragneiss that underwent partial melting at 340-330 Ma
(TUMIATI et alii, 2003; Sm-Nd whole rock and internal isochron).
For the present work, a foliated garnet-kyanite paragneiss
consisting of (in order of decreasing abundance) quartz, white
mica, plagioclase, biotite, garnet, kyanite and accessory phases
(rutile, ilmenite, monazite, apatite, zircon and graphite) has been
selected. The high white-mica content suggests an unmelted
nature of the rock because this rock is probably from a relatively
dry and also cold portion of the ca. 1 km thick pile of the UZ
deep crust. This is also confirmed by multi-equilibria
thermobarometry involving garnet + white mica + biotite solidsolutions
yielding 9-10 kbar, 520 °C (using garnet core and mica
inclusions therein) for an early metamorphic stage.
On the basis of textural position, monazite grains were
grouped in: i) monazite grains within garnet and kyanite
porphyroblasts (hereafter, included Mnz), and ii) monazite grains
disseminated within the matrix (Fig. 1) and/or interstitial within
apatite aggregates (hereafter, matrix Mnz). The dimensions vary
of one order of magnitude, from 30x20 μm 2 to 500x250 μm 2 .
Locally, monazite is partially or totally intersected by
microcracks. In a few cases, these fractures create a connection
between the included Mnz and the matrix. Rarely monazite
contains small rounded inclusions of matrix forming minerals
(e.g. quartz) and of xenotime and Th-rich oxides.
DISCUSSION OF LA-ICP-MS DATING OF COARSE- AND
FINE-GRAINED MONAZITE
In the analysed sample, the 208 Pb/ 232 Th ages range nearly
continuously between 365 and 306 Ma, defining three major
clusters at ca. 350, 333, and 314 Ma. Monazite grains yielding
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SESSIONE 4
Th-Pb ages in the range of ca. 350 Ma correspond to large matrix
Mnz (Fig. 1). These grains are characterised by single or multiple
Th(+Ca)-rich internal domains surrounded by La+Ce-rich
external domains, suggesting a pseudomorphic replacement of
allanite during the prograde metamorphic history. The Th-Pb
ages clustering at ca. 330 Ma have been obtained from smaller
matrix Mnz, from overgrowths of the larger matrix Mnz (Fig. 1)
and from included Mnz, or domains of it. Locally, the matrix
Mnz at ca. 330 Ma are characterised by Th(+Ca)-rich internal
domains surrounded by La+Ce-rich external domains. The Th-Pb
ages of ca. 330 Ma have been attributed to a second
crystallisation/re-equilibration event which occurred during peak
or near-peak metamorphic conditions and anatexis. The minor
younger Th-Pb ages (ca. 314 Ma) resulted from dating of external
domains of matrix Mnz and have been assigned to a retrograde
metamorphic evolution. Locally, these younger domains are
characterised by high Y concentration, which can be attributed to
the retrograde garnet breakdown (e.g. KRENN et alii, 2009).
CONCLUSIONS
Different monazite grains form a single thin section yield an
age span of nearly 60 Ma, from prograde amphibolite-facies
conditions through peak metamorphism to subsequent retrograde
amphibolite-facies conditions. We noted that the textural site
occupied by monazite does not deliver relative time information:
coarser monazite retains older ages, regardless its textural site.
The armouring effect may be absent where microcracks connect
included Mnz and the matrix. Interestingly, unshielded matrix
Mnz can also retain older ages, thus suggesting a limited isotopic
resetting by metamorphic fluids. We suggest that sorting
monazite grains based on their size may provide different age
populations and thus a more complete geochronologic history of
the rock. The larger older grains can be seen as clasts formed
during the prograde metamorphic history and survived the peak
metamorphism, during which they developed locally only
overgrowth domains (Fig. 1).
Fig. 1 – Th-elemental map of matrix Mnz showing 208Pb/232Th
(white) and 206Pb/238U (grey) ages. The white circles represent the
ablated areas of ca. 20 μm diameter.
98
REFERENCES
KRENN E. & FINGER F. (2007) – Formation of monazite and
rhabdophane at the expense of allanite during Alpine low
temperature retrogression of metapelitic basement rocks from
Crete, Greece: microprobe data and geochronological
implication. Lithos, 95, 130–147.
KRENN E., J. M., FINGER F., BROSKA I. & KONECNY, P.
(2009) - Two types of metamorphic monazite with contrasting
La/Nd, Th, and Y signatures in an ultrahigh-pressure
metapelite from the Pohorje Mountains, Slovenia: Indications
for pressure-dependent REE exchange between apatite and
monazite? Am. Mineral., 94, 801–815.
LANGONE A., GODARD G., PROSSER G., CAGGIANELLI A.,
ROTTURA A. & TIEPOLO M. (2010) – P-T-t path of the
Hercynian low-pressure rocks from the Mandatoriccio
complex (Sila Massif, Calabria, Italy): new insights for
crustal evolution. J. Metamorp. Geol., 28, 1367-162.
MARTIN A.J., GEHRELS G.E. & DE CELLES P.G. (2007) - The
tectonic significnce of (U,Th)/Pb ages of monazite inclusions
in garnet from the Himalaya of central Nepal. Chem. Geol.,
244,1-24.
TUMIATI S., THÖNI M., NIMIS P., MARTIN S. & MAIR V. (2003) -
Mantle-crust interactions during Variscan subduction in the
Eastern Alps (Nonsberg-Ulten zone): geochronology and new
petrological constraints. Earth Plan. Sci. Lett., 210, 509-526.

Basic magmatism in the Triassic sequences from the Alpujarride
Complex (Betic Cordillera, Spain) and the Lungro-Verbicaro Unit
(Southern Apennines, Italy)
GILDA MATRANGOLO (*), FRANCESCO LIBERI (*), IVAN MARTIN-ROJAS (**) & EUGENIO PILUSO (*)
Key words: Alpujarride Complex, Lungro-Verbicaro unit,
Triassic basic magmatism.
This research project is focused on the study of the basic
magmatism in the Triassic metacarbonate and metapelitic rocks
belonging to the Alpujàrride Complex (Betic Cordillera, SE
Spain) and Lungro-Verbicaro Unit (Southern Apennines, Italy).
These domains were involved in the geodynamic processes active
in the Mediterranean region from the Mesozoic onwards and, in
particular, in the opening of the Jurassic Tethys.
In literature, both the HP/LT Alpujàrride Complex and the
San Donato Unit are interpreted as passive margin successions
deposited during the Triassic rifting, pointing to a stratigraphic
correlation for that regarding the paleogeographic context.
The aim of this study is to characterize the source, the
petrogenetic process and to determine the age of the basic
magmatism affecting the Betic and the Triassic successions, in
order to test this hypothesis.
Triassic magmatic rocks in the Mediterranean area are
distributed along the orogenic Apennines-Alpine-Dinaric-
Hellenic-Reef-Betic belts. In the Northern Calabria basic rocks
are represented by pillow-lavas and dykes cutting through
Triassic and Jurassic formations (IANNACE et alii, 2007). In the
Betic Cordillera gabbros intrude sedimentary successions until
Middle Trias (VERA, 2004 and references therein).
Preliminary petrographic analysis on samples from both the
studied areas allow to recognize three main lithotypes: i)
metagabbros showing ophitic to subophitic texture, with a
mineral assemblage made of Pl+Cpx+Amph+Ep-Chl+Qz+Mg; ii)
fine grained metabasites whose original magmatic texture is
completely reworked by metamorphic recrystallization, the
mineral assemblage is mede of Na-amph+ Stp+ Chl+ Pmp+ Cal+
Mg; iii) gabbros with ophitic structure with mineral assemblage
made of Pl+ Cpx+ Na-Cl-amph+ Act+ Ep+ Bt+ K-mica+ Chl+
Mg.
_________________________
(*) Dipartimento di Scienze della Terra, Università della Calabria,
gilda.matrangolo@unical.it
(**) Departamento de Ciencias y del Medio Ambiente, Universidad de
Alicante
99
Bulk rock compositions obtained by XRF indicate the
presence of two suites: 1) the samples from Northern Calabria
and four from the Betic Cordillera show an alkaline to alkalinetransitional
character and have a relatively low Y/Nb vs Zr/Nb
ratio; For these samples, according to the La/10-Y/15-Nb/8
diagram, a continental to intracontinental rift context is supposed;
2) most of the samples from the Alpujarride complex show a
linear fractionation trend in the Ti/V diagram, according to the
La/10-Y/15-Nb/8 diagram they plot in the basalt calc-alkaline
fields.
REFERENCES
IANNACE A., VITALE S., D'ERRICO M., MAZZOLI S., DI STASO,
MACAIONE E., MESSINA A., SOMMA R., REDDY S.,
ZAMPARELLI V. & BONARDI G. (2007) - The carbonate
tectonic units of northern Calabria (Italy): A record of
Apulian paleomargin evolution and Miocene convergence,
continental crust subduction, and exhumation of HP-LT
rocks. J. Geol. Soc., London, 164, 1165-1186
VERA J.A., (ed.) (2004) – Geologia de Espana. SGE-IGME,
Madrid.
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SESSIONE 4
Combining zircon chemical composition and geochronology (Pb/Pb
dating) to characterize the Southalpine and the Austroalpine
quartzphyllite complexes from the eastern Alps
Key words: Austroalpine Complexes, evaporation method,
quartzphyllite, Southalpine Complexes, zircon.
INTRODUCTION
Zircon evaporation thermal ionisation mass spectrometry
(TIMS) is used in geochronology to determine absolute
207 Pb/ 206 Pb ages and to distinguish between crystal rim and core,
providing precise information about the time of magmatic crystal
growth, partial dissolution, and/or metamorphic overgrowth
(KLÖTZLI, 1997).
Detrital zircon composition and geochronology has been used
to constrain the thermal evolution of orogenic systems;
furthermore zircon is used both as a thermometer for
crystallization conditions and as petrogenetic indicator (e.g.,
PUPIN, 1980; VAVRA, 1993; HANCHAR &HOSKIN, 2003). The
typological study of zircon populations is, for instance, an
extremely valuable tool to identify the protholith features (PUPIN,
1980). Moreover, zircon is widely used in geochronological
studies (e.g., MEZGER &KROGSTAD, 1997; PARRISH &NOBLE,
2003; HANCHAR &HOSKIN, 2003).
Trace-element contents and elemental ratios have been
suggested both as indicator of magma fractionation and as a
estimate of magma source (e.g., PUPIN, 1992, 1994).
This paper present Pb-Pb single zircon evaporation data and
typological and geochemical study on the Austroalpine (Goldeck,
Gailtal, Thurntaler) and the Southalpine quartz-phyllites
(Vetriolo, Recoaro). The data are discussed for a tentative
comparison of the two complexes.
GEOLOGICAL SETTING
The Austroalpine and Southalpine basement were located in
the northern margin of the Adria microplate. The northern margin
_________________________
(*) Università della Calabria, perri@unibas.it
(**) Dipartimento di Chimica, Università della Basilicata, Potenza,
giovanna.rizzo@unibas.it
FRANCESCO PERRI (*) & GIOVANNA RIZZO (**)
100
of the Adria microplate is cut by the EW tectonic Insubric Line
which separates the Austroalpine basement from the Southalpine
(Fig. 1). Two tectonic lines cut the Austroalpine basement: the
Defferegen-Anterselva-Valles (DAV) and the Kalkstein-Vallarga
faults. All these two basements were involved in the Alpine
orogeny and were affected by a variously aged Alpine
metamorphism (SASSI et alii, 2004).
The Austroalpine and Southalpine complexes consist of a
rather monotonous series of mainly meta-pelitic rocks with
interbedded thick mafic vulcanites, subordinate acidic vulcanites
as well as thin carbonate layers. The Austroalpine and
Southalpine quartzphyllite complexes were overprinted by at
least a pre-Permian greenschist facies metamorphism and took
place under low pressure conditions and a metamorphic thermal
gradient of about 40°C/Km (MAZZOLI &SASSI, 1988; SASSI et
alii, 1994).
Fig. 1 – Simplified geological map displaying the distribution of basement
units in tha Alps and location of sampling areas (modified from SASSI et alii,
2004).
Alpine overprinting, where present, is of variable intensity.
Scarce fossil records, mostly conodonts and acritarchs, have
given rise to a partly resolved stratigraphy of incomplete known
sections. In fact in the Southalpine quartz-phyllite an acritarch
assemblage was locally found (Col di Foglia, near Agordo)
suggesting a Late Cambrian to Tremadocian sedimentation age
(SASSI et alii, 1984). In the Austroalpine quartz-phyllite the range
of biostratigraphic data suggests a general late Ordovician to
Devonian age, mainly based on conodonts from carbonate strata

(SASSI et alii, 1994). All data (SASSI et alii, 1994) suggest the
hypothesis that the Austroalpine and Southalpine complexes in
the Eastern Alps shared a common Paleozoic evolution at least
since Upper Ordovician.
The zircon studied come from the quartz-phyllite
Austroalpine Complex (Thurntaler, Gailtal and Goldeck) and
from the quartz-phyllite Southalpine Complex (Recoaro,
Vetriolo) and their location is shown in figure 1.
DISCUSSION AND CONCLUSIONS
Combination of zircon morphology and geochronological
analyses (single zircon evaporation technique) was used in order
to obtain significant constraints for the age of the studied
protoliths.
The Austroalpine quartzphyllites are grey, fine to medium
grained and display a schistosity that in some cases is crenulated.
The Austroalpine quartzphyllites consists of quartz, plagioclase,
garnet, white mica and chlorite. Zircon, ilmenite, apatite and
titanite are common accessory minerals. Alternating layers of
different grain size and composition are present. The garnet in
some cases is presents in porfiroblasts and surrounded by a
lepidoblastic interlacing of chlorite and white mica. In some cases
occurs as poikiloblasts. The bands enriched in quartz and
plagioclase show a granoblastic texture.
The Southalpine quartzphyllites are grey or grey-green, finegrained
that is in some cases is transposed and crenulated. The
Southalpine quartzphyllites consists of quartz, albite, white mica
and chlorite. Zircon, ilmenite, apatite and titanite are common
accessory minerals. The Southalpine quartzphyllites are banded
with bands enriched in quartz and albite that show a typical
granoblastic texture and bands enriched in chlorite and white
mica that occurs in elongate flakes and show a lepidoblastic
texture.
The zircons from Austroalpine and Southalpine
quartzphyllites show many differences for shape, colour, size,
types of inclusions, cracks, and turbidity based on the
morphological study, suggesting the existence of two distinct
groups.
Electron microprobe analyses (Si, Zr, Hf, P, HREE) indicate
homogeneous compositions, suggestive of probably common
source-areas characterized by granitoid rocks.
The zircon ages of the Southalpine and Austroalpine quartzphyllites
are quite different and those of the Austroalpine samples
are younger than the Southalpine studied samples. Protolith Pb–
Pb zircon ages data define two principal evolution lines. The
Australpine Complexes are characterized by an older evolution
typical of subduction-related magmatism, started by 598-Ma N-
MORB-type, which mainly involved depleted mantle sources. It
finished with mainly crustal source 379–341-Ma acid magmatites.
The Southalpine Complexes zircon ages show an evolution line
101
by tholeiitic and 473-Ma alkaline within-plate basalt type suites
in both pre- and post-Early-Ordovician units characterized by an
intraplate mantle metasomatism and enrichment trend along
multicomponent sources. These magmatic evolution lines can be
related to a plate tectonic scenario that involved terranes in a
progressively mature Neoproterozoic to Ordovician active
margin, and a subsequent Palaeo-Tethys passive margin along the
north Gondwanan periphery.
REFERENCES
HANCHAR J.M. & HOSKIN P.W.O. (2003) - Zircon. Rev. Mineral.
Geochem., 53, 1-500.
KLÖTZLI U.S. (1997) - Single zircon evaporation thermal
ionisation mass spectrometry: method and procedures.
Analyst, 122, 1239-1248.
MAZZOLI C. & SASSI R. (1988) - Caratteri del metamorfismo
ercinico nella fillade sudalpina ad ovest di Bressanone. Mem.
Sci. Geol., 40, 295-314.
MEZGER K&KROGSTAD J. (1997) - Interpretation of discordant
U-Pb in zircon ages: an evaluation. J. Metamorph. Geol., 15,
127-140.
PARRISH R.R. & NOBLE S.R. (2003) - Zircon U-Th-Pb
Geochronology by Isotope Dilution - Thermal Ionization
Mass Spectrometry (ID-TIMS). In: Hanchar JM and Hoskin
PWO (Eds), Zircon. Rev Miner Geochem, 53, 183-213.
PUPIN J.P. (1980) - Zircon and granite petrology. Contrib.
Mineral. Petrol., 73, 207-220.
PUPIN J.P. (1992) - Les zircons des granites océaniques et
continentaux: couplage typologie-géochimie des éléments en
traces. Soc. Géol. France, Bull., 163, 495–507.
PUPIN J.P. (1994) - Caractérization des protolithes des
migmatites et granites anatectiques crustaux d'après l'étude
des zircons. 319, C.R. Acad. Sci., Paris série II, 1191-1197.
SASSI F.P., NEUBAUER F., MAZZOLI C., SASSI R., SPIESS R. &
ZIRPOLI G. (1994) - A tentative comparision of the Paleozoic
evolution of the Austoalpine and Southalpine quartzphyllites
in the Eastern Alps. Per. Mineral., 63, 35-52.
SASSI F.P., CESARE B., MAZZOLI C., PERUZZO L., SASSI R. &
SPIESS R. (2004) - The crystalline basements of the Italian
eastern Alps: a review of the metamorphic features. Per.
Mineral., 73, 23-42.
VAVRA G. (1993) - A guide to quantitative morphology of
accessory zircon. Chem. Geol., 110, 15-28.
SESSIONE 4

SESSIONE 4
Magmatic and metamorphic processes in late-Hercynian lower crust
section from the Northern Calabria
Key words: Crust, late-Hercynian, Northern Calabria.
The northern sector of the Calabrian Arc is a Cenozoic nappe
stack formed of three main tectonic complex, from the bottom to
the top: the Apenninic units derived from the Apulian passive
continental margin, the ophiolite-bearing units with Jurassic
Thetys affinity and an Hercynian crust complex, referred to as
Calabride nappe. New data allow to define the Calabride nappe,
cropping out in the Catena Costiera range and in the Sila massif,
as a continous continental lithospheric section whose main
tectonic framework was achieved between Hercynian and early
Mesozoic times and remobilized during Tertiary.
The deepest part of the Hercynian continental crust and the
crust-to-mantle boundary are exposed in the northern sector of
the Catena Costiera area.
The continental crust rocks are formed of garnet-biotitegneiss,
garnet-pyroxene-beraing granulites, migmatites, restites,
small oxide-silicate-bearing marble lenses and small stocks of
calcalkaine-peraluminous granitic rocks.
The mantle rocks mainly consist of Spl-amphibole-peridotites,
which sometimes include folded, transposed and boudinated
pyroxenite veins.
The peridotites are severely serpentinized, altough small, less
serpentinized portions are locally preserved. The contact between
mantle and crustal rocks is marked by gabbroic intrusions that
show a tholeiitic fractionation trend. The gabbros crop out as
centimetric veins, as metric dykes intruded within peridotites and
as decametric banded-textured bodies enclosed between crustal
granulites and mantle ultramafites, showing sharp contacts with
the country rocks.
The physical conditions inferred from deepest crustal rocks
are 0.9-1.1 GPa, P and 750-800°C, T for the Hercynian (300
m.y.) granulitic metamorpic climax.
After the metamorphic climax, the thermobarometric data
documented a composite decompression path characterized by a
first stage of anydrous adiabatic decompression to 800°C, T, and
0.8 GPa, P, followed by a second stage of decompression and
cooling to about 650-700°C, T and 0.6-0.7 GPa, P. The
calculated P-T-path for crustal rocks documented a post
_________________________
(*) Dipartimento di Scienze della Terra, Università della Calabria,
e.piluso@unical.it
EUGENIO PILUSO (*) & FRANCESCA LIBERI (*)
102
Hercynian lithospheric scale thermal anomaly, probably due to an
astenospheric upwelling that caused partial melting in the upper
mantle.
The upper mantle partial melting is likely responsible for the
Triassic underplating magmatism that produced gabbro intrusions
at the crust to mantle interface during the decompression.
On the basis of the above data, it can be inferred that a lower
crust-mantle transition, sealed by gabbroic intrusion, formed
during late Permian- early Triassic time in the Northern Calabria.
During subsequent Tethyan rifting phase, these rocks were
exhumed at higher crustal levels as testified by the occurences of
unmetamorphosed basaltic dyke that cross cut the migmatites, A
whole rocks K-Ar age of 120Ma has been determined for these
dyke. During the Tertiary Apenninic convergence the deepest
part of the Calabrian continental lithosphere were accreted onto
the present Northern Calabria nappe stack.

Contribution to the knowledge of the Hyblean lithosphere (southeastern
Sicily, Italy): the petrophysical approach
Key words: Deep seated xenoliths, Hyblean Plateau,
petrophysics.
INTRODUCTION
The Hyblean Plateau, cropping out in the south-eastern corner
of Sicily (Italy), consists of a thick Meso-Cenozoic carbonate
sequence and of Neogene-Quaternay open shelf terrigenous
sediments with interbedded volcanic basic rocks. The volcanic
activity occurred according to more episodes: the eldest from late
Triassic to the end of Cretaceous (alkali basalts with OIB
affinity); in the late Miocene the activity is characterised by the
emplacement of alkaline basic tuff breccia pipes within both
shallow and deep water carbonate sediments. During Pliocene
and early Pleistocene fissural eruptions occurred along a NW-SE
fault system. Finally, the Neogene products mostly consist of
tholeiitic basalts, alkaline basalts and basanites (ROCCHI et alii,
1998; BECCALUVA et alii, 1998; DI GRANDE et alii, 1999).
In this paper, attention focused on deep-seated xenoliths
occurring within Miocene tuff-breccias from Valle Guffari,
whose diatremes have been interpreted as part of a seamount belt
located within the carbonate ramp (SUITING &SCHMINKE, 2009).
Collected specimens consist of spinel facies peridotites (lherzolite
and harzburgite) and different types of spinel bearing pyroxenites
(Cr-diopside websterites, Al-augite websterites, spinel and garnet
clinopyroxenites; ATZORI et alii, (1999) and therein references)
accompanied by a feldspar bearing suite mostly represented by
mafic granulites and minor metagabbros and anorthosites
(PUNTURO et alii, 2000).
In order to contribute to knowledge of the inaccessible
lithosphere beneath the Hyblean Plateau, a petrophysical
investigation was carried out on a selection of representative
litho-types.
EXPERIMENTAL RESULTS
_________________________
(*) Dipartimento di Scienze Geologiche, Università degli Studi di Catania,
punturo@unict.it
ROSALDA PUNTURO (*)
103
Fig. 1 – Location of the Hyblean Plateau. Star indicates Valle Guffari.
Petrography
The petrographic features of the Hyblean xenoliths from Valle
Guffari may be summarized as follows: peridotites (harzburgites
and harzburgitic lherzolites) are constituted by olivine (Fo89-91),
orthopyroxene (En88-91; mg#90-92), clinopyroxene (Cr-Diopside;
En51-54Fs2-4Wo44–48 ), Cr-rich spinel (Cr number= 23-35) and very
rare phlogopite, this latter testifies metasomatic events within the
Hyblean mantle (PUNTURO, 1998). They exhibit a widespread
protogranular texture, with grain size ranging from medium (1-
4mm) to coarse (2-6mm); olivine and orthopyroxene are kinkbanded,
Cr-diopside and spinel show smaller grain size.
Pyroxenites show various features, in terms of texture, colour
and grain size: Cr-Diopside websterites (Cr-diopside, Ca-poor
pyroxene, Cr-Al spinel, ±olivine and amphibole) occur as veins
into peridotites are green and coarse with xenomorphic granular
texture; Al-diopside websterites are black and polygonal textured,
constituent minerals are Al-diopside, Ca-poor pyroxene, Alspinel,
garnet (Py54.5Alm32Grs13.5); pyroxenes often exhibit
exolution lamellae. Al-augite pyroxenites are constituted by Alclinopyroxene,
Al-spinel, garnet (Py64Alm25.6Grs9.6) and have
been interpreted as igneous adcumulitic products; they look
glassy black and are ultracoarse (>20mm); intergranular glass is
very common.
Among feldspar-bearing xenoliths, mafic granulite is the most
abundant litho-type; texture is polygonal with grain size from fine
(0.3-1 mm) to medium. Constituent minerals are plagioclase, Ca-
SESSIONE 4

SESSIONE 4
pyroxene, Ca-poor pyroxene and Al-spinel; amphibole is very
rare. Metagabbro and metadiorite (plagioclase, Ca-pyroxene, Fe-
Ti oxides, apatite) and anorthosite (plagioclase ± Al-spinel and
pyroxene) occur at a lesser extent.
Pressure-temperature estimates, based on the coesistence of
two pyroxenes plus garnet assemblage within pyroxenites
(ATZORI et al., 1999) provided equilibration values of 0.98GPa at
740°C for spinel pyroxenite and 1.32GPa at 1040°C for garnet
pyroxenite. As far as mafic granulite, P-T estimate are not
reliable because of evident disequilibiurm features; however, the
occurrence of spinel with no evidence of olivine or garnet would
suggest as the temperature interval for the mafic granulite plots
within the equilibration field of Al-diopside websterite. It is
worth noting that pressure estimates by NIMIS &ULMER (1998)
gave values of 0.5GPa for clinopyroxene within gabbros.
Petrophysical investigation
Three deep-seated xenoliths, representative of the main lithotypes
occurring within the studied suite, were selected for
petrophysical investigation: one spinel-harzburgite, one
pyroxenite and one mafic granulite.
The seismic properties of this suite of deep-seated xenoliths
were experimentally determined with a multi-anvil apparatus at
confining pressure up to 600MPa (room temperature) and up to
600°C (at 600MPa), by using the ultrasonic transmission pulse
technique. For a more complete experimental dataset see
PUNTURO et al. (2000). Average Vp and Vs values as well as Vprelated
seismic anisotropy are here presented as a function of
pressure and temperature. The average of P-wave velocities at
600MPa at 600°C are 7.15 km/s, 7.46km/s and 6.41km/s for
spinel harzburgite, pyroxenite and mafic granulite, respectively.
The corresponding average values of S-wave velocities are
4.02km/s, 4.22km/s and 3.59km/s. Vp-related seismic anisotropy
ranges from 2.02 to 1.26 to 0.91. All of the three xenoliths exhibit
very weak shear wave splitting within the foliation plane
(0.08km/s). Density values at 600MPa and 600°C are 3.038
g/cm 3 , 3.295 g/cm 3 and 2.958g/cm 3 for spinel harzburgite,
pyroxenite and mafic granulite, respectively.
FINAL REMARKS
The petrophysical study carried out on the xenoliths from
Valle Guffari is aimed as a contribution to the comprehension of
the Hyblean inaccesible lithosphere; for this reason, investigation
was carried out on a suite of litho-types considered to be more
representative of large scale lithological units. At the same time,
obtained information permit available geophysical data to be
constrained and interpreted at a better extent; this particularly
holds for unravelling the nature of the Hyblean lithosphere, which
is still matter of debate.
104
REFERENCES
ATZORI P., MAZZOLENI P., PUNTURO R. & SCRIBANO V. (1999) -
Garnet-bearing pyroxenite xenoliths from Hyblean Plateau
(South-Eastern Sicily, Italy) – Mineral.and Petrol., 27, 1-17.
BECCALUVA L., SIENA F., COLTORTI M., DI GRANDE A., LO
GIUDICE A., MACCIOTTA G., TASSINAR R. & VACCARO C.
(1998) - Nephelinitic to Tholeiitic Magma Generation in a
transtentional Tectonic Setting: an Integrated Model for the
Iblean Volcanism, Sicily. J. Petrol., 39 (9):1-30.
NIMIS P. & ULMER P. (1998) - Clinopyroxene geobarometry of
magmatic rocks. Part 1: an expanded structural
geobarometer for anhydrous and hydrous, basic and
ultrabasis systems. Contrib. Miner. Petrol., 133, 122-135.
PUNTURO R., KERN H., SCRIBANO V. & ATZORI P. (2000) -
Petrophysical and petrological characteristics of deep-seated
xenoliths from Hyblean Plateau, south-eastern Sicily, Italy:
suggestions for a lithospheric model. Mineral. Petrogr. Acta,
43, 1–20.
ROCCHI S., LONGARETTI G. & SALVADORI M. (1998) - Subsurface
Mesozoic and Cenozoic magmtism in south-eastern Sicily:
distribution, volume and geochemistry magmas. Acta
Vulcanologica, 10 (2), 395-408.
DI GRANDE A., LO GIUDICE A. & TRANCHINA A. (1999) - Carta
Geopetrografica delle vulcaniti subaree dell’area “M. Lauro-
M.Santa Venere” (Monti Iblei, Sicilia sud-orientale).
SUITING I. & SCHMINKE H. (2009) - Iblean diatremes 2: shallow
marine volcanism in the Central Mediterranean at the onset
of the Messinian Salinity Crisis (Iblean Mountains, SE-Sicily)
– a multidisciplinary approach. Int. J., Earth Sci. (Geol.
Rundsch). DOI 10.1007/s00531-009-0495-4.

Hybridization of the peridotite layers from the Serre lower-crust
section (Calabria)
Key words: Calabria, hybriditization, lower-crust section, Serre
Massif.
The metasomatic processes and the metasomatising agents
affecting mantle peridotites have been studied and documented in
both mantle xenoliths in basaltic rocks and in Alpine-type
peridotite.
Conversely the metasomatic transformations that interested
the peridotites forming part of a basic lower-continental crust
sequence and interlayered with cumulitic metagabbros, are less
studied and almost unknown.
The deepest part of the continental crust section outcrops in
the northerwestern part of the Serre Massif, southern Calabria. It
is mainly formed of metagabbroic rocks and pyriclasites.
Ultramafic rocks occur as continous metric layers or as
decimetric lenses within metagabbroic sequences.
The ultramafic rocks comprehend phlogopite-bearing and
orthopyroxene-rich peridotites, and phlogopite-bearing
orthopyroxenite.
The metagabbros and ultramafics rocks of the Serre Massif
are intruded by trondhjemitic-tonalitic dykes. The occurrence of
phlogopite and orthopyroxene-rich portions and veinlets in the
peridotites from the Serre Massif indicates that the rocks
underwent metasomatic events.
The Curinga ultramafics carry a peculiar chemical
composition. To account for that a hybriditization process
between trondhjemitic-tonalitic melt and peridotites has been
suggested and the composition of different mixtures were
calculated according to the data and procedure of the literature.
The comparison between the composition of the calculated
mixtures and that of the Serre peridotites shows that the latters
have compositions comparable with mixtures of about 20-30 wt%
of trondhjemitic-tonalitic melt; whereas the phlogopite
orthopyroxenite composition may be obtained with mixture up to
50 wt% of the contaminant agent.
_________________________
(*) Dipartimento di Chimica, Università della Basilicata, Potenza,
giovanna.rizzo@unibas.it
(**) Dipartimento di Scienze della Terra, Università della Calabria,
e.piluso@unical.it
GIOVANNA RIZZO (*) & EUGENIO PILUSO (**)
105
SESSIONE 4

SESSIONE 4
Rodingites from Frido Unit: evidences for metasomatic alteration
Key words: Frido Unit, metasomatism, rodingites, Southern
Apennine.
GEOLOGICAL SETTING
The Southern Apennine Chain is a fold-and-thrust belt,
formed between the upper Oligocene and the Quaternary ages
(PATACCA &SCANDONE 2007 and references therein), resulting
from the convergence between African and European plates and
the simultaneous rollback of the SE-directed Ionian subduction
(GUEGUEN et alii, 1998; CELLO &MAZZOLI 1999; DOGLIONI et
alii, 1999). The Apennine accretionary wedge is related to the
northward subduction of an Alpine Tethys (Stampfli et alii, 2002)
sea floor remnant, also known as western Tethys (BORTOLOTTI &
PRINCIPI, 2005), under Europe since Oligocene times. In the late
Miocene age, the slab rollback reached another oceanic remnant
in the Ionian sea region constituted by the westernmost part of the
Neotethys Ocean (STAMPFLI et alii, 2002). The ophiolitic
sequences, which are part of the southern Apennines, are
remnants of the Ligurian sector lithosphere of the Jurassic
western Tethys which. The Liguride tectonic units are derived
from the western Tethys Ocean which separated the European
plate from the African one, situated at the NW and the SE,
respectively. These units outcrop extensively in the southern
Apennines, especially in the north-eastern slope of the Pollino
Ridge. They consist of sedimentary sequences ranging from the
Upper Jurassic to the upper Oligocene ages and several bodies of
oceanic and continental crust. These sequences are divided up
into different tectonic units some of which show a very low to
low-grade metamorphic overprint (VEZZANI, 1969).
The ophiolitic rocks occurring in the Frido Unit consist of
serpentinites derived from mantle lherzolite and subordinately
harzburgites. Serpentinites are frequently associated with
metagabbros, metabasalts with a relic pillow structure
(LANZAFAME et alii, 1979; SPADEA, 1982; 1994) as well as
tectonic slices made of diabase and medium-to high grade
metamorphic rocks (such as amphibolites, gneiss, and granofels).
___________________________________________
(*) Dipartimento di Scienze Geologiche, Università degli studi della
Basilicata, cristi.sansone@unibas.it
(**) Dipartimento di Chimica, Università degli studi della Balilicata,
giovanna.rizzo@unibas.it
MARIA T. CRISTI SANSONE (*) & GIOVANNA RIZZO (**)
106
RODINGITES
Rodingites outcrop as dikes cutting through serpentinites and
are a few centimeters thick, grey-whitish and show a ductile
deformation. The ultramafic rocks consist of serpentinized
peridotite derived from lherzolites and subordinately
harzburgites. Petrography and mineral chemistry of rodingites
facilitated the finding of the igneous and metamorphic mineral
assemblages related both to the primary magmatic protolith and
to the subsequent metamorphic evolution. Rodingites show
granoblastic texture. The primary igneous assemblage consists of
plagioclase and clinopyroxene; these minerals cannot be
preserved in rodingites due to a more accentuated rodingitic
alteration. The metamorphic mineral assemblage consists of
garnet, prehnite, chlorite, pumpellyite and quartz. Accessory
minerals are titanite, epidote, opaque minerals, zircon and apatite.
The veins cut through rodingites filled of prehnite, pumpellyite,
chlorite and calcite and show cataclastic-mylonitic deformations.
In order to obtain mineral chemistry electron microprobe analyses
were performed on the garnet, chlorite, titanite and ilmenite.
Garnet overgrowing on plagioclase is hydrogrossularite. Typical
rodingitization reactions in rodingitic dikes are shown by the
replacement of plagioclase by hydrogrossularite (SANSONE et alii,
2009).
REFERENCES
CELLO G. & MAZZOLI S. (1999) - Appenine tectonics in southern
Italy: a rewiew. J. Geodin., 27, 191-211.
DOGLIONI C., GUEGUEN E., HARABAGLIA P. & MONGELLI F.
(1999) - On the origin of west-directed subduction zones and
applications to the western Mediterranean. In: B.Durand,
L.Jolivet, F.Horváth and. M. Séranne (Eds) - The
Mediterranean basins: Tertiary Extension withing the Alpine
Orogenen. Geol. Soc. London, Spec. Publ., 156, 541-561.
GUEGUEN E., DOGLIONI C. & FERNANDEZ M. (1998) - On the
post-25 Ma geodynamic evolution of the western
Mediterranean. Tectonophysics, 298, 259-269.
LANZAFAME G., SPADEA P. & TORTORICI L. (1978) - Provenienza
ed evoluzione dei Flysch Cretacico - Eocenici della regione

Calabro-Lucana. II: Relazioni tra ofioliti e Flysch Calabro-
Lucano. Ofioliti, 3, 189–210.
LANZAFAME G., SPADEA P. & TORTORICI L. (1979) - Mesozoic
Ophiolites of Northern Calabria and Lucanian Apennine
(Southern Italy). Ofioliti, 4 ,173-182.
PATACCA E. & SCANDONE P. (2007) - Geology of the Southern
Apennines. In: Mazzotti A., Patacca E. &. Scandone P. Eds.,
Results of the CROP Project, Sub-project CROP-04 Southern
Apennines (Italy). Boll. Soc. Geol. It., Spec. Issue, 7, 75-119.
SANSONE M.T.C., RIZZO G. & MONGELLI G. - Petrochemical
characterization of mafic rocks from Ligurian ophiolites,
southern Apennines. Int. Geol. Rev., DOI:
10.1080/00206810902954993.
SPADEA P. (1982) - Continental crust rock associated with
ophiolites in Lucanian Apennine (Southern Italy). Ofioliti, 7,
501-522.
SPADEA P. (1994) - Calabria-Lucania ophiolites. Boll. Geofis.
Teor. Appl., 36, 271-281.
STAMPFLI G.M., BOREL G.D., MARCHANT R. & MOSAR J. (2002).
Western Alps geological constraints on western Tethyan
reconstructions. In: Rosembaum G. & Lister G. S., Eds.,
Reconstruction of the evolution of the Alpine-Himalayan
Orogen. J. Virtual Expl., 8, 77-106.
VEZZANI L. (1969) - La Formazione del Frido (Neocomiano-
Aptiano) tra il Pollino ed il Sinni. Geol. Rom., 8, 129-176.
107
SESSIONE 4

SESSIONE 4
Key words: Adamello batholith, dunite, geochronology, wehrlite,
zircon.
INTRODUCTION
The eclogites from the Piedmontese domain of the Western
Alps provide evidence for subduction of oceanic lithosphere and
show crystallisation ages mainly ranging from ~50 to 44 Ma
(RUBATTO et alii, 1998; RUBATTO & HERMANN, 2003;
DUCHESNE et alii, 1997; BOWTELL et alii, 1994). However, no
igneous activity synchronous with this HP-UHP event was ever
found in the Alpine belt. The oldest magmatic products are dated
at 40-42 Ma (HANSMANN &OBERLI, 1991; DEL MORO et alii,
1983) and were found for the southern portion of the Adamello
batholith.
PETROLOGY
In different localities of the southern Adamello batholith (Re
di Castello Unit), dunitic to wehrlitic clots were found in
amphibole-rich mafic and ultramafic intrusives. Ultramafic clots
consist of olivine (Fo = 85-87 mol%, Ni = 1180-1400 ppm), Crrich
spinel and minor clinopyroxene. Clinopyroxene has high
mg# (up to 0.90) and Cr contents (up to 4560 ppm). Its chondrite
normalised REE pattern has slight depleted to nearly flat LREE
(LaN/SmN = 0.7-1.0) and almost flat HREE at about 2-3 times C1
chondrite. The incompatible trace element pattern reveals
depletions in Nb, Zr, Hf and Pb with respect to neighbouring
elements.
The compositions of the melts in equilibrium with
clinopyroxene was calculated by applying Cpx/L D suitable for
basaltic systems. The incompatible element pattern of calculated
melts is characterised by low concentrations of HREE, Zr and Hf
(at ~0.2 times N-MORB) and marked enrichment in LREE, Pb,
_________________________
Evidence for a hidden subduction-related igneous activity in the
Alps during Early Eocene
MASSIMO TIEPOLO (*), RICCARDO TRIBUZIO (**) & ANTONIO LANGONE (°)
(*) C.N.R - I.G.G. U.O di Pavia, tiepolo@crystal.unipv.it
(**) Dipartimento di Scienze della Terra, Università di Pavia,
tribuzio@crystal.unipv.it
(°) Dipartimento di Scienze della Terra e Geologico-Ambientali
dell’Università di Bologna, antonio.langone@unibo.it
108
Th and U. In addition, calculated equilibrium melts display
negative Nb anomaly (NbN/LaN = 0.3) and high SrN/YN values.
According to the textural and chemical features, the dunitic to
wehrlitic clots represent fragments of ultramafic intrusives
crystallised from subduction-related, high-Mg melts. These rocks
were dismembered by the injection of volatile-rich melts, which
gave rise to host amphibole-rich mafic and ultramafic intrusives.
GEOCRONOLOGY
Zircons were separated from amphibole-rich intrusives
hosting the dunitic to wehrlitic clots. The cathodoluminescence
characterisation of zircon internal structures revealed two
different typologies: i) pseudo-prismatic zircons with welldeveloped
oscillatory zoning and quartz inclusions; ii) anhedral
zircons with xenocrystic cores overgrowth by rims with a welldeveloped
oscillatory or sector zoning. In particular, xenocrystic
cores exhibit light grey or low CL emission; a weak oscillatory
zoning is locally recognisable.
U-Pb determinations were carried out on the different zircon
domains. Three different age populations have been
distinguished. The major age peak is at ~40 Ma and pertains to
zircon domains with well-developed oscillatory zoning in zircon
type I or to the rim of zircon type-II. The xenocrystic zircon
domains with light grey CL emission define a statistically
distinguishable peak at ~44 Ma. The xenocrystic zircon domains
with low CL emission show the oldest ages, which define a peak
at ~50 Ma. In addition, a few U-Pb analyses of the darkest
xenocrystic domains have furnished up to 58 Ma old ages. The
xenocrystic zircon domains do not show negative Eu anomaly in
their REE patterns and thus they were not equilibrated with
plagioclase.
The zircon domains dated at ~40 Ma formed during the latest
igneous event and most likely record the emplacement of the
amphibole-rich mafic and ultramafic intrusives hosting the dunitic
to wehrlitic clots. This conclusion is consistent with the ~40 Ma
age indicated by HANSMANN & OBERLI (1991; U-Pb TIMS
zircon data) for the crystallisation of mafic rocks from the Re di
Castello Unit, and with the age of 41.8 ± 1.4 Ma (K/Ar in
hornblende) reported by DEL MORO et alii (1983) for a quartzbearing
gabbro of the same Unit. The xenocrystic zircon domains
dated at ~44 Ma and ~50 Ma show evidence for an older
magmatic event synchronous with the HP and UHP

metamorphism recorded by the eclogites from the Piedmontese
domain (RUBATTO et alii, 1998; RUBATTO &HERMANN, 2003;
DUCHESNE et alii, 1997; BOWTELL et alii, 1994).
CONCLUSIONS
A subduction-related igneous activity that formed dunitic to
wehrlitic to intrusives predated the early magmatic pulses that
gave rise to the Adamello batholith. The formation of the dunites
to wehrlites was most likely related to the subduction of oceanic
lithosphere in the Early Eocene.
REFERENCES
BOWTELL S.A., CLIFF R.A. & BARNICOAT A.C. (1994) - Sm–Nd
isotopicevidence on the age of eclogitization in the Zermatt-
Saas ophiolite. J. Met. Geol., 12, 187–196.
DEL MORO A., PARDINI G., QUERCIOLI C., VILLA I.M., &
CALLEGARI E. (1983) – Rb/Sr and K/ar chronology of
Adamello Granitoids, southern Alps. Mem. Soc. Geol. It., 26,
285-299.
DUCHESNE S., BLICHERT-TOFT J., LUAIS B., Te?LOUK P.,
LARDEAUX J.M. & ALBAREDE F. (1997) - The Lu–Hf dating
of garnets and the ages of the Alpine high-pressure
metamorphism. Nature, 387, 586 – 589.
HANSMANN W. & OBERLI F. (1991) - Zircon inheritance in an
igneous rock suite from the southern Adamello batholith
(Italian Alps). Contrib. Mineral. Petrol ., 107, 501–518.
RUBATTO D., GEBAUER D. & FANNING M. (1998) - Jurassic
formation and Eocene subduction of the Zermatt-Saas-Fee
ophiolites; implications for the geodynamic evolution of the
Central and Western Alps. Contrib. Mineral. Petrol., 132, 269.
RUBATTO D. & HERMANN J. (2003) - Zircon formation during
fluid circulation in eclogites (Monviso, Western Alps):
implicationsfor Zr and Hf budget in subduction zones.
Geochim. Cosmochim. Acta, 67, 2173–2187.
109
SESSIONE 4

SESSIONE 5
Modelli matematico-statistici nelle GeoScienze
CONVENERS
Antonella Buccianti (Università di Firenze)
Carlo Cardellini (Università di Perugia)
111
SESSIONE 5

SESSIONE 5
An analogue model of triple junction for the Neapolitan volcanism
Key words: analogical models, caldera, Phlegraean Fields.
The Phlegraean Fields, whose name recalls myths and ancient
traditions, is a volcanic complex that extends over the city of
Naples and its western surroundings; it takes up the central sector
of the Campanian Plain, a Plio–Quaternary graben which formed
during the distensive tectonic phase associated with the opening
of the Tyrrhenian basin (LUONGO et alii, 1991).
The volcanic field is constituted of two calderas, associated to
large explosive eruptions, and of several monogenic cones. The
oldest caldera is related to the Campanian Ignimbrite eruption,
the largest eruption of this area, that occurred about 39 ka B.P.,
and the youngest caldera was formed 15 ka B.P. with the
Neapolitan Yellow Tuff eruption (SCARPATI et alii, 1993).
The dating was obtained by the 40 Ar / 39 Ar method (RICCI et
alii, 2000; DE VIVO et alii, 2001; INSINGA et alii, 2004; DEINO et
alii, 2004).
Two questions arise from the analysis of the volcanic history
of the Phlegraean area: 1) genesis of volcanism of the whole
Neapolitan volcanic area; 2) actual location of the caldera
boundary of the Campanian Ignimbrite eruption.
The two points are strictly related because the mechanism of
the migration of the magma towards the surface and its
outpouring produce the present structure of the caldera.
In order to find a solution we analyzed, at first, data available
from the literature and an analytical model (LUONGO et alii,
1991) proposed for the Phlegraean Fields, and after analogical
models to simulate the process of the building up of the
Campanian Ignimbrite caldera.
An accurate analysis of the data available from the literature
showed that many authors have outlined the rim of the
Campanian Ignimbrite Caldera both on land and at sea, but
without any reliable geological constraint (ROSI & SBRANA,
1987; ORSI et alii, 1996; PERROTTA et alii, 2006) for which
concern the existence of the caldera rim at sea (BARBERI et alii,
1991; ZOLLO et al., 2003; JUDENHERC & ZOLLO, 2004).
Our research began with assumption that at the origin of the
Neapolitan volcanism there is a mantle upwelling occurring about
2 Ma B.P., associated with tensile tectonics generated by the
opening of Tyrrhenian basin: the rising plume generates a crustal
tumescence, a triple junction and a detumescence.
_________________________
(*) Dipartimento di Scienze della Terra – Università degli studi di Napoli
“Federico II”, menadalbore@libero.it, luongius@unina.it
FILOMENA D’ALBORE (*) & GIUSEPPE LUONGO (*)
112
After the check that evidences of the rising plume there are in
the Phlegraean Fields and the study of the analytical model, that
links the phlegraean caldera resurgence to a hotspot, we built two
analogue models, set by volcanological, geophysical and
geochemical constraints, in order to simulate a rising plume.
For the two models a gelatine layer was used as analogue to the
crust. According to empiric evidences, the material showed a
brittle behaviour for a temperature below +7 C and a viscous one
for a temperature above +7 °C. The difference between the
models was the type of source: in the first model, a silicon
balloon was placed at the bottom of the gelatine layer and was
slowly inflated to simulate a rising plume (Fig. 1); in the second
model, animal fat was injected in the gelatine through a conduit
in order to constrain the material during the upward migration
(Fig. 2).
The effects of two experiments were similar on the surface:
crustal tumescence, tripartite fracture and detumescence.
Fig. 1 – Analogue model by gelatine and balloon.
Fig. 2– Analogue model by gelatine and fat.

The analogue models allowed to obtain the pressure for the
overburden uplift and the triple junction by the ratio between the
lithostatic pressure of the overburden and the pressure in the
balloon, in the first model, and the ratio between the lithostatic
pressure and the pressure necessary for the ascent of the fat, in
the second model. These ratios were utilized for the Phlegraean
Fields to obtain the pressure exerted by the magmatic source.
The pressure values obtained by the analogue models are
similar to the analytical ones, confirming that the models are a
reliable representation of the examinated process.
Moreover, the analogical models were used to determine the
plume diameter, responsible of the observed deformation in the
Phlegraean Fields, and to calculate ground uplifts produced by
the same plume.
The results of the proposed analogue models show that the
Phlegraean Fields take up the centre of a triple junction whose
Fig. 3– Location of the triple junction associated to the whole Neapolitan
Volcanism. PF: Phlegraean Fields; I: isle of Ischia; V: Vesuvius; P?: Villa
Literno volcanism.
arms, arranged at about 120° from each other, are responsible of
tectonic structures of the whole Neapolitan volcanism (fig. 3).
In addition, the analogue models suggest that the caldera
formation is not due to the overburden collapse following a large
explosive eruption that empties a shallow magma reservoir, but to
erosion of conduit and widening of vents due to tephra ejection at
supersonic speed through the opening fractures.
REFERENCES
BARBERI F., CASSANO E., LA TORRE P. & SBRANA A.. (1991) -
Structural evolution of Campi Flegrei caldera in light of
volcanological and geophysical data. J. Volcanol. Geoth.
Res., 48, 33 – 49.
DEINO A..L., ORSI G., DE VITA S. & PIOCHI M. (2004) - The age
of the Neapolitan Yellow Tuff caldera – forming eruption
113
(Campi Flegrei caldera, Italy) assessed by 40 Ar/ 39 Ar dating
method. J. Volcanol. Geoth. Res., 133, 157–170.
DE VIVO B., ROLANDI G., GANS P.B., CALVERT A.., BOHRSON
W.A.., SPERA F.J. & BELKIN H.E. (2001) - New constraints on
the pyroclastic eruptive history of the Campanian volcanic
Plain (Italy). Mineral. Petrol., 73, 47–65.
INSINGA D., CALVERT A.., D’ARGENIO B., FEDELE L., LANPHERE
M., MORRA V., PERROTTA A.., SACCHI M. & SCARPATI C.
(2004) – 40 Ar/ 39 Ar Dating of the Neapolitan Yellow Tuff
eruption (Campi Flegrei, southern Italy):Volcanological and
Chronostratigraphic Implications. EGU Assembly, Nice.
JUDENHERC S. & ZOLLO A. (2004) - The Bay of Naples (Southern
Italy): constraints on the volcanic structures inferred from a
dense seismic survey. J. Geophys. Res., 109, B10312.
LUONGO G., CUBELLIS E., OBRIZZO F. & PETRAZZUOLI S.M.
(1991) - The mechanics of Campi Flegrei resurgent caldera –
a model. J. Volcanol. Geoth. Res., 45, 161–172.
LUONGO G., CUBELLIS E., OBRIZZO F. & PETRAZZUOLI S.M.
(1991) - A physical model for the origin of volcanism of the
Tyrrhenian margin: the case of Neapolitan area. J. Volcanol.
Geoth. Res., 48, 173–185.
ORSI G., DE VITA S. & DI VITO M. (1996) - The restless resurgent
Campi Flegrei nested caldera (Italy): Constrains on its
evolution and configuration. J. Volcanol. Geoth. Res., 74,
179 – 214.
PERROTTA A., SCARPATI C., LUONGO G. & MORRA V. (2006) -
The Campi Flegrei caldera boundary in the city of Naples. In
B. DE VIVO (Ed.) - Volcanism in the Campania Plain:
Vesuvius, Campi Flegrei and Ignimbrites. pp. 85 – 96.
Elsevier, New York.
RICCI G., LANPHERE M., MORRA V., PERROTTA A., SCARPATI C.
&MELLUSO L. (2000) - Volcanological, geochemical and
geochronological data from ancient pyroclastic successions
of Campi Flegrei (Italy). AGU 2000 Fall Meeting, Eos,
Transactions, American Geophysical Union, 81(48).
ROSI M. & SBRANA A. (1987) - Phlegraean Fields. CNR, Quad.
Ric. Sci., 114, 1 – 175.
SCARPATI C., COLE P.D. & PERROTTA A.. (1993) - The
Neapolitan Yellow Tuff – A large volume multiphase eruption
from Campi Flegrei, southern Italy. B. Volcanol., 55, 343 –
356.
ZOLLO A., JUDENHERC S., AUGER E., D’AURIA L., VIRIEUX J.,
CAPUANO P., CHIARABBA C., DE FRANCO R., MAKRIS J.,
MICHELINI A. & MUSACCHIO G. (2003) - Evidence for the
buried rim of Campi Flegrei caldera from 3-D active seismic
imaging. Geophys. Res. Lett., 30(19), 2002,
doi:10.1029/2003GL018173.NO.19.
SESSIONE 5

SESSIONE 5
Key words: Effective parameters, relaxation, thermoelasicity,
viscosity.
INTRODUCTION
Solid geological environments, or in other words, rocks were
never homogeneous. They always have different types of
heterogeneity, such as the inclusions of other material, pores,
cracks, and dislocations. The primary method of studying these
inclusions is the laboratory experiments. However, reliable
explanations of laboratory experiments are impossible without
theoretical research. In the mechanics of heterogeneous mediums
methods of averaging the physical fields are developed based on
the theory of random functions. Application of this method to
explain the properties of rocks is promising. Reliable
mathematical modeling of processes in rocks will draw the
correct conclusions when interpreting the data of geophysical
observations.
EFFECTIVE MECHANICAL AND PHYSICAL
PARAMETERS OF ROCKS
The problem of finding effective parameters of stochastically
inhomogeneous mediums was considered by many researchers
(SHERMERHOR, 1977; KHOROSHUN & SHCHERBAKOV, 1979;
SANCHES-PALENSIA, 1984; FEDORYSHYN, 1999). The final
formulas for averaging almost all physical parameters are
developed: elasticity modules, electrical conductivity, dielectric
and magnetic constant. In order to find all these parameters the
same approach is used – averaging of differential equations
where coefficients are unknown parameters.
r r
r
∗ r
Lu
= −f
; L u = −f
Here L is differential operator where coefficients are random
∗
functions, L is the same differential operator, but the coefficients
in it are effective parameters. All methods use the same
_________________________
Study of basic physical properties of rocks based on theory of
stochastic inhomogeneous mediums
(*) Carpatian Branch of Subbotin Institute of Geoptysics NASU,
ofedor@lviv.farlep.net
OLEKSANDR FEDORYSHYN (*)
114
approximation when fluctuations of fields within component of
medium are neglected. At application of these methods to the
geological mediums we have two problems. The first problem is
that the internal geometric structure of the environment is
unknown and application of the developed methods should
introduce empirical coefficients taken from laboratory
experiments. In this work it is proposed to link the neglecting of
fluctuations of fields with the problem of introduction of
empirical coefficients, i.e., it is proposed to introduce empirical
coefficients where fluctuations of fields are neglected. In such
way effective elastic modules, the velocity of elastic waves in
porous media and electrical conductivity are derived. And the
method of estimation of reservoir properties of rocks according to
laboratory and field observations is developed.
ELASTIC WAVES PROPAGATION IN GEOLOGICAL
MEDIUMS
The second problem is that those differential equations that
are valid for each component are not sufficiently good for
describing the geological environment in general. That is, for
rocks it is not sufficient to find effective physical parameters, we
need to have improved differential equations for describing the
behavior of rocks. In this work the process of averaging the wave
Fig.1. - Dependence of the length of the wave vector of
frequencies, taking into account non-locality.
equation takes into account non-local relations between stress and
strain. σ = C 4ε
+ C6∇∇ε
, where 4 C is fourth range tensor, C6 is
sixth range tensor. As a result we obtained differential equation
of 4-th order, which describes the distribution of four different
waves. In Figure 1 it is shown the dispersion characteristics of

these waves. As we can see, in heterogeneous mediums besides
ordinary waves (curve 1) "standing waves" appear with length of
approximately equal to the average size of non-homogeneities
and it weakly depends on frequency (curve 2). A similar
situation exists in the crystal lattice. In the atomic crystal lattice
there are only acoustic phonons, and in the diatonic lattice more
optical phonons appear.
THERMO ELASTIC PHENOMENA IN GEOLOGICAL
MEDIUMS
Thermal conductivity is also the physical quantity for which
the effective value should be determined. To do this we need to
average common system of equations of mechanics and heat
balance, using the Duhamel-Neumann law. But in this case the
evaluation of stress fluctuations is more important problem than
finding effective thermo elastic parameters. In heterogeneous
mediums the thermal stress will always occur due to different
coefficients of thermal expansion of components. Partial melt,
which exists in asthenosphere, can also be considered as a twocomponent
thermo elastic medium. Melting is a phase transition
of first sort, accompanied by the volume increasing. The region
of partial melt is at depth of 80-100 kilometers, and there is no
room for expansion, so the melting process is accompanied by the
emergence of internal overpressure. This paper evaluates the
internal pressure in asthenosphere due to partial melt. In Figure 2
it is shown the pressure dependence on the depth at heating the
medium by 2 º C.
Fig.2. - Dependence of overpressure in the partial
melt on depth.
VISCOSITY AND RELAXATION
Most of the processes taking place in geological mediums are
not subordinated to classical mechanics. A significant part of
their behavior is described by rheological properties: viscosity
and relaxation. Definition and solution of the problem of
viscoelasticity of heterogeneous environments is extremely
difficult problem that is why we can hope to find solutions only
115
for separate problems. In this paper the attempt is made to build a
common system of equations for saturated porous medium, which
would describe the liquid filtration process and relaxation of
stresses in the solid component. A two-component viscoelastic
cracked and porous medium saturated with liquid is considered.
For such medium the equations of viscoelasticity are written. For
hard part of rocks the Maxwell viscosity model is taken
d d d
σs + τσ�
s = 2μεs
, and for pore material – the Voigt viscosity
d d d
model σf
= 2 με f + ηε�
f . As a result of statistical averaging of
these equations the equation of fluid filtration is derived
K ∂p
∇p
− = 0 ,
kη
∂t
and equations for estimation of stress changes due to relaxation in
hard component of rock
d
∂σs
∗⎛
p ⎞
σs
+ τ = C ⎜ε
s + ⎟ .
∂t
⎝ K ⎠
This mathematical model can be used to define layer pressure in
the oil and gas fields.
REFERENCES
FEDORYSHYN O. (1999) – Prognozirovanie svoistv
microneodnorodnykh materialov s razlichnymi tipami
vkluchenij, (Predicting the properties of microscopically
inhomogeneous materials with different types of inclusions).
Math. Methods and Phys.-Mech. Fields. 42, 136-140.
SHERMERHOR T. (1977) – Teoria uprugosti
microneodnorodnykh sred (Theory of Elasticity of
Microscopically Inhomogeneous Media). Nauka, Moscow,
400 pp.
KHOROSHUN L. & SHCHERBAKOV A. - (1979) Prochnost i
deformativnost arbolita, (Strength and Deformability of
Arbolite). Naukova Dumka, Kiev, 191 pp.
SANCHES-PALENSIA E. (1984) Inhomogeneous media and
vibration theory. Mir, Moscow, 472 pp.
SESSIONE 5

SESSIONE 5
Transient behaviour simulation of large, explosive, and ignimbrite
forming eruptions by a multiphase thermo-fluid dynamic model
Key words: Ignimbrite-forming eruptions, multiphase dynamic
model, stratified deposits, two-dimensional numerical
simulations.
INTRODUCTION
A multiphase thermo-fluid dynamic model has been improved
to assess the effect of a range of particle size on the transient
two-dimensional behaviour of large, explosive, and ignimbrite
forming eruptions. The model accounts for mechanical and
thermal non-equilibrium conditions between a continuous gas
phase and N solid phases characterized by specific physical
properties (NERI et alii). The dynamics of the process was
simulated by adopting a grid scale approach able to resolve the
meso-scale features of the flow and the high sub-grid gas
turbulence. Viscous and interphase effects were expressed in
terms of newtonian stress tensors and gas-particle or
particle-particle coefficients (DARTEVELLE et alii). Several
numerical simulations of such collapsing explosive eruptions
were carried out. Their dynamics depict the formation of the
vertical jet, the column collapse, the building of the pyroclastic
fountain, the generation of radially spreading pyroclastic current,
and the development of thermal convective instabilities in the
fountain and in the current. The results highlight the importance
of the multiphase development of the model and describe several
mechanical and thermal non-equilibrium effects. Low
concentration zones tend to follow the dynamics of the hot
ascending gas, both in the convective plume above the fountain,
and in the propagation of the associated pyroclastic current. High
concentration parts tend to sediment mainly along the ground,
both in the proximal area for the mixing of material in the
fountain, and in the boundary layer for the loss of momentum.
DISCUSSION
Two large, explosive, and ignimbrite forming eruptions
_________________________
(*) Dipartimento di Scienze della Terra, Università degli studi di Napoli
“Federico II”, simone.lepore@unina.it
Lavoro eseguito nell’ambito del progetto “Meccanismi eruttivi, di trasporto
e deposizionali di eruzioni pliniane” con il contributo finanziario
dell’Università degli studi di Napoli “Federico II”
SIMONE LEPORE (*) & CLAUDIO SCARPATI (*)
116
Fig. 1 – A picture of a stratified pyroclastic current with a concentrated
boundary layer (from BRANNEY &KOKELAAR, 2003).
occurred during the last 40 ka in the Campi Flegrei volcanic field.
The oldest (39 ka) and largest (>300 km 3 ) is the Campanian
Ignimbrite (CI) that emplaced a grey to yellow ash deposit widely
dispersed. The general features of the CI are quite similar to the
standard ignimbrite (SPARKS et alii, 1973). The youngest is the
Neapolitan Yellow Tuff (NYT), a phreatoplinian eruptive event
(50 km 3 in DRE) occurred about 15 ka ago (DEINO et alii, 2004).
Two different depositional members (A and B) have been
identified. The member B is constituted by pyroclastic currents
deposits which form a thinly stratified succession tens of metres
thick, with hundreds of layers centimetres to metres thick
(SCARPATI et alii, 1993). This succession is composed of six
depositional units: massive, inverse-graded, regressive
sand-wave, stratified, particle aggregate, and vesicular. Vertical
and horizontal facies variations testify the unsteady and
non-uniform nature of the parental pyroclastic currents. The
stratified unit is poorly sorted and characterized by numerous
laminae whose thickness vary from a few millimetres to about ten
centimetres (COLE & SCARPATI, 1993). The thinly stratified
nature of this unit can be interpreted as the deposition product
from a concentrated boundary layer of a turbulent, stratified
pyroclastic current, where sedimentation is mainly due to traction
carpet motion (BRANNEY &KOKELAAR, 2003). For a more clear
view, in Fig. 1 a schematic picture of the dynamics of a stratified
pyroclastic current is represented, together with the associated
concentrated and traction-dominated boundary layer.

Fig. 2 – Two snapshots at 90 s and 135 s of a numerical simulation of a collapsing explosive eruption together with the associated pyroclastic current and rising
phoenix clouds around five hundred metres and between two and four kilometres.
The numerical simulations carried out recently reproduce the
behaviour of a pyroclastic current emplacing such type of
stratified units. In Fig. 2 two snapshots at 90 and 135 seconds of
a numerical simulation of a collapsing explosive eruption are
shown. After about five hundred metres, the high-concentration
(red) layer may be assimilated to the concentrated and
traction-dominated boundary layer, while the stratified and
turbulent section (orange ? blue) represents the main part of the
pyroclastic current. Closer to source, phoenix clouds start to form
because the flow system is losing its horizontal momentum. At
greater distances, other rising phoenix clouds come out for
turbulence from the high-concentrated basal part. Our final
purpose is to relate stratified ignimbrites with the simulated
turbulent pyroclastic current.
REFERENCES
BRANNEY M.J. & KOKELAAR P. (2003) – Pyroclastic density
currents and the Sedimentation of ignimbrites. Geol. Soc.
Lond. Mem., 27, 1-142.
COLE P.D. & SCARPATI C. (1993) – A facies interpretation of the
eruption and emplacement mechanisms of the upper part of
the Neapolitan Yellow Tuff, Campi Flegrei, Southern Italy.
Bull. Volcanol., 55 (5), 311-326.
DARTEVELLE S., ROSE W.I., STIX J., KELFOUN K. & VALLANCE
J.W. (2004) – Numerical modelling of geophysical granular
117
flows: Computer simulations of plinian clouds and pyroclastic
flows and surges. Geochem. Geophys. Geosys. , 5 (8), 1-36.
DEINO A.L., ORSI G., DE VITA S.&PIOCHI M. (2004) – The age of
Neapolitan Yellow Tuff caldera-forming eruption (Campi
Flegrei caldera – Italy) assessed by 40 Ar / 39 Ar dating method.
J. Volcanol. Geotherm. Res., 133 (1-4), 157-170.
NERI A., ESPOSTI ONGARO T., MACEDONIO G. & GIDASPOW D.
(2003) – Multiparticle simulation of collapsing volcanic
columns and pyroclastic flows. J. Geophys. Res., 108 (B4),
1-24.
SCARPATI C., COLE P.D. & PERROTTA A. (1993) – The
Neapolitan Yellow Tuff: A large multiphase eruption from
Campi Flegrei, Southern Italy. Bull. Volcanol., 55 (5), 343-
356.
SPARKS R.S.J., SELF S. & WALKER G.P.L. (1973) – Products of
ignimbrite eruptions. Geology, 1 (3), 115-118.
SESSIONE 5

SESSIONE 5
Application of cellular automaton model for river morphological
studies: CAESAR and the Pellice River (Piedmont, Italy)
ANTONIO PASCULLI (*), CHIARA AUDISIO (**) & GIORGIO LOLLINO (°)
Key words: CAESAR, cellular automaton model, Italy,
morphological changes, Piedmont.
INTRODUCTION
The cellular automaton concept is based on the continued
interaction of a series of local process “rules” that governs the
behavior of the entire system (WOLFRAM, 1983).
In the geomorphological contest, the basic principles of
cellular modeling are that landforms are represented by a lattice
of cells and that the interactions between cells (routing of water
and sediment for rivers) are treated using simple rules based on
abstractions of the governing physics (NICHOLAS, 2005).
The first models used in the river geomorphological contest
were applied to the braided river modeling (MURRAY &PAOLA,
1994). Then, other studies have followed, always in the river
dynamic contest, also considering alluvial fans and artificial
channels (COULTHARD et alii, 2002; THOMAS & NICHOLAS,
2002).
CAESAR, Cellular Automaton Evolutionary Slope And River
model, is a open source cellular model which can be run in two
modes: a catchment mode with no external influxes other than
rainfall; and a reach mode with one or more points through which
sediment and water enter to the system (VAN DE WIEL et alii,
2007). The CAESAR model employs a scanning algorithm that
“pushes” water across a grid to the cells in front, along four
directions (fig. 1; COULTHARD et alii, 2002 and COULTHARD et
alii, 2007). This overcomes some problem for braided and
meandering river.
The bed-load transport can be calculated with WILCOCK &
CROWE (2003) or EINSTEIN (1950) formula.
_________________________
(*) Department of Science, Università degli Studi “G. d’Annunzio” di Chieti-
Pescara, a.pasculli@unich.it
(**) CNR-IRPI U.O.S. di Torino, chiara.audisio@irpi.cnr.it
(°) CNR-IRPI U.O.S. di Torino, giorgio.lollino@irpi.cnr.it
This research began in the context of a PhD in collaboration with the
Department of Science of Chieti University and then in the context of PRIN
2007 “Present evolutionary trends and possible future dynamics of alluvial
channels in Northern and Central Italy” (national co-ordinator: Dr Nicola
Surian, University of Padua; local co-ordinator: Ing. Giorgio Lollino, CNR-
IRPI of Turin) with the economic contribution of Research and University
Minister.
118
The cellular model was applied on some part of Pellice River,
a Po River tributaries, characterized by a 905 km 2 wide drainage
basin.
Fig. 1 – Schematic representation of the scanning algorithm of CAESAR
(COULTHARD et alii, 2002)
CASE STUDY: PELLICE RIVER
The Pellice river is characterized by a single and multi-thread
pattern: wandering in the upper part and meandering in the lower,
near the Po river confluence. The river can be considered a
cobble – gravel bed in the upper part and a gravel – sand bed in
the lower, near the confluence.
The geomorphological characteristics were analyzed by indepth
studies on the planimetric variation occurred in the last one
hundred and fifty years. The studies were conducted using
historical maps (1880-1945) and aerophotographs (1945-1999).
The CAESAR simulations in reach mode request a digital
terrain model (DTM), hydrometric and discharge data and
granulometric data. The DTM has been obtained by a LiDAR
survey made on February 2007, the hydrometric data have been
acquired from both the Hydrological Annals and the regional
hydrometric service (ARPA Piemonte, the local district

Fig. 2 – Schematic cross-section along one of the studied Pellice River reach. In blue the original DTM, in green and red two different simulation: number one
without lateral erosion and the number two with lateral erosion. The distance of point along the cross-section is 1 m and the simulation time is one year.
Environmental Protection Agency). The granulometric data were
measured thanks a field survey during the 2008 summer.
Then, a census of the civil and engineering defense has been
done. The census has done both by field survey and archive
investigation.
The simulations have been done on a two-three kilometers
long river reach for a period of one year. The hydrometric data
are the measured value at one of the water gauge in the basin
(about 6 km up-stream). The erosion method use Einstein
formula, because the granulometric characteristics of the reach.
Velocity was fixed 3 m/s. the maximum erodible limit was 0.01m.
The first results point out fifty cm – one hundred cm variation
of the section due to both erosion and deposit phenomena (fig. 2).
REFERENCES
COULTHARD T.J., MACKLIN M.G. & KIRBY M.J. (2002) - A
Cellular Model Of Holocene Upland River Basin And
Alluvial Fan Evolution. Earth Surf. Proc. Land., 27, 269-288.
COULTHARD T.J., HICKS D.M. & VAN DE WIEL M.J. (2007) -
Cellular modelling of river catchments and reaches:
advantages, limitations and prospects. Geomorphology, 90,
192-207.
EINSTEIN H.A. (1950) - The bed-load function for sediment
transport on open channel flows. Technical Bulletin USDA,
Soil Conservation Service, 1026, 71.
119
MURRAY A.B. & PAOLA C. (1994) - A cellular model of braided
rivers. Nature, 371, 54-57.
NICHOLAS A. P. (2005) - Cellular modelling in fluvial
geomorphology. Earth Surf. Proc. Land., 30, 645-649.
THOMAS R. & NICHOLAS A.P. (2002) - Simulation of braided
river flow using a new cellular routing scheme.
Geomorphology, 43, 179-195.
VAN DE WIEL M.J., COULTHARD T.J., MACKLIN M.G., LEWIN J.
(2007) - Embedding reach-scale fluvial dynamics within the
CAESAR cellular automaton landscape evolution model.
Geomorphology, 90, 283-301.
WILCOCK P.R. & CROWE J.C. (2003) - Surface-based transport
model for mixed-size sediment. J. Hydraul. Eng.-ASCE,
129(2), 120-128.
WOLFRAM S. (1983) - Statistical Mechanics of Cellular
Automata. Rev. Mod. Phys., 55, 601-644.
SESSIONE 5

SESSIONE 5
Key words: Diffusion, kaolinite, mathematical modeling,
sodalite.
Sodalite [Na4(AlSiO4)3Cl]2 experimental synthesis was here
performed in alumina crucibles at 850°C and ambient pressure by
the mixing of kaolinite plus NaCl. A continuous loss in weight of
the NaCl plus metakaolinite starting matrix contained in the
alumina crucible heated in oven was testified and attributed to Cl
vaporization. An analytical mathematical model to solve the
parabolic differential equation related to the chlorine diffusion
processes occurring within the crucible has just been proposed in
a previous paper (in press). The comparison between the
experimental data and the theoretical results was satisfactory
enough. Even so, a better matching has been pursued through an
improvement of the analytical expression.
In the previous paper, the solution of a simple differential
equation with homogeneous Newmann condition, related to the
diffusion of Cl mass through a truncated cone (the crucible) and
then released to the oven atmosphere, was selected. The
following was the expression of the Cl mass released to the oven
atmosphere at the time τ after the start of the transient (STRANG,
1986; ZWILLINGER, 1986) :
=
⎪⎧
⎡
( )
( − )
( )
( − ) ( − ) ( − ) ⎤⎪⎫
⎨ − ∑ − ⎢ ⋅ − ⋅ −
⎥⎬
⎪⎩
⎢⎣
⎥⎦
⎪⎭
∞
M(
τ ) rel
n
n 2
π
2
n −λ
D 1 2 B b 1 B b
n τ
M 0 1
1 e
B h 2 h b 2
3
2
3
4
2h
V n= 0
λn
λn
λn
where 0
An empirical-analytical mathematical model to simulate the loss in
weight of Cl during the synthesis process of sodalite by the use of
meta kaolinite
(1)
M was the total inventory of Cl mass, assumed available
1 2
2
inside the crucible; while V h(
B + Bb + b )
= π was the
12
volumetric capacity of the crucible, considered as a truncated
cone; ‘ B ’ and ‘b’ were, respectively, the diameter of the major
( 2n + 1)
π
and minor base of the cone, and λn
= , n = 0,
1,
2,
3...
2h
were the eigenvalues associated to eigenfunctions cos( λnx)
(ZWILLINGER, 1986). The order of the magnitude of diffusion
coefficient D (assumed constant as a first step), has been assumed
________________________
(*) Dipartimento di Scienze, Università D’Annunzio, Chieti,
apasculli@unich.it.
(**) Dipartimento di Geotecnologie per l’Ambiente ed il Territorio,
Università D’Annunzio, Chieti, dnovembre@unich.it.
ANTONIO PASCULLI (*) & DANIELA NOVEMBRE (**)
120
equal to 10 -9 m 2 /s. The series, in the above relation, has been
truncated at the 10 th term, because of the decreasing exponential
numerical values with the increasing order of the eigenvalue λ n .
Experimental data and numerical results, when compared,
although satisfactory enough, suggest the necessity of some
modelling improvements. Fig. 1 shows the comparison between
experimental data and the results obtained by expression (1) for
different values of diffusion coefficient D. It is evident that the
assumption of a simple diffusion of Cl through the crucible, in
order to describe experimental data, is able to provide only poor
results.
weight lost (g)
2,5
2,0
1,5
1,0
0,5
experimental data and analytical results
experimental data
numerical results:
[D] =m 2 /s
D =1.1x10 -9
D =1.5x10 -9
D =2.0x10 -9
D =2.5x10 -9
0,0
0 100 200
time (hour)
300 400
Fig. 1 –Comparison among eexperimental data and analytical solution
of a simple diffusion differential equation.
After about 120 hours, the best results has been obtained
−9
2
assuming D = 2.
5×
10 m / s . Before that time, however, lower
diffusion coefficient values are more suitable to match
experimental measures. As a consequence, a simple diffusion
equation appeared to be not well suitable to numerically describe
this kind of phenomena. Thus the attempt was to modify directly
the analytical solution in order to achieve a better matching
between experimental measures and analytical results. The first
attempt to modelling this kind of phenomena through a simple
diffusion differential equation was based on the assumption that
all the Cl atoms were free to diffuse through the NaCl matrix
contained in the crucible. This hypothesis subtends another
assumption: the entire matrix of NaCl molecules was at a
temperature over the Cl ionization temperature since the transient
(and the subsequent set of experimental measures) started. Just
only two are the parameters that can be changed: diffusion
coefficient and the actual free Cl gas availability inside the NaCl

matrix during the transient. First we employed a time variable Cl
mass inside the matrix and free to diffuse. The following
expression was assumed:
−BF
⋅τ
M () τ avail = M tot ⋅ ( 1−
e )
(2)
M τ was the total Cl mass inside the NaCl matrix
Where ( ) avail
that at the instant τ has been converted into free gas and has
been available to diffuse through the matrix; M tot (2.56 g) was
the total mass of Cl contained in whichever form inside the NaCl
matrix; BF coefficient was related to conductive-convective
thermal conditions of the matrix respectively inside and on the
surface of the crucible, through Biot and Fourier adimensional
numbers, (KREITH, 1973). A physical justification of expression
(2) could be provided by considering a non complete crucible
heating at 850°C.
−BF
⋅τ
Thus M 0 ≡ M () τ avail = M tot ⋅ ( 1−
e ) expression has been
introduced into equation (1):
M(
τ )
M
tot
rel
≅
⋅(
1 − e
−B
⎪⎧
⋅τ
π
) ⎨1
−
3
⎪⎩ 2h
V
n ( −1)
( B ⋅ h)
n
( B − b)
( −1)
( B b)
⎡ τ
2
−
⎢
− 2 h ⋅ b − 2
2
3
4
⎢⎣
λn
λn
λ
10
2
n −λn
D
∑ ( −1)
e
n= 0
n
(3)
Then some parametric studies have been carried out to select the
optimal numerical parameter values of both BF and D, in order
to acquire the best matching among experimental data and semi
analytical results. The first numerical experiments suggested the
−6
−1
employment of the following values BF = 5.
× 10 s , for all
the simulations carried out.
weight lost (g)
2,5
2,0
1,5
1,0
0,5
experimental data and analytical results
experimental data
analytical results [D] = m 2 /s:
Variable conc Mfree =1.5 g; D =variable
Variable conc Mfree =1.5 g; D =2.5x10 -9
0,0
0 100 200
time (hour)
300 400
Fig. 2 – Final comparison among experimental data and numerical
results.
Thus the diffusion coefficient was increased from
−9
2
−9
2
D = 1.
1×
10 m / s up to D = 2.
5×
10 m / s improving the
quality of the matching, but even so, the results were not very
satisfactory yet within the entire range. Some further parametric
studies suggested that an improvment would has been obtained if
the curve was homothetically translated up. By a physical point
of view, a reasonable and suitable assumption, aimed to justify
this “mathematical” operation, was to suppose that some Cl mass
was already available to diffuse freely through the matrix, just
2
⎤⎪⎫
⎥⎬
⎥⎦
⎪⎭
121
since the start of transient. It means that the expression (2) and
consequently the expression (3), should be substituted by:
−BF⋅τ M = M τ = M − M ⋅ 1−
e + M
(4)
0
() ( tot free ) ( ) free
avail
where M free was supposed to be the Cl mass already free to
diffuse since the transient start. This assumption improved
significantly the capability of the model to match experimental
data for the first 100 hours as it is shown, in Fig. 2, by “clear
triangle up” line with = 1.
5g
. The same figure shows the
M free
comparison between the model with M = 2.
56 g and
−9
2
D = 2.
5×
10 m / s (both constant for the entire transient,
“dark triangle down”) and the experimental data. At the 100 th
hour, the experimental plot displays a steeper trend. This
behaviour could be explained supposing that, at that time, the
actual diffusion coefficient was higher than the value assumed
carrying out the previous numerical calculations. Thus, within
that time range, a raising of diffusion coefficient was supposed.
In Fig. 3, both diffusion coefficient and Cl available mass trend
have been displayed.
diffusion coefficient D/10 -9 (m 2 /s)
3,4
3,2
3,0
2,8
2,6
2,4
diffusion coeff (D)
available Cl mass
D
parameters
( ) [ ] ⎟ ⎟
2
−9 = × ⎜
−2
τ m / s 2.
5 10 1+
7.
× 10 × e130×
3600
2 ( m / s)
2.
5
D =
−6 −5×
10 ⋅τ
()[ τ g]
= 1.
06×
( 1−
e ) 1.
5
M avail +
( ) [ ] ⎟ ⎟
2
−9 = × ⎜
−2
τ m / s 2.
5 10 1+
7.
× 10 × e 130×
3600
0 100 200
time (hours)
300 400
Fig. 3 – Implemented key parameters
D
Through the last improvement, based any way on physical
considerations, a very good matching between experimental data
and numerical simulations has been achieved, as it is shown in
Fig. 2 (“clear circle” vs “dark triangle down”).
⎛
⎜
⎝
REFERENCES
KREITH F. (1973) - Principles of Heat Transfer. Dun-Donnelley
Publishing Corporation New.
STRANG G. (1986) - Introduction to Applied Mathematics. Wellesley-
Cambridge Press U.S.A.
ZWILLINGER D. (1986) - Handbook of Differential Equations. Academic
Press, Inc.
⎛
⎜
⎝
0
−τ
⎞
⎠
τ
⎞
⎠
2,8
2,6
2,4
2,2
2,0
1,8
1,6
1,4
available Cl mass inside crucible (g)
SESSIONE 5

SESSIONE 5
Key words: Digital terrestrial photogrammetry, distinct elements
numerical methods, laser scanning, marble quarry, stability
analysis.
INTRODUCTION
The knowledge of the structural setting of slopes is essential
when considering the stability in rock exploitation planning. In
addition to the physical-mechanical properties of the intact
material and its discontinuities, the analysis of stability requires
information about the geometrical-structural setting of slopes and
joints.
Physical-mechanical parameters are derived from in situ and
laboratory tests, while geometrical characteristics traditionally
derive from direct attitude measurements on the field. If
accessibility problems do not allow direct measurement of
discontinuity surfaces by traditional geological methods, data are
achievable only by statistical approaches; unfortunately, this is
useless for deterministic analysis of slopes characterized by
appreciable outcrops and evident joint systems.
In such cases, Laser Scanning (LS) represents a useful
technique that allows detailed surveys of the geometricalstructural
setting even in inaccessible sites. Moreover Digital
Terrestrial Photogrammetry (DTP) can be used for the
interpretation of shadows and for the identification of bolts,
previous installed in the slope, unappreciable in the point clouds
from LS.
The equipment necessary for the photogrammetric survey can
be arranged either on an aerostatic balloon, an helicopter or an
Unmanned Aerial Vehicle (UAV) so that, through vertical strips
of acquisition, it is possible to obtain a complete stereoscopic
viewing of the slopes.
All this deterministic information, integrated by data from
fieldwork, such as geological-engineering surveys, and material
and joints properties, allows the application of distinct elements
_________________________
Application of distinct elements methods for rocky slope stability
analysis in the Carrara Marble District (Apuan Alps)
SILVIA RICCUCCI (*), RICCARDO SALVINI (*), MIRKO FRANCIONI (*) & EMILIO MACHETTI (**)
(*) Dipartimento di Scienze della Terra, Università di Siena,
riccucci8@unisi.it
(**) Copernico SRL, Montalcino, Siena, machemil@libero.it
122
methods for the slope stability analysis. Moreover, the
combination of these updated techniques of survey and analysis,
consents to obtain several information to be used for the risk
mapping and hazard mitigation in quarries.
DATA ACQUISITION AND ANALYSIS
The present paper describes the acquisition and processing
procedures of data performed by LS and DTP, aimed to the study
of quarry fronts stability through the distinct elements numerical
methods. The quarry, located in the Carrara Marble District, is
about 150 meters wide and over 100 meters high and it is made
up by Ordinario and Venato marbles (Lower-Middle Lias – Fig.
1).
Data coming from LS surveys has been elaborated in order to
create the Digital Dense Slope Model (DDSM), from the points
cloud, and from it to compute the slopes attitude and joints
attitude, spacing and persistence (Fig. 2a). With the aim of
carrying out a preliminary kinematic analysis, the joints attitude
has been statistically analyzed by the use of Dips software
(Rocscience TM ).
Fig.1 – LS in a marble quarry of the Apuan Alps.
Then, in order to assess the accuracy of the adopted
methodology for the extraction of geometrical info from LS and
DTP, the joint systems resulted from statistical analysis have
been compared with those from the geological-engineering
survey. These last have been carried out in accessible and safe

Fig. 2 – a: Example of topographic profile (blue) and discontinuity systems (red) obtained by DDSM and DTP. b: Example of displacement vectors and Factor
of Safety calculated from the UDEC simulation.
quarry areas whit the aim of getting the physical-mechanical
properties of intact material and its discontinuities necessary to
calculate the mass rock shear strength.
The areas verified by fieldwork represent 1/10 of the
extension of the total study zone (the one acquired by LS and
DTP); this fact confirms the evident advantage of the use of such
modern technologies for getting geometrical-structural data for
the whole slope.
From the processing of the DDSM, 14 topographic profiles
have been created. These profiles have been drawn toward the
directions correspondent to the more probable movements of
sliding blocks; such directions have been gained thank to the
kinematic stability analysis previous performed.
The stability analysis of the slope has been done through
UDEC 4.0 software (Universal Distinct Element Code -
ITASCA TM ).
For every profile, within UDEC environment, all the
engineering-geological parameters necessary for the
characterization of the quarry fronts has been inserted. Then,
from the simulation of the probable movements of blocks and the
calculation of the Factor of Safety (Fig. 2b), it has been possible
to compute the displacement velocity and the stress conditions.
Results indicate that most part of the slope is stable even if, in
some cases, the simulation shows displacements that are
symptomatic of a precarious stability; there, it could be necessary
to rapidly plan the installation of stabilization works.
Moreover, it has been possible to determine the important
contribute of the bolts previous installed in the slope; in many
areas, the simulation without them, has pointed out a condition of
instability.
123
SESSIONE 5

SESSIONE 5
Slope stability analysis and rock fall simulation for the assessment of
geological risk of a railroad line
Key words: Digital terrestrial photogrammetry, laser scanning,
limit equilibrium method, rock fall simulation.
INTRODUCTION
With the increasing awareness to the geological risks, the
study of slope stability plays a key role in the Earth Sciences,
especially in areas of high vulnerability for the presence of
infrastructures and human activities.
These issues require an accurate study of the geological
processes based on several independent or integrated
measurements techniques; nowadays, Digital Terrestrial
Photogrammetry (DTP) and Laser Scanning (LS), together with
the necessary geological-engineering measurements about intact
material and joints, are the principal techniques used for the slope
stability analysis.
These methodologies, in addition to the advent of modern
calculation systems, consent to carry out accurate and
deterministic rocky slopes stability analysis and to simulate the
rock falls useful for the risk zonation and mitigation.
STABILITY ANALYSIS AND ROCK FALL SIMULATION
The present paper describes the rock slope stability and
runout analysis of rocky unstable blocks on a slope, 500 m wide
and 600 m high, overhanging the railroad line Domodossola –
Iselle (Fig. 1).
In addition to the traditional geological, geomorphological
and engineering–geological surveys, DTP has been used to
perform a detailed analysis of rocky blocks sited in inaccessible
areas. The stereopairs acquisition has been done by means of an
helicopter.
In order to accomplish the investigation, DTP has been
combined with LS with the aim of creating the DDSM (Digital
Dense Surface Model) of the slope.
Aims of the work are the assessment of the rock falls
potentially dangerous for the railroad line, of the efficiency of
_________________________
(*) Dipartimento di Scienze della Terra, Università di Siena,
salvinir@unisi.it
RICCARDO SALVINI (*), MIRKO FRANCIONI (*) & SILVIA RICCUCCI (*)
124
existing protection measures and the prompt of mitigation and
monitoring strategies.
In order to collect the exact position and size of blocks and
wedges, a digital interpretation of stereopairs coming from DTP
has been carried out. Subsequently, the stereorestitution of
blocks and discontinuity surfaces has allowed to obtain all the
necessary data for the computation of stability, performed by
limit equilibrium methods (Rocplane and Swedge - Roscience TM ).
The photointerpretation has been also used to realize the land
cover map (ex. outcropping rock, soil covered by vegetation) and
to recognize the mitigation and protection measures already
installed to be used as input data in the runout analysis.
Starting from blocks position the DDSM has allowed to
determine the most probable trajectories of rock falls along the
slope (Fig. 2a). These have been calculated by means of a GIS
procedure by the use of the ArcHydro module of Esri TM ArcMap
assuming a correspondence between probable trajectories and
flowdirection (Fig. 2a).
Fig.1 – Rock slope overhanging the railroad line Domodossola – Iselle
The morphologic profile of rock falling paths has been
obtained by the interpolation of 3D points coming from a
properly procedure developed inside Esri TM Arcinfo Workstation
environment integrated with the Easy Profiler tool of Esri TM
ArcMap.
The physical-mechanical characteristics of blocks, the
morphologic profile, the land cover and the location of the
protection barriers (classified according to the height – from 2 to
4 m – and to the preservation status), have been used as input

Fig. 2 – a: Example of the most probable trajectory of a rock fall along the slope. b: Example of a rockfall simulation along the profile and graphical results of
end points and kinetic energy along the falling path
data in RocFall2D (Roscience TM ) software to calculate the
runout.
Local slope land cover has been managed by a statistical
approach utilizing the coefficient of normal and tangential
restitution; in this way, probabilistic results about rock fall end
point and kinetic energy along the falling path and on the barriers
have been obtained (Fig. 2b).
Considering the railroad line proximity, the analysis has
shown the high probability to reach the train track for some
unstable block. Some other ends their fall mainly in
correspondence of vegetated and less steep areas; the remaining
blocks are stopped by the existing protection measures.
Results from this work have allowed the hazard zoning in
respect to the railway; moreover, comparing them with results
coming from the rock slope stability analysis it has been possible
to suggest the proper protection methods in different areas.
125
SESSIONE 5

SESSIONE 5
126

SESSIONE 6
Ofioliti del sistema Appennino - Corsica - Alpi
Occidentali
CONVENERS
Alessandra Montanini (Università di Parma)
Luca Pandolfi (Università di Pisa)
127
SESSIONE 6

SESSIONE 6
The Middle Triassic to Late Jurassic ophiolites along the Albania to
Greece geotraverse: a tool for the reconstruction of the Mesozoic to
Tertiary tectonic history of Dinaric-Hellenic Belt
VALERIO BORTOLOTTI (°), MARCO CHIARI (°), MICHELE MARRONI (*) (°) LUCA PANDOLFI (*) (°),
GIANFRANCO PRINCIPI (**) (°) & EMILIO SACCANI (°°)
Key-words: Albania, back-arc, fore-arc, ophiolites, Greece,
Mesozoic, obduction, subduction, Tertiary.
INTRODUCTION
The Dinaric-Hellenic Belt is an Alpine collisional belt which
extends from Slovenia to the southern Greece. This belt is
derived from the collision between the Adria Plate and the
southern Eurasia Macroplate that resulted by the closure, due to
subduction, of the interposed Vardar Ocean (BORTOLOTTI et alii,
2005 and quoted references).
Many models about the tectonic evolution of the Dinaric-
Hellenic Belt have ben proposed (see for instance the discussion
in the recent papers provided by SCHMID et alii., 2008 and
ROBERTSON et alii, 2009). A valuable tool to check the different
geodynamic models is represented by the stratigraphic,
geochemical and tectonic features of the ophiolites.
To provide valuable contributions to the scientific debate, a
study of the different ophiolite sequences cropping out along the
Albania to Greece geotraverse is provided. In addition, a
geodynamic model is proposed according to the collected data.
THE OPHIOLITE SEQUENCE ALONG THE ALBANIA
TO GREECE GEOTRAVERSE
Along the Albania to Greece geotraverse, three main domains
can be identified; the lowermost is represented by the units
derived from the Adria continental margin, that are overlain by
the units of the Vardar Domain, i.e. an assemblage of oceanic and
continental units, that in turn, are overlain by the continental units
________________________
(°) Istituto di Geoscienze e Georisorse, CNR, valerio.bortolotti@geo.unifi.it
(*) Dipartimento di Scienze della Terra, Università di Pisa
(**) Dipartimento di Scienze della Terra, Università di Firenze
(°°) Dipartimento di Scienze della Terra, Università di Ferrara
Lavoro eseguito nell’ambito del progetto PRIN con il contributo finanziario
dell’Università di Ferrara, Firenze e Pisa.
128
of the Serbo-Macedonian-Rhodope Massif, regarded as
representative of the deformed western margin of the Eurasia
Macroplate. The Vardar Domain belongs several ophiolite units,
that are distributed along two main alignment, i.e. the External
(EOB) and Internal ophiolite (IOB) belt, that are in turn separated
by the tectonic window where the Pelagonian-Korab units is
exposed. The ophiolitic units include coherent oceanic sequences
of different age and geodynamic significance, but also slices of
metamorphic sole and ophiolite-bearing mélanges, referred as
sub-ophiolite mélange.
Thus, the western alignment (EOB) include the Mirdita, South
Albania, Pindos, Koziakas and Otrys, Vardoussia and Argolis
ophiolitic units, whereas to the eastern one (IOB) are referred as
the Vourinos, Evvia, Almopias and Guevgueli ophiolitic units.
The latter alignment represents the most internal ophiolites of the
Dinaric-Hellenic Belt. Sum up all the features from IOB and
EOB allows a reconstruction of an overall picture of the
geological setting of the ophiolites along the Albania to Greece
geotraverse. The reconstructed setting includes, from bottom to
the top: 1) a ophiolite-bearing sub-ophiolite mélange; 2) Middle
to late Triassic MOR ophiolites, strongly deformed under very
low-grade metamorphism; 3) Middle Jurassic MOR-IAT
ophiolites that represent a fore-arc oceanic basin opened inside a
MOR trapped crust; 4) Middle Jurassic IAT ophiolites that
represent a fore-arc oceanic basin; 5) BABB ophiolites
(Guevgueli ophiolites) of uppermost Middle Jurassic age. Both
the MOR-IAT and IAT ophiolites show a metamorphic sole at
their base, whereas MOR and BABB ophiolites do not display
evidences of metamorphic sole. In addition, the BABB ophiolites
are thrust onto the Paikon unit, that is intepretd as a remnants of a
Middle Jurassic continental arc. In turn, the BABB ophiolites are
thrust by the continental units of the Serbo-Macedonian-Rhodope
Massif.
THE PROPOSED MESOZOIC TO TERTIARY TECTONIC
HISTORY OF THE DINARIC-HELLENIC BELT
The history started in the Early Triassic with a rifting stage
followed by the Middle to Late Triassic MOR (TOP in Fig.1)
oceanic opening (Vardar Ocean) between the Adria (including
the Pelagonian-Korab unit) and the Eurasia continental margin.

Subsequently, in the Early Jurassic, the MOR oceanic basin was
affected by convergence resulting into the development of an
intraoceanic east-dipping (present-day coordinates) subduction
zone, where the role of the lower and upper plates were played,
Fig. 1 – Bidimensional reconstruction of the Mesozoic to Tertiary tectonic
history of the Dinaric-Hellenic belt.
respectively by Adria and Eurasia Plates. This event originated in
the Middle Jurassic a wide supra-subduction zone, consisting of
an IAT oceanic basin (JOb in Fig.1) opened in a MOR trapped
crust (JOa in Fig.1). This suprasubduction zone was bounded to
the west by an accretionary wedge, whose remnants are
represented by the slices of Middle to Late Triassic MOR
ophiolites. In the Middle Jurassic, the subduction of oceanic
lithosphere was still active with a progressive retreat of the slab.
As consequence, a fore-arc oceanic basin opened in the
lowermost Middle Jurassic into the trapped MOR oceanic crust,
whose remnants are represented by the MOR- and IAT-related
magmatic sequences. In the same time, a continental volcanic arc
(Paikon arc) developed in the westernmost border of the Eurasian
plate. Soon after, the extension in the intra-continental back-arc
129
area resulted in the production of BABB ophiolitic sequences
(JOc in Fig.1) associated with calc-alkaline magmatism
(Guevgueli ophiolites). The extension in the Guevgueli back-arc
was most likely favoured by strike-slip tectonics. The continuous
convergence resulted in the involvement of the Pelagonian
continental crust (Adria) in the subduction. This event produced a
sharp shifting from extension to compression in the suprasubduction
zone, leading to the obduction of the oceanic
lithosphere, in two different stages, respectively the intraoceanic
and continental phases (GAGGERO et alii, 2009). The
intraoceanic stage (Middle-Late Jurassic boundary) was
characterized by the westward thrusting of young and still hot
section of the oceanic lithosphere leading to development of
metamorphic soles. The continental stage (Late Jurassic-Early
Cretaceous) was characterized by the emplacement of the
ophiolitic nappe onto the continental margin. In the same time
span, the compression, that affected also the volcanic arc and the
neighbouringh marginal oceanic basin, resulted along the
Albania-Greece geotraverse into a continental collision. From
Late Cretaceous to Late Miocene the progressive migration of the
deformation front toward the Adria Plate developed. In this
frame, the root of the fore-arc-derived ophiolite nappe (EOB and
IOB) can be today identified in the Vardar domain. In the Middle
to Late Miocene, an extensional tectonics occurred in the internal
zones of the Dinaric-Hellenic belt, while the compression was
still active in the westernmost areas of the Adria Plate. Thus, the
Pelagonian-Korab tectonic window, i.e. a core of continental
crust units cropping below the ophiolites from EOB and IOB, can
be interpreted as the result of the Tertiary extensional tectonics
that affected the internal areas of the Dinaric-Hellenic Belt.
REFERENCES
BORTOLOTTI V., MARRONI M., PANDOLFI L. & PRINCIPI G.,
(2005) - Mesozoic to Tertiary tectonic history of the Mirdita
ophiolites, northern Albania. The Island Arc, 14, 471-493
GAGGERO L., MARRONI M., PANDOLFI L. & BUZZI L. (2009) -
Modelling of oceanic lithosphere obduction: constraints from
the metamorphic sole of Mirdita ophiolites (Northern Albania).
Ofioliti, 34, 17-43.
ROBERTSON A.H.F., KARAMATA S. & SARIÇ K., (2009) -
Overview of ophiolites and related units in the Late Palaeozoic–
Early Cenozoic magmatic and tectonic development of Tethys in
the northern part of the Balkan region. Lithos, 108, 1-36.
SCHMID S.M., BERNOULLI D., FÜGENSCHUH B., MATENCO L.,
SCHEFER S., SCHUSTER R., TISCHLER M. & USTASZEWSKI K.,
(2008) - The Alpine-Carpathian-Dinaridic orogenic system:
correlation and evolution of tectonic units. Swiss Journal of
Geoscience, 101, 139-183.
SESSIONE 6

SESSIONE 6
Radiolarian ages and geochemical data on the ophiolites from the
Koziakas massif (Greece)
MARCO CHIARI (°), VALERIO BORTOLOTTI (°), MARTA MARCUCCI (*), ADONIS PHOTIADES (**),
GIANFRANCO PRINCIPI (*)(°) & EMILIO SACCANI (***)
Key-words: Basalts, Greece, morb, Middle-Late Triassic,
ophiolites, radiolarians, Koziaka.
INTRODUCTION
The Koziakas massif, located at the western boundary of the
Thessaly plain, consists of a stack of thrust units emplaced
westward onto the Pelagonian s.l., which in turn thrusts onto the
Eocene Pindos Flysch. The dismembered units of the Koziakas
are unconformably overlain by the Oligocene-Miocene molasse
of the Mesohellenic trough (SACCANI et alii, 2003; POMONIS et
alii, 2005).
THE OPHIOLITIC TECTONIC UNITS
In the Koziakas massif, at the top of the “Pelagonian”
succession, three ophiolitic tectonic units crop out.
a) the “Mélange and Fourka Units”. At the base of the Fourka
Unit scattered outcrops of ophiolite-bearing mélange crop out.
The Fourka Unit consists of thrust sheets and blocks of pillow
lavas locally covered by radiolarian cherts.
b) an “Ophiolite Unit”, consists of slivers of sheared
serpentinites, locally containing dunite bodies, plagiogranite and
boninite dykes.
All volcanic rocks studied herein come from the “Fourka
Unit” and consist of basalts and basaltic andesites. Six samples
display a clear alkaline affinity and are similar to the alkaline
within-oceanic plate (WPB) and are interpreted to have generated
in a seamount setting. Two samples display similarities with
enriched MORB (E-MORB) and are interpreted as formed from a
N-MORB type mantle source slightly enriched by a plume
component during the early stage of oceanic spreading or in an
off-axis oceanic setting.
We examined 32 samples for radiolarian analyses. The
assemblages of the samples collected near the WPBs indicate a
Middle and a Late Triassic age, while the radiolarites collected
near the E-MORBs indicate a Late Triassic age.
_________________________
(°) CNR, Istituto di Geoscienze e Georisorse, marco.chiari@unifi.it
(*) Dipartimento di Scienze della Terra, Università di Firenze
(**) Institute of Geology and Mineral Exploration (IGME), Athens, Greece
(***) Dipartimento di Scienze della Terra, Università di Ferrara
130
CONCLUSION
The occurrence of Late Triassic WPBs and E-MORBs point
out for the existence of an oceanic setting in which the N-MORB
asthenospheric source was influenced by a plume-type
component and resulted in the off-axis eruption of enriched
alkaline basalts and enriched MORB-type basalts. This
conclusion is in agreement with similar results obtained from
other sectors of the Hellenide ophiolites. During the post-Late
Jurassic compressive tectonic phase, which affected the Internal
Hellenides, the Mélange and Ophiolitic Units tectonically
overthrust the “Pelagonian” continental margin represented by the
sedimentary units of the Koziakas Massif. During the post-Late
Eocene compressive tectonic phase all these units were refolded
and thrust southwestwards onto the Eocene Pindos Flysch.
REFERENCES
POMONIS P., TSIKOURAS B. & HATZIPANAGIOTOU K. (2005) -
Geological evolution of the Koziakas Ophiolitic complex
(western Thessaly, Greece) .
Ofioliti, 30 (2), 75-84.
SACCANI E., PHOTIADES A. & PADOA E. (2003) - Geochemistry,
petrogenesis and tectono-magmatic significance of volcanic
and subvolcanic rocks from the Koziakas Mélange (Western
Thessaly, Greece). Ofioliti, 28 (1), 43-57.

Key words: Calabrian Arc, cold subduction, Diamante-
Terranova ophiolite, lawsonite blueschists.
The Diamante-Terranova unit is part of the Northern
Calabrian Arc nappe stack and consists of HP-LT
metamorphosed rocks with an ophiolitic affinity. The basement
rocks are characterized by the interlayering of blue and green
metabasites; this is observed at different scale and marks a
pervasive foliation. The blue layers preserves a pristine blueschist
facies mineralogical assemblage made of Na-amphibole
+lawsonite +Na-pyroxene +chlorite +phengite +titanite
+pumpellyite +quartz +calcite; the green layers consist of of Naamphibole
+Na-Pyroxene+ epidote +lawsonite +chlorite
+phengite +titanite +pumpellyite +quartz +calcite, they have been
previously interpreted as a greenschist-facies overprint (CELLO et
alii, 1996; ROSSETTI et alii, 2004; LIBERI et alii, 2006). The
preservation of a pristine blueschist facies mineralogical
assemblage, characterized by the presence of fresh lawsonite, is
not a common feature in the Western Mediterranean orogens and
is not consistent with a greenschist facies overprint. New
petrological, geochemical and microstuctural studies were
performed in order to unravel this problem.
On the base of the obtained data, the blue layers are referred
to lawsonite-blueschists and the green layers are referred to
epidote-blueschists, both reaching 1.0 GPa, P at about 380°C, T
during the metamorphic climax. Geochemical characterization of
the two layers pointed out different bulk rock composition, in
particular the Fetot enrichment and the Si depletion in the
epidote-blueschist, implying differences in the protolith
composition. This fact determined the coexistence of two
different chemical microdomains that led to the development of
different prograde blueschist paragenesis in the green and blue
layers at the same P-T conditions.
_________________________
The Diamante-Terranova retrograde lawsonite blueschist
(Calabrian Arc): an Alpine P-T cold exhumation path
FRANCESCA LIBERI (*), DAVID SHIMABUKURO (**), EUGENIO PILUSO (*), JOHN WAKABAYASHI (°) &
WALTER ALVAREZ (**)
(*) Dipartimento di Scienze della Terra, Università della Calabria,
e.piluso@unical.it
(**) Department of Earth and Planetary Sciences, University of California,
Berkeley
(°) Department of Earth and Environmental Sciences, California State
University, Fresno
131
In both green and blue layers, the retrograde path is
characterized by the blastesis of a late lawsonite, growing at high
angle on the HP mineralogical assemblage, followed by a
pumpellyite-actinolite facies overprint. Lawsonite pseudomorphs
are frequently reported from the Alpine belt as a relict phase of
the prograde metamorphism or the peak pressure mineralogical
assemblage. In constrast, lawsonite of the Diamante-Terranova
ophiolite unit is fresh and growths during the retrogression path,
replacing epidote as the late stable Ca-Al silicate and suggesting a
counterclockwise path. Accordingly, detailed microprobe
analysis on Na-amphibole displays triple core-rim zonation with
crossite cores (NaAm1), glaucophane mantles (NaAm2), and
crossite rims (NaAm3). In particular, increasing AlVI contents
followed by decreasing AlVI indicate prograde burial and
retrograde exhumation path. At the same time, the gradual
decrease in AlIV content from cores to rims indicates
temperature decrease.
Differences in the bulk composition of the protolith led to
formation of two different peak metamorphic paragenesis for the
epidote-blueschists and lawsonite-blueschists. The
decompression path followed a very cool geothermal gradient, in
contrast with the other ophiolite units cropping out within the
Calabrian Arc and the Western Mediterranean orogens,
characterized by an isothermal decompression and a greenschist
facies overprint during their exhumation.
REFERENCES
CELLO G., INVERNIZZI C., & MAZZOLI S. (1996) - Structural
signature of tectonic processes in the Calabrian Arc,
southern Italy: Evidence from oceanic-derived Diamante-
Terranova unit. Tectonics, 15 (1), 187-200.
LIBERI F., MORTEN L. & PILUSO E. (2006) – Geodynamic
significance of ophiolites within the Calabrian Arc. Isl. Arc,
15, 26-43.
ROSSETTI F., GOFFÈ B., MONIÈ P., FACCENNA C. & VIGNAROLI G.
(2004) - Alpine orogenic PT-t-deformation history of the
Catena Costiera area and surrounding regions (Calabrian
Arc, southern Italy): The nappe edifice of north Calabria
revised with insights on the Tyrrhenian-Apennine system
formation. Tectonics, 23.
SESSIONE 6

SESSIONE 6
Tectono-magmatic evolution of the External Ligurian mantle section
(Northern Apennine, Italy)
ALESSANDRA MONTANINI (*), RICCARDO TRIBUZIO (**) & MATTHEW THIRLWALL (°)
Key words: ophiolite, subcontinental mantle, pyroxenite,
Northern Apennine, rifting
In the External Ligurian units, ophiolites consist of slices of
exhumed subcontinental mantle, basalts and rare gabbroic rocks.
These ophiolites are associated with continental crust rocks,
locally retaining primary relationships. This association was
interpreted as a fossil ocean-continent transition along a nonvolcanic
continental margin (MARRONI et alii, 1998; TRIBUZIO et
alii, 2004; MONTANINI et alii, 2008). The mantle exhumation
occurred through high-T ductile deformations developed along
hectometre-size shear zones, followed by a polyphase brittle
deformation under decreasing temperature conditions, coupled
with hydration and formation of serpentine, carbonate and Fe-Ni
sulphide cataclasites (MONTANINI et alii, 2006). The External
Ligurian mantle section represents a tectonic sampling of deep
levels of subcontinental lithosphere and provides a good
opportunity of throwing light into structural and compositional
modifications of subcontinental lithospheric mantle in response to
the extensional processes leading to the formation of an oceanic
basin.
The External Ligurian peridotites occur as decametre- to
kilometre-size bodies and include (i) porphyroclastic spinel
tectonites showing incipient re-equilibration in the plagioclase
facies (RAMPONE et alii, 1995); (ii) plagioclase-facies mylonites
with spinel tectonite relics (MONTANINI et alii, 2006), (iii) coarse
granular rocks enriched in plagioclase as a result of interaction
with asthenospheric melts (PICCARDO et alii, 2004). The
peridotites locally retain extremely depleted Nd-Sr isotope
compositions, coupled with Proterozoic Os model ages
(RAMPONE et alii, 1995; SNOW et alii, 2000). The spinel-facies
assemblage of the peridotites is characterized by Na2O and
Al2O3-rich clinopyroxene with slight LREE depletion, spinel with
low Cr# and by the presence of disseminated Ti-rich amphibole.
Taken as a whole, the External Ligurian peridotites were
considered to represent relatively fertile MORB-type mantle
accreted to the lithosphere in Proterozoic times (RAMPONE et alii,
1995). However, an increasing number of observations and recent
studies (e.g. LE ROUX et alii, 2007; SOUSTELLE et alii, 2009)
_________________________
(*) Dipartimento di Scienze della Terra, Università di Parma,
alessandra.montanini@unipr.it
(**) Dipartimento di Scienze della Terra, Università di Pavia
(°) Department of Geology, Royal Holloway, University of London (UK)
132
show that lherzolite massifs may be the result of multiple
refertilization events during or before their emplacement. The
occurrence of different types of pyroxenites, the widespread
amphibole formation and the evidence of interaction with
asthenospheric melts during their shallow evolution seem in
agreement with this notion.
The peridotite plagioclase mylonites include garnet
clinopyroxenites and orthopyroxene-rich websterites layers
showing Opx + Spl ± Cpx symplectites after Mg-rich garnet
(MONTANINI et alii, 2006). The garnet clinopyroxenites, in
particular, record an early stage of equilibration in the
subcontinental lithosphere at high P (~2.8 GPa) and temperature
conditions (~1150°C). They provided Sm-Nd and Lu-Hf
isochrons testifying a retrograde, rifting-related history of slow
cooling in the plagioclase stability field between 220 and 186
Ma, which followed the decompression from the garnet stability
field (MONTANINI et alii, 2006). The plagioclase mylonites may
have formed by an extensional shearing event related to
lithospheric “necking stage” caused by the ascent of underlying
asthenosphere, as predicted by numerical, analogue and
conceptual models of formation of non-volcanic-rifted margins
(WHITMARSH et alii, 2001; MICHON &MERLE 2003).
The garnet clinopyroxenites are Al2O3- and FeO-rich mafic
rocks with moderate to extreme LREE depletion, positive Eu-Sr
anomaly and nearly flat MREE and HREE. They also include
rocks lacking Eu anomaly which display a gradual increase from
LREE to HREE and high amounts of Sc and V. The websterites
have high mg#, Cr and Ni values, similar or slightly lower than
those of enclosing peridotites. The websterite REE patterns,
subparallel at higher concentration levels to those of the
peridotites, have moderate LREE depletion. Clinopyroxenes from
both websterites and peridotites display slight LREE
depletion, positive Eu anomalies and nearly flat HREE. The
petrogenesis of garnet clinopyroxenites may be related to
recycling of crustal plagioclase-bearing mafic protoliths that
underwent variable degrees of partial melting in the garnet
stability field or to high pressure cumulus processes from melts of
recycled crust, whereas melt-rock reaction may be a viable
process to explain the websterite origin. In particular, the
websterite petrogenesis is consistent with peridotite replacement
by olivine-undersaturated melts through olivine consumption and
pyroxene ± garnet forming reactions. Reactions at lower
melt/rock ratio may have also caused peridotite refertilization. In
addition, a later infiltration of silica-undersaturated melts under

spinel facies conditions, preceding ductile stretching and
dispersion of pyroxenites into the host peridotite, is evidenced by
orthopyroxene-consuming reactions in both websterites and
peridotites, generally associated with crystallization of Tipargasite
+ olivine ± clinopyroxene ± Ni-rich sulphides.
Most pyroxenites have TDM(Nd) and TDM(Hf) younger than
the exhumation age, thus arguing for fractionation of Sm/Nd and
Lu/Hf ratios related to the Mesozoic rifting. Nd-Hf isotope
compositions recalculated for the minimum age of fractionation
vary in a wide range (ε Nd = +4.3 to +12.6, ε Hf = + 2.8 to +
31.5). Most samples, however, fall close or slightly below the
mantle array. The observed isotope heterogeneity presumably
reflects protoliths of different ages crystallized from MORB-type
to slightly enriched melts. Local preservation of highly radiogenic
Hf compositions in the pyroxenites may be attributed to an older
fractionation event involving garnet-bearing lithologies. Nd-Hf
isotopic compositions of clinopyroxenes from the peridotites and
websterites vary from the low end of MORB range to slightly
enriched compositions.
The coarse granular peridotites enriched in plagioclase of the
External Liguride domain are characterized by large plagioclase
patches replacing spinel, clinopyroxene porphyroclasts replaced
by orthopyroxene + plagioclase or rimmed by orthopyroxeneplagioclase
symplectites, and gabbroic microgranular pods. These
peridotites also show the successive intrusion of gabbros to
basalts. Clinopyroxenes from the plagioclase-enriched peridotites
have concave upward REE patterns, Eu-Sr negative anomalies
and significant REE and Zr enrichment with respect to the
porphyroclastic clinopyroxenes of rocks unaffected by
impregnation. The geochemical features of the impregnated
peridotites were most likely due to interaction with low-degree
fractional melts of a MORB-type source (PICCARDO et alii, 2004;
MÜNTENER et alii, 2010).
The subcontinental mantle bodies from External Ligurian
units preserve evidence for entrainment of crustal rocks testified
by rare relics of garnet pyroxenites which were likely derived
from plagioclase-rich mafic cumulates. The fertile nature of the
External Ligurian mantle is attributed to superposition of several
refertilization events under decreasing P-T conditions: (i)
formation of the orthopyroxene-rich websterite layers through
pyroxene-forming reactions and olivine consumption involving
olivine-undersaturated melts (pyroxenite-derived liquids and/or
asthenospheric melts?); (ii) infiltration of silica-undersaturated
melts at spinel facies conditions leading to crystallization of Tiamphibole
+ olivine ± clinopyroxene; (iii) percolation and
impregnation by MORB-type melts in the plagioclase stability
field.
REFERENCES
133
LE ROUX V., BODINIER J.L., TOMMASI A., ALARD O., DAUTRIA
J.M., VAUCHEZ A., & RICHES A.J.V. (2007) - The Lherz spinel
lherzolite: Refertilized rather than pristine mantle. Earth
Planet. Sci. Lett., 259, 599-612.
MARRONI M., MOLLI G., MONTANINI A. & TRIBUZIO R. (1998) -
The association of continental crust rocks with ophiolites in
the Northern Apennines (Italy): implications for the
continent-ocean transition in the Western Tethys.
Tectonophysics, 292, 43-66.
MICHON, L. & MERLE, O. (2003) - Mode of lithospheric
extension: conceptual models from analogue modelling.
Tectonics, 22, 1028
MONTANINI A., TRIBUZIO R. & ANCZKIEWICZ R. (2006) -
Exhumation history of a garnet pyroxenite-bearing mantle
section from a continent–ocean transition (Northern
Apennine ophiolites, Italy). J. Petrol., 47, 1943–1971.
MONTANINI A., TRIBUZIO R. & VERNIA L. (2008) - Petrogenesis
of basalts and gabbros from an ancient continent–ocean
transition (External Liguride ophiolites, Northern Italy)
Lithos, 101, 453-479
MÜNTENER O., MANATSCHAL G., DESMURS L. & PETTKE T.
(2010) - Plagioclase Peridotites in Ocean–Continent
Transitions: Refertilized Mantle Domains Generated by Melt
Stagnation in the Shallow Mantle Lithosphere. J. Petrol., 51,
255 - 294.
PICCARDO G.B., MÜNTENER O., ZANETTI A. & PETTKE, T. (2004)
- Ophiolitic peridotites of the Alpine-Apennine system: mantle
processes and geodynamic relevance. Int. Geol. Review, 46,
1119-1159.
RAMPONE E., HOFFMANN A.W., PICCARDO G.B., VANNUCCI R.,
BOTTAZZI P. & OTTOLINI L. (1995) - Petrology, mineral and
isotope geochemistry of the External Liguride peridotites
(northern Apennine, Italy). J. Petrol., 36, 81-105.
SNOW J.E., SCHMIDT G. & RAMPONE E. (2000) - Os isotopes and
highly siderophile elements (HSE) in the Ligurian ophiolites,
Italy. Earth Planet. Sci. Lett., 175, 119-132
SOUSTELLE V., TOMMASI A., BODINIER J. L., GARRIDO C. J. &
VAUCHEZ A. (2009) - Deformation and Reactive Melt
Transport in the Mantle Lithosphere above a Large-scale
Partial Melting Domain: the Ronda Peridotite Massif,
Southern Spain. J. Petrol., 50, 1235 - 1266
TRIBUZIO R., THIRLWALL M. & VANNUCCI R. (2004) - Origin of
the gabbro-peridotite association from the Northern
Apennine ophiolites (Italy). J. Petrol., 45, 1109-1124.
WHITMARSH R.B., MANATSCHAL G. & MINSHULL T.A. (2001) -
Evolution of magma-poor continental margins from rifting to
seafloor spreading. Nature, 413, 150-154.
SESSIONE 6

SESSIONE 6
Key words: Northern Apennines, stratigraphy, tectonic evolution.
The Val Marecchia Nappe, cropping out in the upper Tiber,
Savio, Marecchia and Foglia valleys, constitutes the highest
tectonic unit of the North-eastern Apennines, overthrusting both
Tuscan and Umbro-Marchean Units. The nappe, made up of a
Meso-Cenozoic mainly pelitic and calcareous succession with
interbedded ophiolite-derived olistoliths, breccias and sandstones,
has been ascribed to the most eastern zone of the External
Ligurian Domain, located close to the Adria margin (Calvana
Supergroup or Monte Morello Unit). However, some authors
considered the Calvana Supergroup as belonging to the Subligurian
Domain, because its stratigraphic succession is quite
similar to those of the Sub-ligurian Units, the latter originated
from the thinned continental crust of the westernmost part of the
Adria plate.
Actually, the stratigraphic succession of the Val Marecchia
Nappe is debated. It has been generally considered to start with a
Base Complex, consisting of several Upper Cretaceous-middle
Eocene dominantly pelitic formations, which laterally and
vertically grade one into another.
Upwards, the Base Complex formations are followed by the
Eocene Monte Morello Fm, comprising up to 700 m of marly,
marly-calcareous and calcareous turbidites, with interbedded
minor thin siliciclastic turbidic beds.
Recently, PLESI et alii (2002) recognized, in the western side
of the upper Tiber Valley, Mid-Upper Jurassic-Lower Cretaceous
ocean-derived magma-tic and sedimentary rocks, that upwards
grade into the Base Complex formations of the Val Marecchia
Nappe.
Researches, carried out in the Tiber and Marecchia valleys,
allowed to recognize for the Val Marecchia Nappe a continuous
stratigraphic succession, consisting, from bottom to top, of: a)
magmatic substratum, made up mainly of more or less
serpentinized peridotites, cut by gabbro dykes, and by minor
basalts and magmatic breccias; b) radiolarites; c) Calpionella
_________________________
The stratigraphic succession of the Val Marecchia Nappe: insights
into the paleogeographic and tectonic evolution of northern
Apennines
(*) Dipartimento di Scienze Geologiche, Tecnologie Chimiche e
Ambientali, Università di Urbino, vincenzo.perrone@uniurb.it
(**) Dipartimento di Scienze della Terra, Università “Federico II” di
Napoli
(***) Badley Ashton and Associates Ltd., Winceby, Horncastle, LN9 6PB,
Lincolnshire (United Kingdom).
VINCENZO PERRONE (*), PAOLA DE CAPOA (**), ANGELIDA DI STASO (**),
SONIA PERROTTA (***) & VALENTINA TIBERI (*)
134
limestones; d) Palombini shales; e) Sillano Fm; f) Monte Morello
Fm; g) Argille Varicolori Fm; h) Monte Senario Sandstone Fm.
Biostratigraphic data point out a systematic re-working of
very abundant Cretaceous to Eocene foraminifers and coccoliths,
that co-exist with taxa indicating younger ages. The Sillano Fm
reaches the late Eocene, the Monte Morello Formation is
Oligocene in age and upwards continues with the upper
Oligocene-lower Aquitanian Argille Varicolori Fm, followed by
the lower Miocene Monte Senario Sandstone Fm.
This succession is quite similar to those characterizing the
Sicilide Complex of Southern Apennines and the Flysch Basin
Complex of the Maghrebian Chain from Sicily to Gibraltar
Straits, and was accreted to the Paleo-Apenninic Chain only
starting from the early Miocene. Consequen-tly, the Val
Marecchia nappe succession - and maybe the whole Sub-ligurian
Complex - deposited in an oceanic realm, different from the
Ligurian domain and located in a more external paleogeo-graphic
position, constituting the northwards continuation
of the Maghrebian Flysch Basin-Lucanian
Ocean system.
REFERENCES
PLESI G., GALLI M. & DANIELE G. (2002) – The Monti Rognosi
Ophioliitc Unit (cfr. Calvana Unit Auct.) paleogeographic
position in the Ex-ternal Ligurian Domain, relationships with
the tectonic units derived from the Adriatic margin. Boll. Soc.
Geol. It., Vol. Spec. 1, 273-284.

Middle Jurassic radiolarian fauna from the cherts in Skenderbej
region (Central Albania)
Key words: Jurassic, radiolarian cherts.
The radiolarian assemblages described here come from
sections Skenderbej 1 and Skenderbej 2, which belong
respectively, to the platformic and pelagic continental formations
situated at the eastern periphery of Shebeniku ophiolitic unit.
The section Skenderbej 1 is localized about 300 meters in the
north of Skenderbej1 village (near to Librazhdi city, central
Albania). The section consist of:
Stromatolitic limestone, capped by hardground
Radiolarian chert (about 6 m thick)
Ophiolitic breccias
3 samples are taken: Sk3, Sk4 and Sk5 respectively, 1m, 1.8m
e 5.8 m above the limestone; but only sample Sk5 yielded a well
preserved radiolarian fauna. The samples have been etched with
hydrofluoric acid at different concentrations. The complete faunal
assemblages from sample Sk5 is the seguent:
Sample Sk5: Eucyrtidiellum semifactum Nagai & Mizutani;
Eucyrtidiellum unumaense s.l. (Yao); Parvicingula dhimenaensis
s.l. Baumgartner; Tricolocapsa sp. cf. T. sp. S. (BAUMGARTNER
et alii, 1995); Tricolocapsa conexa Matsuoka; Tricolocapsa
plicarum s. l. Yao; Tricolocapsa plicarum ssp. A.
(BAUMGARTNER et al., 1995); Theocapsomma cordis Kocher;
Unuma sp. A. (Baumgartner et al., 1995).
The age of sample Sk5 is 5 U.A.Z. or Late Bajocian-Early
Bathonian due to the coexistence of Eucyrtidiellum semifactum
and Tricolocapsa plicarum ssp. A.
The section Skenderbej 2 is localized in the south of Rajca
village, near to Bushtrica river. This section consist of:
Pelagic cherty limestone, capped by hardground
Radiolarian cherts; in this level limestone intercalation are
also present “Blocks in matrix” melange.
Sample Sk2, which is taken about 4 meters above the
limestones, yielded a poor radiolarian fauna. The age of this
sample is 5-8 U.A.Z. or Late Bajocian- Early Bathonian to Late
Callovian- Early Oxfordian due to the presence of Eucyrtidiellum
unumaense pustulatum.
_________________________
(*) Polytechnic University of Tirana, Earth Sciences Department,
mensiprela@yahoo.com
MENSI PRELA (*)
135
REFERENCES
BAUMGARTNER,P.O,BARTOLINI, A.C., CARTER, E.S., CONTI,M.,
CORTESE G., DANELIAN, T.,DE WEVER, P.,DUMITRICA, JUD
R., GORICAN, S.,GUEX G., HULL, D.,KITO, N.,MARCUCCI
M., MATSUOKA A., MURCHEZ B., O,DOGHERTY L., SAVARZ
L., VISHNEVSKAJA V., WIDZ, D&YAO A., 1995.- Middle
Jurassic to Early Cretaceus radiolarian of Tethys :
occurrences, systematics, biochronology. Mem. Geol.,
Lausanne, 23, 1013-1048.
SESSIONE 6

SESSIONE 6
Key words: Jurassic, radiolarian cherts.
INTRODUCTION
The radiolarian cherts of Jurassic age occur to a limited extent
in the Kosova area (KNOBLOCK &LEGLER, 2006). They are
exposed in the northern part of Vardari zone, onto the Rahoveci
ophiolite unit (Çupeva village), in Nerodima region, in Vrella and
Istogu area (in Nord of Skutari-Pec Line) and in Drenovc village
(near the source of Drini i Bardhe river) (fig. 1).
In Vardari zone, radiolarian cherts occur about 1 km in the
South of Selance village. They are characterized by reddish 3 to
12 cm thick chert beds, sometimes alternating with red shale
interlayer. Radiolarian cherts lie on the top of volcanic rocks
(MORB type) and are overlain by olistostrome formation. The
age of olistostrome formation is related to Late Jurassic.
The Rahoveci ophiolite unit represents the northern
continuation of Mirdita ophiolite. (ELEZAJ & KODRA, 2008).
Different from Vardari zone, in the Rahoveci area (Çupeva
village), radiolarian cherts rest unconformably on both the
“blocks in matrix” mélange (Simoni mélange) and the rocks of
mantelic provenance, which are in tectonic contact with Simoni
mélange.
In Nord of Skutari-Pec Line, (in Vrella and Istogu mountains)
and in the Nerodima region, occur the Upper Triassic –Lower
Jurassic neritic carbonate rocks. At the top, this carbonatic
formation show an erosional surface (hardground). This
continental succession is capped by Jurassic radiolarian cherts.
In the section of Drenovc village (source of Drini i Bardhe
river), radiolarian cherts (about 100 m thick), rest conformably
on the Middle Triassic-Early Jurassic cherty limestones.
_________________________
Occurrence of Jurassic radiolarian cherts in Kosova region
(*) Polytechnic University of Tirana, Earth Sciences Department,
mensiprela@yahoo.com
MENSI PRELA (*)
136
Fig. 1 - Localisation of radiolarian chert sections in Kosova region.
REFERENCES
KNOBLOCH A. &LEGLER C. (2006) – Geological map of Kosovo
1: 200 000
ELEZAJ Z. &KODRA A. (2008) – Gjeologjia e Kosoves. Studim
monografik.

Interplay between tectonic and magmatic events during exhumation
of a gabbro-peridotite section to the seafloor
(Internal Ligurian ophiolites)
Key words: Exhumation, gabbro-peridotite section, internal
Ligurian ophiolites, mantle lherzolites, pyroxenites.
The Scogna-Rocchetta Vara ophiolite (Internal Ligurian units,
Northern Apennine) is attributed to an intra-oceanic domain of
the Jurassic Ligure-Piemontese basin and is characterised by the
lack of the basalt flow layer, similar to many magma-poor
segments from (ultra-)slow spreading ridges (e.g. KELEMEN et
alii. 2007). The mantle sequence of the Scogna-Rocchetta Vara
ophiolite consists mostly of spinel facies lherzolites with
tectonitic to mylonitic fabric. The chemical compositions of
porphyroclastic clinopyroxene from these lherzolites document a
depleted geochemical signature, similar to what found by
RAMPONE et alii (1996) and PICCARDO et alii (2004) for another
mantle sequence of Internal Ligurian ophiolites. The lherzolites
locally include thin pyroxenite layers, which are boudinaged and
elongated concordantly with respect to the foliation of host rocks.
The origin of the pyroxenites is attributed to infiltration of
MORB-type melts under spinel facies conditions. In addition, the
lherzolites contain a high modal proportion of plagioclase, which
commonly forms micro-veins that are oriented nearly parallel to
the spinel facies foliation of host rocks. These veinlets show that
the decompression of the mantle sequence to plagioclase facies
conditions was associated with melt impregnation by silicaoversatured
melts. The lherzolite structures are locally replaced
by dunite bodies, which include spinel trails that are oriented
nearly concordant with the contact with host lherzolites and their
foliation. These dunites are interpreted to derive from pyroxene
reactive dissolution by silica-undersaturated melts. The mantle
ultramafics are crosscut by two generations of gabbroic bodies,
which both retain a MORB-type geochemical signature. The first
is represented by olivine-rich gabbroic dykes that are nearly
parallel to the mantle structures and display diffuse contacts with
host peridotites. These dykes are post-dated by sills made up of
clinopyroxene-rich gabbro, which show sharp planar boundaries
and crosscut at a high angle the foliation of host peridotites. The
formation of the gabbroic sills is most likely associated with the
_________________________
_________________________
(*) Dipartimento di Scienze della Terra, Università di Pavia,
alessio.sanfilippo@dst.unipv.it
(*) Dipartimento di Scienze della Terra, Università di Pavia
(**) Dipartimento di Scienze della Terra, Università di Pavia & C.N.R. -
Istituto (**) di Dipartimento Geoscienze e di Georisorse, Scienze della Unità Terra, di Pavia)
Università di Pavia & C.N.
Istituto di Geoscienze e Georisorse, Unità di Pavia)
ALESSIO SANFILIPPO (*) & RICCARDO TRIBUZIO (**)
137
building of a huge gabbroic pluton (up to 400 m thick) that
intrudes the mantle sequence. The gabbroic pluton mostly
consists of clinopyroxene-rich gabbros and minor olivine-gabbros
to troctolites. Gabbros to troctolites are locally characterised by a
weak modal and/or grain size layering, which is nearly parallel to
the orientation of the gabbroic sills. The gabbroic pluton contains
up to 80 m thick bodies made up of olivine-rich troctolites and up
to 50 m thick mantle lenses. The structural and compositional
features of these mantle lenses reveal the same origin and
exhumation-related history of the mantle sequence enclosing the
gabbroic pluton. In particular, the structures of the mantle lenses
and the mantle sequence are geometrically concordant. The
clinopyroxene-rich gabbros from the gabbroic pluton are in
places characterised by a ductile shear foliation that forms a low
angle with respect to the igneous layering. The ductile
deformation evolution comprises early re-crystallisation of
clinopyroxene and plagioclase (± Ti-pargasite) at T ~850 °C,
followed by an amphibolite facies event associated with
development of hornblende and plagioclase at T ~700 °C. The
gabbroic pluton is finally crosscut by basalt dykes with chilled
margins, which form a high angle with respect to the igneous
fabric of host gabbros. The basalt dyking represents the last event
of injection of MORB-type melts that occurred during
exhumation of studied section to the seafloor.
REFERENCES
RAMPONE E., HOFFMAN A.W., PICCARDO G., VANNUCCI R. &
OTTOLINI L. (1996) - Trace element and isotope geochemistry
of depleted peridotites from an N-MORB type ophiolite
(Internal Liguride, N.Italy). Contrib. Mineral. Petrol. 123, 61-
76.
PICCARDO G., MUNTENER O., ZANETTI A. & PETTKE T. (2004) –
Ophiolitic peridotites of the Alpine–Appenine system: mantle
processes and geodynamic relevance. Int. Geol. Rev. 46,
1119–1159.
KELEMEN P.B., KIKAWA E., MILLER D.J. & PARTY, S.S. (2007).
Leg 209 summary: Processes in a 20-km-thick conductive
boundary layer beneath the Mid-Atlantic Ridge, 14°–16°N.
In: Kelemen P.B., Kikawa E. & Miller D.J. (Eds.) - Proc.
ODP Sci. Results, 209, 1–33.
SESSIONE 6

SESSIONE 6
Metadolerites from the Frido Unit ophiolites (Southern Apennine):
oceanic and orogenic evolution
Key words: Frido Unit, HP/LT metamorphism, metadolerite
dykes, ocean-floor metamorphism, ophiolites, Southern
Apennine.
GEOLOGICAL OUTLINE AND OPHIOLITES IN THE
SOUTHERN APENNINE CHAIN
The Southern Apennine Chain is a fold-and-thrust belt,
formed between the upper Oligocene and the Quaternary ages
(PATACCA &SCANDONE 2007 and references therein), resulting
from the convergence between African and European plates and
the simultaneous rollback of the SE-directed Ionian subduction
(GUEGUEN et alii, 1998; CELLO &MAZZOLI 1999; DOGLIONI et
alii, 1999). The Apennine accretionary wedge is related to the
northward subduction of an Alpine Tethys sea floor remnant, also
known as western Tethys (BORTOLOTTI &PRINCIPI 2005) below
European plate since Oligocene times. In late Miocene, the slab
rollback reached another oceanic remnant in the Ionian sea region
represented by the westernmost part of the Neotethys Ocean
(STAMPFLI et alii, 2002). The ophiolitic sequences, which are part
of the southern Apennines, are remnants of the Ligurian sector
lithosphere of the Jurassic western Tethys which. The Liguride
tectonic units are derived from the western Tethys Ocean which
separated the European plate from the African one. These units
extensively crop out in the southern Apennines, especially in the
north-eastern slope of the Pollino Ridge. They consist of
sedimentary sequences ranging from the Upper Jurassic to the
upper Oligocene ages and several bodies of oceanic and
continental crust. These sequences are divided up into different
tectonic units some of which show a very low to low-grade
metamorphic overprint (VEZZANI, 1969).
The ophiolitic rocks occurring in the Frido Unit consist of
serpentinites derived from mantle lherzolites and, subordinately,
harzburgites. Serpentinites are frequently associated with
metagabbros, metabasalts with a relict pillow structure
(LANZAFAME et alii, 1979; SPADEA, 1982; 1994) as well as with
tectonic slices made of diabase and medium-to high grade
metamorphic rocks (such as amphibolites, gneisses, and
granofels). The metasedimentary rocks of this unit form a
MARIA T. CRISTI SANSONE (*)
138
sequence of shales, quartzarenite, and limestone. The ophiolites
of the North Calabria Unit (BONARDI et alii, 1988) consist of
metabasalts, mostly pillow lavas and pillow-breccias, crosscut by
rare diabase dikes. The sedimentary cover is made up of
radiolarian cherts and marly limestone (LANZAFAME et alii,
1979). In the Timpa delle Murge-Timpa Pietrasasso area
(LANZAFAME et alii, 1978), the most complete ophiolitic
sequence cropping out on the Calabrian–Lucanian boundary can
be observed.
METADOLERITES
Metadolerites occur as dikes cutting through serpentinized
peridotites. Metadolerites have different kinds of texture
reflecting various degree of crystallinity and strain: porphyritic or
aphyric, intersertal/intergranular, blastophitic, cataclastic to
mylonitic. In all metadolerites, primary plagioclase and
clinopyroxene are preserved. The metamorphic mineral
assemblage consists of brown amphibole, green amphibole,
chlorite, blue amphibole, pumpellyite, prehnite, quartz, epidote,
white mica, lawsonite and plagioclase (Pl2 and Pl3). Accessory
phases are opaque minerals, Fe-hydroxides and zircon.
Metadolerites are cross- cut by veins filled with pumpellyite,
chlorite, prehnite, tremolite, plagioclase, white, mica, quartz,
lawsonite, epidote and zircon.
The veins are straight, a few millimetres in thickness and
occur isolated or in closely spaced sets. The vein morphology
ranges from planar to sinuous and irregular. On the basis of
metamorphic mineral phases three different types of metadolerite
can be distinguished: i) rocks with a high content of prehnite
crystals in cataclastic–mylonitic bands, exhibiting an intersertal
or a blastophitic texture or a mylonitic fabric and in some cases a
seriate texture; ii) rocks with brown horneblende showing an
intersertal or a blastophitic texture or a partially blastophitic and
foliate texture in one specimen; iii) rocks with brown horneblende
and blue amphibole with an intersertal or a blastophitic texture.
Primary clinopyroxene is replaced by brown and green
amphiboles interpreted as being of oceanic origin; brown
amphiboles show Mg-hastingsite, edenite, pargasite, Fehastingsite,
Mg-horneblende and tschermakite compositions,
whereas green amphiboles show Mg-hastingsite, hastingsite,
edenite, Mg-horneblende, tschermakite and Fe-tschermakite
compositions. Other minerals developed in the amphibolite facies
conditions are: oligoclase, titanite and apatite. The blue

amphiboles have a winchite and barroisite composition and are
interpreted as being originated during the early stages of the
orogenic metamorphism, since they rim the oceanic brown and
green amphiboles.
The mineral assemblage of orogenic metamorphism is typical
of the LT-blueschist facies conditions and consists of
glaucophane, Mg-riebeckite, lawsonite, phengite, pumpellyite and
aegirine-augite.
Bulk-rock composition of metadolerites suggests that
protoliths of the mafic rock have a N-MORB-type affinity. Carich
metadolerites are affected by ocean-floor rodingitic
alteration, whereas Na-rich metadolerites show a spilitic
alteration.
The study of metadolerites from the Frido Unit shows
evidence of the entire evolution from their origin in the ocean
floor to their emplacement in the accretionary wedge. Textural
and mineralogical observations suggest that the metadolerites of
the Frido Unit have been affected by both ocean-floor
metamorphism under amphibolite to greenschist facies and
subsequent orogenic metamorphism under relatively HP/LT
conditions. The HP/LT orogenic metamorphism reflecting
underplating of the ophiolitic suite at the base of the Liguride
accretionary wedge during subduction produced mineral
assemblages typical of the lawsonite-glaucophane facies. Such
polyphase metamorphic evolution has been entirely preserved in
the metadolerites, probably in response to inhomogeneous
deformation within the Apennine accretionary wedge.
REFERENCES
BONARDI G., AMORE F.O., CIAMPO G., DE CAPOA P., MICONNET
P. & PERRONE V. (1988) - Il Complesso Liguride Auct.: stato
delle conoscenze attuali e problemi aperti sulla sua evoluzione
Pre - Appenninica ed i suoi rapporti con l’Arco Calabro. Mem.
Soc. Geol. It., 41, 17-35.
CELLO G. & MAZZOLI S. (1999) - Appenine tectonics in southern
Italy: a rewiew. Journal of Geodinamics, 27, 191-211.
DOGLIONI C., GUEGUEN E., HARABAGLIA P. & MONGELLI F.
(1999) - On the origin of west-directed subduction zones and
applications to the western Mediterranean. In: Durand B., Jolivet
L., Horváth F. &. Séranne M.. Eds, The Mediterranean basins:
Tertiary Extension withing the Alpine Orogenen. Geological
Society, London, Special Publications, 156, 541-561.
GUEGUEN E., DOGLIONI C. & FERNANDEZ M. (1998) - On the
post-25 Ma geodynamic evolution of the western Mediterranean.
Tectonophysics, 298, 259-269.
LANZAFAME G., SPADEA P. & TORTORICI L. (1978) -
Provenienza ed evoluzione dei Flysch Cretacico-Eocenici della
regione Calabro-Lucana. II: Relazioni tra ofioliti e Flysch
139
Calabro-Lucano. Ofioliti, 3, 189–210.
LANZAFAME G., SPADEA P. & TORTORICI L. (1979) - Mesozoic
Ophiolites of Northern Calabria and Lucanian Apennine
(Southern Italy). Ofioliti, 4 ,173-182.
PATACCA E. & SCANDONE P. (2007) - Geology of the Southern
Apennines. In: Mazzotti A., Patacca E. &. Scandone P. Eds.,
Results of the CROP Project, Sub-project CROP-04 Southern
Apennines (Italy). Boll. Soc. Geol. It., Spec. Issue, 7, 75-119.
SPADEA P. (1982) - Continental crust rock associated with
ophiolites in Lucanian Apennine (Southern Italy). Ofioliti, 7,
501-522.
SPADEA P. (1994) - Calabria-Lucania ophiolites. Boll. Geofis.
Teor. Appl., 36, 271-281.
STAMPFLI, G.M., BOREL, G.D., MARCHANT, R. & MOSAR, J.
(2002). Western Alps geological constraints on western Tethyan
reconstructions. In: Rosembaum G. & Lister G. S., Eds.,
Reconstruction of the evolution of the Alpine-Himalayan Orogen.
J. Virtual Expl., 8, 77-106.
VEZZANI L. (1969) - La Formazione del Frido (Neocomiano-
Aptiano) tra il Pollino ed il Sinni. Geol. Rom., 8, 129-176.
SESSIONE 6

SESSIONE 6
Spl-peridotites from the Frido Unit ophiolites (Southern Apennine):
evidence for oceanic metamorphism
MARIA T. CRISTI SANSONE (*), GIACOMO PROSSER (*), GIOVANNA RIZZO (**) & PAOLA TARTAROTTI (°)
Key words: Frido Unit, ocean-floor metamorphism, ophiolite,
serpentinite, Southern Apennine.
GEOLOGICAL SETTING
The southern Apennine chain is a fold-and thrust belt formed
between the upper Oligocene and Quaternary as a result of the
convergence between the African and European plates (PATACCA
&SCANDONE, 2007, and reference therein) and a simultaneous
SE-directed rollback of the Ionian subducting lithospere
(DOGLIONI et al., 1999; GUEGUEN et alii,, 1998; STAMPFLI et alii,
2002). The ophiolitic sequences, which are part of the Southern
Apennines, are remnants of the Ligurian oceanic lithosphere
pertaining to the Jurassic western Tethys.
The ophiolites crop out in the north-eastern slope of the
Pollino Ridge (Calabria-Lucania border zone) and are enclosed
within remnants of the Liguride accretionary wedge now
incorporated in the Southern Apennine chain.
The Liguride Units of the Southern Apennines include
sequences characterized by HP/LT metamorphic overprint in the
Frido Unit (VEZZANI, 1969) and sequences lacking orogenic
metamorphism in the North-Calabria Unit (BONARDI et alii,
1988). The ophiolitic rocks occurring in the Frido Unit include
serpentinites derived from a lherzolitic to harzburgitic mantle, as
suggested by and petrographical and microstructural features.
The serpentinites are frequently associated with tectonic slices
and dykes composed of diabase and medium to high-grade
metamorphic rocks such as amphibolites, gneisses, granofels as
well as of gabbros and pillow basalts.
_________________________
(*) Dipartimento di Scienze Geologiche, Università degli Studi della
Basilicata - Potenza, mariacristisansone@virgilio.it
(**) Dipartimento di Chimica, Università degli studi della Basilicata -
Potenza.
(°) Dipartimento Scienze della Terra, Università degli studi di Milano.
140
Mafic and ultramafic rocks, with garnet-bearing felses,
amphibolites, gneiss and granitoides occur as tectonic slices
within a matrix mainly composed of calcschists and phyllites
(LANZAFAME et alii., 1979; SPADEA, 1982, 1994).
SERPENTINITES
The studied serpentinites of the Frido Unit show mesh and
xenomorphic textures. Primary mantle minerals are represented
by olivine, orthopyroxene, clinopyroxene and spinel.
Pseudomorphic minerals are serpentine, magnetite and tremolite.
Olivine is replaced by serpentine forming a mesh texture;
orthopyroxene is mostly altered to bastite and in some cases
shows exsolution lamellae of clinopyroxene and kink bands.
Clinopyroxene is armoured by a tremolite rim. Spinel shows a
holly-leaf habit (MERCIER &NICOLAS, 1975) and is often rimmed
by Cr-chlorite. The core of the analyzed spinel has a Cr-Al spinel
composition corresponding to chromite (Al2O3 = 29-31 wt.%;
Cr2O3 = 28-37 wt.%), whereas the rim has a Fe-Cr spinel
composition corresponding to ferritchromite (Al2O3 = 1-2 wt.%;
Cr2O3 = 28-30 wt.%). The Cr-Al spinel/ferritchromite ratio may
be various in different spinel porphyroclasts. Serpentine has a
fibrous stretched subidiomorphic habit, it is colourless or pale
green. Tremolite is present as nematoblasts associated with
orthopyroxene. Magnetite replaces spinel or occurs within the
mesh textured serpentine.
The metamorphic assemblages in the Frido Unit serpentinites
allowed to infer the physical conditions operating during
serpentinization. The mineralogical assemblages found are
typical of the amphibolite facies, greenschist-amphibolite
transition and greenschist facies conditions. Serpentinites are cut
by veins filled with mineralogical assemblages typical of
prehnite-pumpellyite facies likely related to the late orogenic
Apennine evolution.
The geochemical features of serpentinites show differences in
compositions with respect to the Primitive Upper Mantle (PUM).
These are likely related to serpentinization processes, since trace
elements normalized to PUM show different trends, comparable

to Residual MORB Mantle and to Primitive Upper Mantle
respectively. HP/LT metamorphic conditions can be documented
in mafic dykes enclosed in serpentinites, but similar conditions
are not recognizable in serpentinites.
REFERENCES
BONARDI G., AMORE F.O., CIAMPO G., DE CAPOA P., MICONNET
P. & PERRONE V. (1988) - Il Complesso Liguride Auct.: stato
delle conoscenze attuali e problemi aperti sulla sua evoluzione
Pre - Appenninica ed i suoi rapporti con l’Arco Calabro. Mem.
Soc. Geol. It., 41, 17-35.
DOGLIONI C., GUEGUEN E., HARABAGLIA P. & MONGELLI F.
(1999) - On the origin of west-directed subduction zones and
applications to the western Mediterranean. In: Durand B., Jolivet
L., Horváth F. &. Séranne M.. Eds, The Mediterranean basins:
Tertiary Extension withing the Alpine Orogenen. Geological
Society, London, Special Publications, 156, 541-561.
GUEGUEN E., DOGLIONI C. & FERNANDEZ M. (1998) - On the
post-25 Ma geodynamic evolution of the western Mediterranean.
Tectonophysics, 298, 259-269.
LANZAFAME G., SPADEA P. & TORTORICI L. (1979) - Mesozoic
Ophiolites of Northern Calabria and Lucanian Apennine
(Southern Italy). Ofioliti, 4 ,173-182.
PATACCA E. & SCANDONE P. (2007) - Geology of the Southern
Apennines. In: Mazzotti A., Patacca E. &. Scandone P. Eds.,
Results of the CROP Project, Sub-project CROP-04 Southern
Apennines (Italy). Boll. Soc. Geol. It., Spec. Issue, 7, 75-119.
SPADEA P. (1982) - Continental crust rock associated with
ophiolites in Lucanian Apennine (Southern Italy). Ofioliti, 7,
501-522.
SPADEA P. (1994) - Calabria-Lucania ophiolites. Boll. Geofis.
Teor. Appl., 36, 271-281.
STAMPFLI G.M., BOREL G.D., MARCHANT R. & MOSAR J. (2002).
Western Alps geological constraints on western Tethyan
reconstructions. In: Rosembaum G. & Lister G. S., Eds.,
Reconstruction of the evolution of the Alpine-Himalayan Orogen.
J. Virtual Expl., 8, 77-106.
VEZZANI L. (1969) - La Formazione del Frido (Neocomiano-
Aptiano) tra il Pollino ed il Sinni. Geol. Rom., 8, 129-176.
141
SESSIONE 6

SESSIONE 6
142

SESSIONE 7
Acquiferi e loro gestione
CONVENERS
Giovanni Beretta (Università di Milano)
Pietro Celico (Università di Napoli "Federico II")
Massimo Civita (Politecnico di Torino)
Vincenzo Francani (Politecnico di Milano)
Giovanni Barrocu (Università di Cagliari)
Giovanni Sarti (Università di Pisa)
Alessandro Amorosi (Università di Bologna)
143
SESSIONE 7

SESSIONE 7
Co-seismic and post-seismic hydrogeological and hydrochemical
response to the 2009 L'Aquila earthquake
RAFFAELE ADINOLFI FALCONE (*), ANTONELLA FALGIANI (*), MAURO MANETTA (**), BARBARA PARISSE (**),
MARCO PAOLESSI (**), MARCO PETITTA (°), SERGIO RUSI (°°), DONATO SCIANNAMBLO (^),
MICHELE SPIZZICO (^) & MARCO TALLINI (**)
Key words: Discharge increase of springs, earthquake, Gran
Sasso massi, groundwater flow, increase of water table, Italy.
The Mw = 6.3 L’Aquila earthquake on April 6, 2009 in the
Gran Sasso carbonate fractured aquifer produced changes in the
groundwater flow system that had short- and mid-term effects on
the recharge and discharge areas:
1) the sudden disappearance at the time of the mainshock of some
springs located exactly along the surface trace of the Paganica
Fault;
2) an immediate increase in the discharge of the Gran Sasso
highway tunnel drainages (+20%) and of other springs (+10%);
3) a progressive increase of the water table elevation (+1m) at the
boundary of the Gran Sasso aquifer during following months.
Using data collected since the 1990s (Tab. 1) that includes
aftershock monitoring as well as data regarding spring discharge,
water table elevations and rainfall events, a conceptual model of
the earthquake’s consequences on the Gran Sasso aquifer is
proposed herein (Fig. 1) in accordance with previous studies
(MUIR-WOOD &KING, 1993; SATO et alii, 2000; MONTGOMERY
144
et alii, 2003). In this model that excludes the contribution of
seasonal recharge, the short-term hydrologic effects registered
immediately after the mainshock are determined to have been
caused by a pore pressure increase related to aquifer deformation.
Mid-term effects observed in the months following the mainshock
suggest that there was a change in groundwater hydrodynamics.
Supplementary groundwater that flows toward aquifer boundaries
and springs in discharge areas reflects a possible increase in
hydraulic conductivity in the recharge area. This increase can be
related to fracture clearing and/or dilatancy.
Additional monitoring including hydrochemical data
collection allows a refinement of the proposed model. The
preliminary outcomes of the hydrochemical spot sampling of the
pre-seismic (2001 – 2007) (ADINOLFI FALCONE et alii, 2008),
post-seismic (april 2009) and after-seismic (july and september
# Spring Elevation Epicenter Pre-mainshock Post-mainshock % difference Time delay After the mainshock
(m a.s.l.) distance (km) discharge (L/s) discharge (L/s)
(min)
(-)
(L/s)
1 Highway tunnels W drainage 967 16 468 620 (*) +32

Fig. 1 – 1) Conceptual scheme of groundwater changes caused by the L’Aquila earthquake; RAQ – regional aquiclude; TH – permeability boundary (main regional
thrust); HT – highway tunnels (950 - 1000 m asl); RA - high elevation recharge area (2700 - 1500 m asl); TKP – high elevation tectono-karstic plain (preferential
recharge area); HEDA – high elevation discharge area (750-1600 m asl); LEDA – low elevation discharge area (270 - 350 m asl); SSWT - spring-summer water table
(groundwater recharge period); FWWT – Fall-winter water table (groundwater exhaustion period). 2) Conceptual sketch of groundwater changes caused by the
L’Aquila earthquake in the main discharge area (LEDA). A- situation before the mainshock; B- short-term response after the mainshock. Pore pressure causes the
water table to raise with instantaneous spring discharge increases relative to the pre-mainshock state (dotted line); C- mid-term response associated with a change in
the bulk hydraulic conductivity of the recharge area. This causes spring discharge increases with respect to those of the pre-mainshock period (dotted line).
to the pre- and after-seismic ones could be more magnified,
considering the higher values of discharge (Tab. 1) which diluted
the hydrochemical content. This dilution effect can be attributed
to the high recharge rate recorded during 2009 with respect to the
previous ones and it was more evident in the Tempera and Vera
spring group, where the discharge values in the post-seismic
period were 70% higher than those of pre- and after-seismic
periods (AMORUSO et alii, 2010). Complete interpretation of both
quantitative and hydrochemical data is necessary to determine the
long-term consequences of this earthquake on the groundwater
flow of the Gran Sasso carbonate massif, as suggested also by
other geochemical monitoring results (CHIODINI et alii, 2010).
Tab. 2 – Rn (pC/L), T (°C), pH and E.C.: electrical conductivity (μS/cm) of
Tempera and Vera groundwater; pre-seismic period: spring and summer months
from 2002 to 2007 and post-seismic period: from april 17 to july 12 2009. AV:
average value; ST DEV: standard deviation.
REFERENCES
145
ADINOLFI FALCONE R., FALGIANI A., PARISSE B., PETITTA M.
SPIZZICO M. & TALLINI M. (2008) - Chemical and isotopic
(δ 18 O‰, δ 2 H‰, δ 13 C‰, 222 Rn) multi-tracing for groundwater
conceptual model of carbonate aquifer (Gran Sasso INFN
underground laboratory – central Italy). J. Hydrol., 357,
368– 388.
AMORUSO A., CRESCENTINI L., PETITTA M., RUSI S. & TALLINI M.
(2010) – Co-seismic and post-seismic hydrogeological
response of the Gran Sasso carbonate aquifer to the L’Aquila
earthquake (central Italy). Geophysical Research Abstracts;
12, EGU2010-6954 general Assembly 2010.
CHIODINI G., CALIRO S., CARDELLINI C:, AVINO R., MONOPOLI C.,
INGUAGGIATO S. & FRONDINI F. (2010) - One year of
geochemical monitoring of groundwater in the Abruzzi region
after the 2009 earthquakes. Geophysical Research Abstracts;
12, EGU2010-14951 general Assembly 2010.
MONTGOMERY DR., GREENBERG HM. & SMITH DT. (2003) -
Streamfow response to the Nisqually earthquake; Earth and
Plan. Sci. Lett., 209, 19-28.
MUIR-WOOD R. & KING GCP. (1993) - Hydrological signatures
of earthquake strain; J. Geophys. Res., 1993, 22035-22068.
SATO T., SAKAI R., FURUYA K. & KODAMA T. (2000) - Coseismic
spring flow changes associated with the 1995 Kobe
earthquake. Geophys. Res. Lett., 27, 1219-1222.
SESSIONE 7

SESSIONE 7
Key words: Aquifer stratigraphy, fluvial architecture, Po Plain,
Quaternary.
Increasing demand of groundwater for municipal and
agricultural use is shifting applied sedimentology in focus toward
detailed reservoir and hydrostratigraphic characterization. In this
respect, sequence stratigraphy has proved to be a powerful tool
for delineating aquifer geometry and the vertical stacking of
regional hydrostratigraphic units.
The Po Plain is one of the largest alluvial plains in Europe
and makes up an appealing target for water research. Extensive
subsurface investigations have been performed during the last
decade in the Po Basin, with the aim of defining a general
framework of aquifer distribution within the middle-late
Quaternary alluvial succession (REGIONE EMILIA-ROMAGNA &
ENI-AGIP, 1998; REGIONE LOMBARDIA &ENI-DIVISIONE AGIP,
2002).
Detailed sedimentological analyses, concurrently with a
multiproxy investigation of cores and its framing into a sequencestratigraphic
context, provide the basis for depicting aquifer
architecture on a regional scale, including specific facies
connotation of aquifer systems (AMOROSI, 2008; AMOROSI et alii,
2008; AMOROSI &PAVESI, 2010).
Large-scale stratigraphic architecture of the Po Basin reflects
the complex interplay between thrust tectonics, subsidence and
sea-level change during the middle-late Quaternary.
Two major unconformities, identified on a seismic basis and
dated to about 400 and 870 ka, respectively, represent the lower
bounding unconformities of depositional sequences that can be
tracked throughout the basin.
A distinctive cyclic organization of facies characterizes the
stratigraphic architecture of the Po Basin. Particularly, the Po
Basin fill is characterized by the stacking of eight successive
“transgressive-regressive” sequences, falling in the Milankovitch
(100 ka) band, the accumulation of which was strongly controlled
_________________________
Contrasting fluvial architecture in the middle-late Quaternary
succession of the Po Plain: implications for aquifer stratigraphy
(*) Dipartimento di Scienze Geologiche e Ambientali, Università di
Bologna, alessandro.amorosi@unibo.it
ALESSANDRO AMOROSI (*)
146
by middle-late Quaternary interglacial/glacial cycles. These
depositional cycles form the major stratigraphic units of the
geological map to 1:50,000 scale.
Landward of maximum marine ingression, the middle-late
Quaternary deposits consist of a thick alluvial succession. The
lower parts of sequences, which are correlative at seaward
locations with retrograding (transgressive) coastal and shallowmarine
deposits, are made up chiefly of monotonous successions
of silt-clay overbank deposits (with thin and lenticular fluvialchannel
sands), forming major permeability barriers.
These display upward transition to increasingly amalgamated
and more laterally extensive fluvial-channel sand bodies, which
form distinctive aquifer systems.
High-resolution stratigraphy from the late Quaternary alluvial
deposits of the Bologna area provides new insights for detailed
comparison of fluvial architecture within “glacial” (Last Glacial
Maximum) versus “interglacial” (Holocene) alluvial deposits.
Isolated fluvial geometries are clearly related to stratigraphic
intervals showing expansions of warm-temperate vegetation
(interglacial conditions), while laterally extensive, amalgamated
sand bodies appear to be related to phases of low accommodation
under lowstand and early transgressive cold-climate conditions.
This contrasting fluvial style is likely to represent a peculiar
feature of alluvial architecture beneath modern alluvial plains.
REFERENCES
AMOROSI A. (2008) - Delineating aquifer geometry within a
sequence stratigraphic framework: Evidence from the
Quaternary of the Po River Basin, Northern Italy. In: A.
Amorosi, B.U. Haq and L. Sabato (Eds.) Advances in
Application of Sequence Stratigraphy in Italy. GeoActa
Special Publication, 1, 1-14.
AMOROSI A. & PAVESI M. (2010) - Aquifer stratigraphy from the
middle-late Pleistocene succession of the Po Basin. Mem.
Descr. Carta Geol. It., 90.
AMOROSI A., PAVESI M., RICCI LUCCHI M., SARTI G. & PICCIN A.
(2008) - Climatic signature of cyclic fluvial architecture from
the Quaternary of the central Po Plain, Italy. Sediment.
Geol., 209, 58-68

REGIONE EMILIA-ROMAGNA & ENI–AGIP (1998) - Riserve
idriche sotterranee della Regione Emilia-Romagna.
S.EL.CA. (Firenze).
REGIONE LOMBARDIA &ENIDIVISIONE AGIP (2002) - Geologia
degli acquiferi Padani della Regione Lombardia. S.EL.CA.
(Firenze).
147
SESSIONE 7

SESSIONE 7
Modeling and design of a groundwater remediation system by using
recirculation of treated water: a case history
Key words: Groundwater modeling, phenols, reinjection and
recirculation.
The consolidated approach to groundwater remediation in
Italy includes a limited number of technical solutions that
generally imply a Pump &Treat system and the discharge of the
treated water as wastewater into a sewer or into a ditch.
This case study is related to an industrial site located in the Po
plain, mainly impacted by phenols and other organic compounds
from leaking underground tanks. At this site a remediation system
combining pumping of groundwater, on-site treatment, addition
of oxygen and up-gradient reinjection of the treated water has
been designed and approved by the local authorities.
According to the current Italian regulation contaminated sites
(Legislative Decree No. 152 of April 3, 2006), the impact was
notified to the local authorities. According to the general criteria
set by the above mentioned Legislative Decree, further to the
exceedance of the threshold limits, a risk assessment study has to
be conducted in order to define site-specific Risk Threshold
Concentrations. The results of the environmental investigation
showed that the contamination is mainly dissolved and located in
the shallower aquifer, at a depth of 3-4 m below ground surface
(“bgs”).
The aquifer, which has a thickness of 1-1.5 m and is overlying
a thick silty clay layer, is unconfined and has a moderate
permeability. The geometric features of the aquifer were defined
by drilling a number of monitoring wells, conducting slug tests
and pumping tests, and by a geophysical survey (Fig. 1).
The chemical parameters were surveyed by periodical
groundwater sampling and chemical analyses.
The design of the remediation system was supported by a
dedicated groundwater modeling.
Groundwater modeling was applied to the Site following the
modeling protocol indicated in Applied Groundwater Modeling
(ANDERSON & WOESSNER, 1992). The purpose of the
groundwater modeling was to assess the hydraulic efficiency of
the proposed remediation system. It includes a containment
system made of pumping wells and a drainage trench (Pump &
_________________________
(*) Golder Associates S.r.l., Torino, eantonucci@golder.it
ELENA ANTONUCCI (*) & CLAUDIA COSTANZO (*)
148
Fig. 1 – Tomographical model of electrical resistivity – 3D view, west side.
Treat) located down-gradient of the contaminated area, combined
with an reinjection system of oxygenated water (up-gradient).
In this work a series of steps were followed:
• Groundwater model construction
• Groundwater model calibration
• Predictions.
At first code FEFLOW 5.4 was selected, a finite element
numerical code capable of simulating groundwater flow and
chemical transport under complex boundary conditions, suitable
to achieve the objectives mentioned. The Site conceptual model,
identifying hydrostratigraphic units (geologic units of similar
hydrogeologic properties), system boundaries and values of
hydrodynamic parameters was then reproduced. Consequently,
the numerical model was designed.
The groundwater model was calibrated by modifying the
boundary conditions and the hydraulic conductivity values until
there was a reasonable match between the simulated hydraulic
head values and those measured in the field.
Once calibrated, the numerical model was used for assessing
the hydraulic performance of the proposed pumping and
reinjection systems evaluating different scenarios in terms of
number of pumping wells, length of the drainage trench and
number of reinjection wells (Fig. 2).
The best/final configuration for the remediation system
identified was:
• 3 pumping wells and one drainage trench (15 m length);
• 4 oxygenated water reinjection wells.

Fig. 2 – Detail of the results of prediction of the recirculation of groundwater resulting from the P&T and reinjection.
REFERENCES
ANDERSON M.P. & WOESSER W.W. (1992) – Applied
groundwater modeling. Academic Press, San Diego, 385 pp.
149
SESSIONE 7

SESSIONE 7
Geological-structural analisys and hydrogeology of carbonate ridge
between Ambro and Fiastrone rivers (Umbria-Marche Apennine)
ANDREA BAGGIO COMPAGNUCCI (*), STEFANO CICORA (**), STEFANO PALPACELLI (°) & PIETRO PAOLO PIERANTONI (°°)
Key words: Hydrogeology, hydraulic conductivity, limestone
acquifers.
INTRODUCTION
In the present work has been characterized and verified the
actual geological and structural setting of a portion of the
carbonate ridge located in the Monti Sibillini area, and between
the Ambro river and the Fiastrone river.
Recognition, spatial layout of the main tectonic elements and
analysis of the slotted associated with them has allowed an
accurate description of the main feeding areas, the routes of
underground drainage, the geological conditions leading to the
main event of emergency water. The directions of maximum
hydraulic conductivity, obtained by the method of geometricstatistical
Kiraly on a variety of complex hydrogeological, are
arranged around NNW-SSE, in agreement with the available
space of the majority of the lines of discontinuity. The meaning
of these Apennine tectonic elements, together with the axial
culmination of macro structures then, would be responsible for a
strong preferential direction of flow towards the north of the deep
aquifers that are superficial, albeit the latter with some deviation
to either the eastern and western sectors.
The analysis confirms the importance that a plan of geological
and structural characterization becomes more specific in the
context of the movement of water within the rock masses.
CONSIDERATIONS
Results from field observations carried out for this thesis
suggest that the groundwater circulation in the upper portion of
Tennacola stream is closely influenced by the hydrogeological
characteristisc of emerging formations and by the tectonic-
_________________________
(*) eabaggio@tiscali.it
(**) stefanocicora@virgilio.it
(°) Scuola di Dottorato in Scienze della Terra, Università di Camerino
(°°) Dipartimento di Scienze della Terra, Università degli Studi di
Camerino, pietropaolo.pierantoni@unicam.it
150
structural setting of entire system.
The porpoise of this work of thesis was the detailed
geological-structural characterization of a portion of the Umbria-
Marche Apennine thus to describe the main groundwater ways
circulation and the zones of feeding associated, let alone a
conceptual scheme to define the hydrogeological conditions that
characterize the phenomena of sources taken in consideration.
For this work we have taken care of census water points being
inside the study area, that carried to identification of 18 sources,
34 hydrometric measures stations, and 6 wells dispersed in the
hydrographical basin of the Tennacola stream.
The data collected during the geological-structural survey
allowed to characterize fractured rocks heaps represented by
Maiolica Formation in Monte Castel Manardo. It is the aquifer
hanging from which the Tennacola stream and different sources
origin. The diagrams that relate the spacing with strata thickness
design an increasing linear relation with a = 0,47 for the set 85/80
and a = 0,62 for the set 220/70 and length and spacing of
fractures follow an exponential curve second a poissonian
distribution with 0,80>R2>0,84.
As the fractures connectivity approaches itself to the base of
formation it seems to decrease. Moreover, through collected data,
it has been possible to obtain an hydraulic conductivity value
from the formula’s application proposed from Kiraly (1975) for
the characterization of the rocks heaps, that, even though clear
simplifications, provides a real parameter that can be compared
with that obtained from the Darcy’s law.
In the aquifer units of Maiolica and Scaglia Formations rain
waters are rapidly delivered to the spring area through the
unsatured zone by micro-karstic and fissuration; instead in the
superficial complexes composed of detrital and alluvial deposits,
the rapidity of groundwater flow is influenced by the tessitural
architecture of deposits. Both situations evidence a good
correspondence between structural setting and groundwater
circulation.
From these results it has been possible to define that the
Carbonate ridge near Pizzo di Meta is a structure stopped by
tectonics and stratigraphic contacts with low permeability bodies;
the structure drainage may continue towards external basin
situated in the North. To the South, the basal groundwater flow
guarantees the feeding of the Fiastrone river relationship with the
bending that the thrust assumes near the structural highs of Monte
Sassotetto e Monte Valvasseto. Particularly, although the Monte

Fig. 1 – Monte Castel Manardo Anticline. NEO: Calcare Massiccio formation, MSE: Marne del Monte Serrone formation, PSD: Calcari a Posidonia formation,
MAJ: Maiolica formation.
Valvasseto structure is constituted for the majority by limestone
of Massiccio complex it does not supply contributions at all to
Tennacola stream capacity.
This portion of carbonate ridge represents a watershed of the
bases aquifer that stretches to flow down the major part of water
toward the Fiastrone river and toward the deep valley of Ambro
river, testified from the presence of linear spring. In according to
such considerations it has been possible to recognize into the
inside of the Monte Castel Manardo macro-anticline several
suspended hydrological bodies supported by low conductibility
layers witch feed both the Tennacola stream and several sources.
The sources situated at the entrance of Tre Santi valley are
feed by Scaglia and Maiolica Formation that represent the reverse
forelimb of fold and they are confined as a horses defined by
several segment of Monti Sibillini thrust zone (CENTAMORE et
alii, 1971; CHIOCCHINI et alii, 1976; LAVECCHIA, 1979;
CALAMITA et alii, 1990; DEIANA et alli, 1994; PIERANTONI et alii,
2005).
REFERENCES
CENTAMORE E., CHIOCCHINI M., DEIANA G., MICARELLI A. &
PIERUCCINI V. (1971) - Contributo alla conoscenza del
Giurassico dell’Appennino umbro-marchigiano. Studi
Geologici Camerti, 1.
151
CHIOCCHINI M., DEIANA G., MICARELLI A., MORETTI A. &
PIERUCCINI U. (1976) - Geologia dei Monti Sibillini Nord-
Orientali. Studi Geologici Camerti, 2, 7-44.
DEIANA G. & PIALLI G. (1994) - The structural provinces of the
Umbria-Marche Appennines. Mem. Soc. Geol. It., 48, 473-
484.
PIERANTONI P.P., DEIANA G., ROMANO A., PALTRINIERI W.,
BORRACINI F. & MAZZOLI S. (2005) - Geometrie strutturali
lungo la thrust zone del fronte montuoso umbromarchigiano-sabino.
Boll. Soc. Geol. It., 124, 395-411.
KIRALY L. (1975) - Rapport sur l’état actuel des connaissances
dans le domaine des caractères physiques des roches
karstiques. In: Burger A., Dubertret L. Eds., Hydrogéologie
des terrains karstiques, IAH, Paris, 53-67.
LAVECCHIA G. (1979) - Analisi cinematica del sovrascorrimento
del F.Fiastrone (Sibillini Nord-Orientali). Boll. Soc. Geol. It.,
98, 457-468.
SESSIONE 7

SESSIONE 7
Aquifers and integrated water resources management in coastal
areas
Key words: Coastal zone, deltas, groundwater, pollution,
seawater intrusion, water quality.
Coastal areas, consisting of the emerged and submerged parts
of the coast, are the final part of catchments and transition zones
between continents and seas, where the fragile natural
equilibrium between fresh, brackish and salt water interfaces may
be easily jeopardized by human actions. This equilibrium is, of
course, strongly dependent upon the interactions between rock
and water, and sea level variations due to subsidence and
changing climate. The natural water cycle is a process strongly
affected by human activities, and need time and space, which are
ineluctable boundary conditions for sustainable water resource
development and good life quality.
Coastal aquifers are important freshwater sources, especially
in deltas. A large proportion of the world’s population (about
70%) dwells in coastal zones, and many coastal areas are so
heavily urbanized that the need for freshwater, to meet domestic,
agricultural and industrial demands, is even more acute. Many of
these sprawling urban areas have mushroomed with little or no
planning, so that groundwater is endangered by overexploitation
and degradation due to mismanagement, and lack of drainage,
sewage systems and sanitation. The situation may be critical in
areas with a heavy tourist influx, especially in seaside resorts
where hotels and large residential areas have been sprung up by
the sea, swelling the population.
Excess pumping produces seawater intrusion directly from the
sea or by upconing of connate waters trapped in depth into
ancient unleached sediments. Over the last few decades, saltwater
intrusion in coastal aquifers has become a major environmental
problem worldwide.
Freshwater is threatened not only by saltwater encroachment
but also by pollution produced by human activities, especially in
developing countries, where the problem of water resources
management is more acute. In recent years, public attention has
been focused on groundwater contamination by hazardous
industrial waste, leachate from landfills, oil spills, mining
activities, industrial facilities, unsuitable engineering works,
agricultural activities, and sites of radioactive waste repositories,
to mention but a few of the more acute pollution sources. In most
cases, the source of contamination is above ground surface, with
contaminants passing through the unsaturated zone on their way
to an underlying aquifer.
Deltaic areas are particularly vulnerable to floods and
GIOVANNI BARROCU (*)
152
consequent pollution of surface groundwater and soil.
In heavily populated areas, potential pollution sources are
difficult to remove so as to define a minimum protection zone
depending on local hydrogeological conditions around springs
and wells in order to grant groundwater of acceptable good
quality. However, any potential pollution source should be
encircled by a respect zone, so that remediation actions would be
successful in case of an accident.
Drinking water of good quality from contaminated coastal
aquifers may be mainly supplied in short term by treating
contaminated groundwater, even with mobile modular treatment
plants. The treatment of surface water may be more problematic,
depending on the water quality, which can be strongly degraded
by solid and liquid wastes directly thrown into rivers.
If water quantity and quality are not enough to satisfy local
demands, water is to be imported from elsewhere and/or its
quality is to be improved by treatment processes. In fact, water
supply is a typical problem of integrated regional and urban
planning, as it implies transfer and allocation of water resources
from an area to another so as to avoid conflicts among different
users. The problem is to be assessed considering scientific,
technological, socio-economical and political aspects, and
different people’s point of view, so as to find proper solutions,
involving stakeholders and users.
When taking into account the mutual relationship between
continental and sea waters, the interrelations between surface
waters and groundwater are to be carefully considered under
present and future conditions. Water budgets should be made in
terms of integrated water resources to be defined taking into
account the water quantity and quality needed for different uses,
with reference to watersheds and areas of interests.
Unfortunately, evaluating the influence of groundwater discharge
into the ocean has proven to be very difficult. In spite of the
recognition that many land-sea interface of the world are
characterized by "leaky" continental margins, it is still unclear
how important these "leaks" are in terms of overall marine
geochemical budgets.
The management of coastal zones requires that the dynamics
of coastal aquifers is properly defined, considering the local
effects of water resources development and the results of inland
human actions. Environmental impact and economic effects
associated with saltwater intrusion phenomena requires
monitoring and analysis of the response of the threatened system

and involves the use of reliable models enabling the prediction of
future scenarios.
Aquifer and extensively coastal zone management by its very
nature is very complex. In addition to the hydrogeological input,
it requires contributions from oceanographers, legal specialists,
social scientists and political scientists to develop practical
approaches for governments to adopt. The remediation of
contaminated aquifers may be a necessary step which requires the
integrated planning of all human activities in the urban area under
consideration, and the construction of suitable sanitation
infrastructures.
Major respect of hygienic rules and better population
distribution inland seem necessary in many countries. The natural
water cycle is a process strongly affected by human activities, and
need time and space, which are ineluctable boundary conditions
for sustainable water resource development and good life quality.
Meeting the growing challenge of water scarcity in the future
requires that all appropriate and available technologies be utilized
for the sustainable management of freshwater resources.
Greater integration implies that coastal areas as well as their
integrated water resources be managed simultaneously, paying
due respect to the environment. In coastal areas natural water
resources may be integrated with non-conventional waters
obtained by sea and salty water desalination, and of used water
treatment. Waste waters should be treated and recycled in any
case, especially for the benefit of industrial farming. Polluted
groundwater should be rehabilitated also for environmental
reasons, and depleted aquifers artificially recharged with different
methods, depending on local conditions.
153
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A sustainability decision support tool for remediation options with
respect to the environmental, social, economical as well as technical
dimensions
Key words: Optimization, remediation, sustainability.
The growing technological development of the last decades
has enlarged the number of options for remediation of
contaminated lands. Therefore, considering also the constraints
given to pressing environmental legislation, an holistic approach
to remediation activities is suggested in order to comprehend in
the decision making process for choosing the more suitable
remediation option not only technical elements, but also
environmental, economical and social aspects.
At this aim Golder Associates has developed a sustainability
decision support tool, GoldSET©, to evaluate the strengths and
weaknesses of engineering projects with respect to the
environmental, social, economical as well as technical
dimensions.
It allows for an unbiased comparison of different options on
the basis of sustainability principles. As such, it can help identify
optimal solutions in a decision-making process based on the
principles of sustainable development.
This sustainability analysis results in a “triple-bottom-line”
assessment, expanding the traditional analytical framework from
financial performance to environmental, social and economical
performance. By providing a comprehensive and transparent
framework to understand and manage the sustainability issues of
a project, GoldSET© can achieve the following benefits:
- improve the decision process involving complex issues by
providing a framework to enhance the understanding of the
impacts associated to these issues;
- support proactive stakeholder engagement – the evaluation
process is meant to be rigorous and transparent so that
stakeholders can better understand the alternatives and their
respective impacts;
- ease communication facilitating the issuing of a social
licence to operate a project - the visual representation of
performance with respect to sustainable development is a
fundamental element which can be instrumental in improving the
communication with communities;
_________________________
SIMONE BIEMMI (*), DELIA BOCCARDO (*), ANGIOLO CALI’(*) & VALENTINA OSELLA (*)
(*) Golder Associates S.r.l., Turin, dboccardo@golder.com
154
- optimization of options – provides a framework to compare
alternatives with a set of key criteria, trade-offs leading to
optimized decisions are facilitated;
- improve corporate image: A decision supported by a
sustainability framework is an effective demonstration of a
corporation’s willingness to move forward with sustainable
development, which can consequently promote a positive
corporate image.
The end result is a visual compilation of the sustainability
performance. The visual presentation demonstrates the elements
of each option and allows for effective decisions. The three axes
of the triangle present the performance of an option with respect
to the three dimensions of sustainable development.
Results are compared taking into consideration the
sustainability performances resulting from the visual compilation.

Key words: Friuli Venezia Giulia aquifers, groundwater, water
quality, water resources.
ABSTRACT
One of the objectives of the European Directive 2000/60 and
the Legislative Decree 152/06 is the sustainability of waterbalance
in a reference area with the aim of protecting water
resources. Thorough verification of the water-balance it will be
possible to obtain the consumption sustainable water value and,
together with other protective measures planned, the achievement
of environmental quality.
The constantly increasing water demand for human
consumptions and the constant use of water resources induced to
study deeply the Friuli Venezia Giulia Plain (north eastern part of
Italy) where all the water resources of the Region are storeged.
The aim of the present research is to realize a water-balance in
order to understand the amount of the water resource and its use.
To reach this aim, the Geosciences Department from Trieste
University has been engaged by the Hydraulic Survey of the
Friuli Venezia Giulia Region in order to coordinate an integrated
study finalized to the Friuli Venezia Giulia Plain confined and
unconfined aquifer geometries reconstruction and to provide
guide-lines for water rational exploitation (Agreement D.G.R. n.
1827 dd. 27.07.2007).
Water-balance means the comparison between the water
resources, available or obtainable, and the withdrawn in the
reference area. In order to define water consumption, 2 Data
Base: one for the domestic use (47709 estimated water-wells),
and the other one for all the other uses (7930 water-wells) have
been analyzed. Potable, agricultural, industrial, hygienic and
sanitary, fish breeding and geothermal uses have been
considered. For every single use have been calculated the
number of withdrawal points and the amount of withdrawal for
_________________________
Water sustainability in the Friuli Venezia Giulia Plain
CHIARA CALLIGARIS (*), LUCA ZINI (*), FRANCESCO TREU (*), DANIELA IERVOLINO (**),
(*) Università degli Studi di Trieste, Dipartimento di Geoscienze,
calligar@units.it , zini@units.it , franz_treu@hotmail.com ,
cucchi@units.it
(**) Regione Autonoma Friuli Venezia Giulia, Servizio Idraulica,
Daniela.iervolino@regione.fvg.it , federica.lippi@regione.fvg.it
FEDERICA LIPPI (**) & FRANCO CUCCHI (*)
155
every single aquifer. Figure 1 is showing the actual situation.
Precipitation, evapotraspiration, runoff, infiltration and river
discharge were used to obtain input and output water values from
the regional system. As result, the water availability for the Low
Plain depends from the High Plain recharge and from the water
insisting on the mountain basin (197,7 m 3 /s) but also the total
water extractions are consistent (59,3 m 3 /s). In fact, the total
withdrawal value evaluated by the census of 55639 sampling
points present in the Friuli Venezia Giulia is 59,3 m 3 /s, of which
10,2 m 3 /s are relative to groundwater phreatic withdrawals of the
Low Plain. 49.1 m 3 /s is therefore the amount of the groundwater
withdrawals from the phreatic High Plain and the artesian
aquifers. To this value must be added the withdrawal contribution
from the Veneto Region (in Tagliamento right side).
The withdrawals intensity is well explained in the Figure 1
where they are expressed in l/s for km 2 for every single water
body. The total amount of withdrawals for single aquifer is
represented in Figure 2. While from a comprehensive analysis the
current use of the water resource seems to be sustainable, a
specific analysis made on the single water body shows great,
critical and substantial unevenness. In particular, it highlights the
overfishing of the area located in the Tagliamento right side
where consumers are heavily unbalanced in relation to charging.
The hydroelectric and irrigation withdrawals on the mountain
rivers create a significant deficit in the recharge of the High Plain
in the Tagliamento right side. The result is the crisis on the
artesian groundwater in the Low Plain on the right side of
Tagliamento River. This imbalance is offset by increasing recall
of phreatic and artesian groundwater from the left side of
Tagliamento. The withdrawals that interest, with different
intensity, all the artesian aquifers, induce an always greater
mixing in the waters with the consequent substitution of the deep
ones with the phreatic. Water age analyses indicate that the
waters deeper than 110 m from the ground level (aquifer C), are
older than 15000 years (CUCCHI et alii, 2008). This is a resource
of really high quality but with a low natural recharge. The force
exerted by the wild withdrawals, cause a depletion of water and
take to their accelerate substitution by younger waters having
match lower quality. The balance is not sustainable any more,
water table is subsiding 0,1-0,4 m/yr (CUCCHI et alii, 1999), the
pressure of the confined aquifers is dropping and this imply a
different policy geared towards a conscious use of the resource.
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Fig. 1 – Intensity water withdrawals (l/s at km 2 ).
Fig. 2 – Water withdrawals (m 3 /s) divided on single different body water. Diagrams are on logarithmic scale.
REFERENCES
CUCCHI F., FRANCESCHINI G. & ZINI L., (2008) -
Hydrogeochemical investigations and groundwater provinces
of the Friuli Venezia Giulia Plain aquifers, northeastern
Italy. Environ. Geol., 55, 985-999.
CUCCHI F., MASSARI G. & OBERTI S. (1999) - Water table
fluctuations in the northern Friuli Plain. Gortania, 21, 41-51.
156

Key words: Alluvial sediments geodatabase, GIS,
hydrostratigraphy, Quaternary.
INTRODUCTION
In alluvial plain settings, the correct knowledge of subsurface
geometries is of paramount relevance both for hydrostrigraphic
reconstructions and for models aiming to manage the sustainable
exploitation of groundwater. The integrity of the geographic and
geometric attributes of surface and subsurface data-sets
(geomorphology, geology, hydrology) is a strong condition to
aquifer characterization purposes. The management of the data
flow is relevant point to monitor and improve the different steps
of an hydrogeological study. An example of GIS-based data
management of the hydrostratigraphic work-flow is presented
here, concerning a limited sector of the Adda Lambro interfluve
area.
CASE HISTORY AND DATA-SET
The case study is a small area of the Adda – Lambro
interfluve South of Milan, close to Cassano d’Adda. The area
represents a relevant knot for the hydrogeology of this part of the
Po plain. It spans from the Holocene lower terrace of the Adda
valley to the high terraces of the Middle Pleistocene alluvial fans.
In the subsurface, the transition from the northern glacio-fluvial
alluvial fans and incised valleys to the braided river depositional
systems occurs (BINI et alii, 2004; BERSEZIO et alii, 2004). This
hinge corresponds to the change from a single phreatic aquifer
(North) to a stack of partly confined aquifer complexes
(South),that is accompanied by the emergence of the shallowest
water nappe along the well-known belt of plain springs
(fontanili).
Five data-types have been collected (original and literature
data): 1) geomorphological and morphometrical data; 2) surface
pedological, textural and sedimentological data; 3) poro-perm
_________________________
Gis management of multiple data-sets for hydrostratigraphic
reconstruction in alluvial plains.
An example from the Adda-Lambro plain in Lombardy
(*) Università degli Studi di Milano Dipartimento Scienze della Terra
“A.Desio”, emmanuele.cavalli@unimi.it
EMMANUELE CAVALLI (*)
157
properties of aquifer analogues; 4) subsurface stratigraphic data;
5) hydrological and meteorological data (rainfall, temperature,
humidity).
The data-sets have been managed by arcGIS®. A geodatabase
(file geodatabase) has been designed and loaded, in order to
handle the 4 data types as previously mentioned. The
relationships between surface and subsurface data have been
carefully addressed, aiming to obtain a flexible data-base
structure, account for both the XY (map view) and the XZ - YZ
(cross section view) plains.
WORK-FLOW
As a first step, a new DTM (Fig. 1) has been computed by
kriging of hundreds of elevation points, obtained from the CTR
Regione Lombardia and new field data, collected to highlight any
subtle topographic break (i.e. minor terrace scarps) of the
regional topographic gradient. Then, aspect and slope have been
studied. Two domains of centripetal shallow drainage have been
1
Fig. 1 – DEM modified. 1) Main axis drainage; 2) Adda river; 3) Cassano
d'Adda town
recognized, with respect to a N-S striking medial axis Fig.1).
Subsurface data have been organized in a relational data-base,
consisting of tables with one-to-many relation to the surface data,
from which the geographic attributes are inherited. Subsurface
data can be viewed and/or edited along any horizontal and
vertical section. The switch from horizontal (map) to vertical
(cross–section) editing is based on a script, which makes it an
autonomous and automatic procedure.
The subsurface geological interpretation has been obtained
3
2
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Fig.2 – Vertical section sketch. 1) subsurface geological data shown with
different colours and thikness; 2) Geological surface drawn with different
colour and thikness according to their relative hierarchy ; 3) "Map" of
interpolated litological propreties related to permeability in five different class
(light and dark blue, yellow, light and dark gray).
after visualization of surface and subsurface maps and vertical
cross-sections, that contain all the data coherently input into the
geodatabase (Fig.2). The hierarchic stack of bounding
stratigraphic surfaces has been compared to the existing
literature. Interpolation of lithological, textural and poro-perm
properties has been computed both in map and in cross-section
projections, by implementation of ad hoc interpolation tools.
Once the geological and hydrostratigraphic features have been
defined and mapped on known vertical and horizontal plains,
potential field modeling (Chiles at al., 2004) has been applied, by
the use of the Geomodeller ® software. Again, the migration
from the GIS environment to the new software has been made
automatic by a specific script.
CONCLUSION
The implementation of the work-flow permitted to evaluate
several alternatives and to estimate sensitivity and uncertainty. A
substantial refinement of the available geometrical and geological
models of the subsurface has been obtained, in terms of a
satisfactory match between surface and subsurface data, a
sufficiently good shaping and spatial positioning of sedimentary
bodies and of an ameliorable characterization of their internal
architecture.
The new 3-D model allowed for the assessment of a new
hydrostratigraphic framework, that forecasts the shape and
location of complex aquifer systems. The 3-D rendering
158
highlights the very low continuity of the most and least permeable
sedimentary bodies (aquifers and aquicludes). Connectivity and
spatial heterogeneity of aquifer systems indicate that preferential
flow paths should exist and should be accounted for during flow
and transport modeling experiments. Forecasting the location and
spatial extent of hydrogeological windows is one of the results
made possible by the use of several modeling routines applied to
the Geodatabase.
Excluding the 3-D rendering of maps and cross-sections, the
entire work has been developed in the same GIS environment. In
spite of some minor pitfalls (like the poor visualization of crosssections),
this gave the great opportunity to track systematically
the geographic location of any entity or object. This is
fundamental at the regional scale, for correct positioning of any
spatial feature or property of any sedimentary unit. The use of the
Geodatabase permitted to evaluate many alternatives, computing
and comparing the statistical errors at any step.
REFERENCES
BINI A., STRINI A., VIOLANTI D. & ZUCCOLI L. (2004) – Geologia
di sottosuolo dell’alta pianura a NE di Milano. Il
Quaternario, 17 (2/1): 343 – 354.
BERSEZIO R., Pavia F. , BAIO M., BINI A., FELLETTI F. & RODONDI
C. (2004) – Aquifer architecture of the Quaternary alluvial
succession of the Southern Lambro Basin (Lombardy, Italy).
Il Quaternario, 17 (2/1): 361 – 378.

The hydrogeological model of the thermal fluids of Viterbo – Cimini
Mountains area as a tool for their management
UGO CHIOCCHINI (*), FABIO CASTALDI (**) MAURIZIO BARBIERI (°) & VALERIA EULILLI (°°)
Key words: Carbonate rocks, Cimini Mountains,
hydrogeological model, recharge area, thermal fluids
management.
Viterbo city, located in the lower part of the Cimini
Mountains northwestern slope, is well known since Roman Age
because of its thermal water and developed between 8th and 12 th
centuries.
The overall stratigraphic – structural reconstruction of the
Viterbo - Cimini Mountains area with several hot springs by
deep well logs and geophysical data (geoelectric, seismic and
gravimetric surveying) allowed to recognize that the architecture
of the tectonic edifice, below the Pleistocene Cimino and Vicano
volcanic districts cover (CIMARELLI & DE RITA, 2006), is
characterized by overlapping of the Ligurian Late Cretaceous –
Eocene Tolfa Flysch on to the Mesozoic - Cenozoic Tuscan
Nappe and Umbria – Marche Succession (fig.1). The Pliocene –
Pleistocene extensional tectonic phases split the structural edifice
into some uplifted blocks and a graben trending SW - NE which
hosts the Early Pliocene marine mainly muddy sediments, later
uplifted due to the intrusion of magmatic bodies that fed the
Cimino and Vicano volcanism during Pleistocene.
As a consequence of the stratigraphic – structural setting two
aquifers have been detected: a shallow one consisting of the
volcanic units, bottom delimited by muddy sediments and Tolfa
Flysch of very low permeability; a deep carbonate and dolostone
– evaporite one consisting of the Tuscan Nappe and Umbria –
Marche Succession, confined between the bottom phyllite –
quartzite substrate with low permeability and the top Tolfa
Flysch. The upper aquifer hosts bicarbonate – alkaline hearth
water with low salinity and temperature of 13° - 20°C, whilst the
carbonate aquifer hosts a circulation of sulphate – alkaline hearth
water with high salinity that emerge in the thermal area of Viterbo
_________________________
(*) Università della Tuscia, chiocchi@unitus.it
(**) Università della Tuscia, fabio_castaldi@libero.it
(°) Università La Sapienza, mbarbieri@uniroma1.it
(°°) ISPRA, valeria.eulilli@isprambiente.it
159
with a temperature of 30° - 60°C. The hydrostructure of the two
aquifers and the overall geochemistry characters of ground waters
suggest that the recharge area of cold waters is located in the
Mounts Cimini, whilst hot waters of the carbonate resevoit and
the Viterbo hot springs are derived from a circuit of waters that
emerge along the River Nera near Narni, about 34 km ENE of
Viterbo, with a high salinity, a temperature of 16° - 18°C, a
sulphate – alkaline hearth composition and a discharge of 13.5
m 3 /sec, whose recharge area is located in the River Nera
watershed including the Amelia ridge and the Spoleto, Reatini
and Sabini Mounts consisting of the Umbria – Marche
Succession (BONI et alii, 1998). Then these waters mix with
waters of the surface Pleistocene sandy - gravely aquifer resting
directely on the Late Triassic – Early Liassic aquifer of the
Umbria – Marche Succession along the River Tevere valley, flow
westward under the River Tevere valley, heat progressively
approaching thermal anomaly of the Viterbo – Cimini Mountains
Fig. 1 – Block diagram of the area west of Viterbo as far as Vetralla.
Legend: 1 volcanic units of the Vicano District (middle–late Pleistocene); 2
Tolfa Flysch (Late Cretaceous–Eocene); Tuscan Nappe: 3 Scaglia-Diaspri-
Calcari selciferi-Rosso ammonitico (Early Liassic–Paleogene); 4 Calcare
massiccio (Early Liassic); 5 Calcare cavernoso-Anidriti di Burano Formation
(Late Triassic); 6 normal fault; 7 thrust; 8 well; 9 rising of thermal fluids.
ST1, ST2, ST4, ST5 = Terni Company wells. V1 and V2 = Enel wells.
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Fig. 22- Block - Block diagram showing of of the the stratigraphic reconstruction of of the the area area between the the Cimini Mountains, Viterbo and and the the Amelia ridge, the the springs of of Viterbo
thermal area, of of Orte Orte and and of of the the River Nera valley and and the the overall circuit of of groundwaters (yellow arrows). Legend: 1 1 alluvial sediments (Pleistocene–Holocene); 2 2
magma intrusions of of the the Cimino and and Vicano districts (Pleistocene); 3 3 volcanic units of of the the Cimino and and Vicano districts (Pleistocene); 4 4 clayey and and sandy–gravely
sediments (Pliocene–early Pleistocene); 5 5 mainly clayey sediments (early Pliocene); 6 6 Tolfa Flysch (Late Cretaceous–Eocene); 7 7 units of of the the Tuscan Nappe (Late
Triassic–Paleogene); 8 8 units of of the the Umbria Marche Succession (Late Triassic–Paleogene); 9 9 phyllite–quartzite substrate (Permian); 10 10 thrust; 11 11 normal fault; 12 12
springs of of the the River Nera; 13 13 thermal springs of of Orte Orte and and Viterbo; 14 14 route of of groundwaters that that feed feed the the springs along the the River Nera and and the the thermal springs of of Orte Orte
and and Viterbo; 15 15 well. ST5 ST5 Terni Company well. C1 C1 Enel well.
area, feed the thermal spring of Orte with a temperature of 30°C
and further on, with uprising temperature, the carbonate reservoir
and the springs of the area W of Viterbo (CHIOCCHINI et alii,
2010; fig. 2). The discharge measurements of the springs and
wells of the Viterbo area were drastically reduced from about 60
to 100% as compared to the initial discharge. This negative trend,
probably due also to obstruction of the emission conduits, may be
connected to the very long activity of the thermal system, which
started before 0.150 +/- 0.030 Ma, producing a volume of
approximately 113.5 million m 3 of travertines after deposition of
the Tufo Rosso a Scorie Nere Unit. It is clear that the thermal
resource, utilized for therapeutic purposes in the past in at least
three thermal facilities (and at the moment in two facilities), is
exploited at an insuperable level. In order to avoid endangering
the exploitation potential of the thermal resource, it is necessary
to produce an overall territory planning of the area west of
Viterbo with the aim of protecting the most important spring
(Bullicame), one of the main symbols of Viterbo city, and to
avoid indiscriminate pumping of the thermal waters.
Thus this study contributes to a better understanding of the
geothermal systems in complex stratigraphic - structural and
160
hydrogeological settings. Furthermore the hydrogeological model
can be a useful tool to study similar complex settings in different
areas and can provide a useful contribution to the rational
management and exploiting of thermal resources.
REFERENCES
BONI C., BONO P. & CAPELLI G. (1988) - Schema idrogeologico
dell’Italia Centrale. Mem. Soc. Geol. It., 35, 991 - 1012.
CHIOCCHINI U., CASTALDI F., BARBIERI M. & EULILLI V. (2010) -
A stratigraphic and geophysical approach to studying the
deepcirculating groundwater and thermal springs, and their
recharge areas, in Cimini Mountains–Viterbo area, central
Italy. Hydrogeol. J., DOI: 10.1007/s10040-010-0601-5.
CIMARELLI C. & DE RITA D. (2006) - Structural evolution of the
Pleistocene Cimini trachytic volcanic complex (central Italy).
Bull. Volcanol., 68, 538–548.

Analysis of the possibility of parameters reduction in SINTACS method
Keywords: Contamination vulnerability, groundwater, Pearson
correlation coefficient, SINTACS.
INTRODUCTION
The estimation of contamination vulnerability, especially
referred to complex aquifers, is often difficult to assess,
depending on many hydrogeological factors. Their evaluation is
frequently characterized by a general uncertainty due to
unavoidable inaccuracy and/or incompleteness of field data. The
problem can be worsened by non-linear behaviors of the
inhomogeneous elements of water systems, which can exhibit
non-independence features (DUCCI, 2010). Consequently,
contamination vulnerability mapping, performed by the wellknown
SINTACS standard (CIVITA &DE MAIO, 2000), appear to
be sometimes inadequate to perform reliable models of water
systems. This is particularly true for deterministic as well as
stochastic approaches in defining certain parameters, as hydraulic
conductivity and depth to water ones. In order to minimize the
related uncertainties, analytic calculation routines have been
recently adopted by dedicated software, i.e. implemented in
Matlab ® environment. The goal was to examine possible
redundancies among parameters, so modifying SINTACS method
and leading to a simplified vulnerability mapping (CIMINO et alii,
2009).
This paper shows the preliminary results of a study about the
correlation aspects among the parametric maps of SINTACS
system. More SINTACS applications have been considered as
test-sites on coastal belts Italian Peninsula. Modifications to the
available standard were experimented leading to new protocols
more appropriate for the surveyed areas.
THE CONSIDERED TEST-SITES
The Volturno River Plain. The main aquifer of the southern
_________________________
ANTONIO CIMINO (*), ALFONSO CORNIELLO (**), DANIELA DUCCI (**) & ANTONINO OIENI (*)
(*) Dipartimento di Fisica e Tecnologie Relative, Università di Palermo,
cimino@unipa.it
(**) Dipartimento di Ingegneria Idraulica, Geotecnica e Ambientale,
Università di Napoli, daniela@unina.it
161
part of the Volturno River Plain (~1000 km 2 ) is constituted by
alluvial, pyroclastic and marine porous sediments. These
sediments often underlie tufaceous rocks (Campanian
Ignimbrite), with low permeability and thickness increasing
toward the mountains. In fact, at the foot of the mountains the
aquifer is confined by the tuffs; in the flat area, the
hydrogeological conditions are strongly related to the thickness
and to the physical characteristics of these tuffs, which play the
role of semi-confining or confining bed.
Even though groundwater preferably moves in the deposits
with coarse granulometry, the levels with different granulometry
constitute a single groundwater body. The piezometric surface
shows a groundwater divide, which separates the flow in two
parts: the first directed towards W and the second towards S, in
the eastern part of Naples. The main sources of recharge are
rainfall and underflow from the adjacent relieves: the limestone
Mesozoic mountains (NE), the Somma-Vesuvius volcano (S) and
the Phlegrean Fields pyroclastic hills (SW). The groundwater
chemical facies is the calcium bicarbonate type at the foot of the
mountains, and more alkaline toward the coastline, due to the
influence of the pyroclastic and alluvial aquifers of the plain.
Saline contamination of groundwater along the coastline is
restricted to a sector close to the Volturno River mouth. Human
activities are the cause of widespread NO3 contamination, with
many wells showing very high nitrate concentrations, often
exceeding the threshold limit of 50 mg/l. Close to the Volturno
River lower nitrate content is related to reducing conditions. Low
sulphate contents and high Fe and Mn contents corroborate the
presence of a reducing zone.
In order to construct the aquifer vulnerability maps at medium
scale (1:50,000), the parametric method SINTACS has been
applied to the main aquifer (CORNIELLO &DUCCI, 2001; 2005).
The SINTACS Vulnerability map shows prevalent moderate
vulnerability degree; the high vulnerability class appears near the
coast (for the effect of the layers: Vadose Zone, Soil media and
Recharge), where the granulometry is higher, and at the foot of
the surrounding mountains (for the effect of the layers: Hydraulic
conductivity and Recharge). Lowest vulnerable areas occur in
correspondence of the outcropping area of the clayey-peat Unit.
The Acquedolci coastal plain. The Acquedolci plain is located
in the Northern Sicily coastal sector. Geological formations can
be grouped in a few hydrostructural complexes, characterized by
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very different permeability, mainly distinguishing: 1) a
Quaternary sandy-gravelly-arenaceous unit, permeable for
porosity, that hosts a conspicuous shallow aquifer, a Mesozoic
calcareous complex, highly permeable for fractures and karst,
forming a notable deep aquifer supplying the former through the
foothills detritus. 3) Tertiary clayey-marly-arenaceous units,
including Flysch complexes, this locally performing a tamponage
effect as respect to the groundwater circulation. Permeability is
wholly medium to low.
Numerous minor yield springs rise diffusely in the territory:
they have been accurately inventoried constituting local
groundwater reserve resources.
The general high permeability of coastal and inland rocks
affects aquifer vulnerability as well as the pollution risk of
groundwater for nitrates and sea-water encroachment (CIMINO et
alii, 2008a). In particular in the littoral belt, the spreading of
agricultural practices with a large consumption of fertilizers and
pesticides causes a notable pollution of groundwater. The
contemporary occurrence of nitrates and bacteria confirms the
heavy anthropic intervention. Vulnerability is medium to high for
the 74% of the investigated area, while only 1 % is characterized
by low to very low vulnerability scores (CIMINO et alii, 2008b).
ADVANCES IN SINTACS VULNERABILITY
ASSESSMENT
Pearson correlation coefficient ρ is used as an analysis tool to
validate consistency of SINTACS parameters for the studied
areas. A Matlab ® routine has processed all the possible
combinations of couples of non-weighted matrixes, recognizing
similarity and/or singularity grades. The aim is to propose the
elimination of parameters affected by redundancy in vulnerability
assessment. Preliminary outcomes show, for both areas, different
ρ values, allowing categorizing SINTACS parameters on the basis
of their non-independence or singularity features (Fig. 1,
Acquedolci plain, Infiltration, Depth to water and Slope).
Further step of this investigation is to validate this redundancy
analysis comparing final vulnerability maps by the same
correlation procedure. As rough SINTACS matrixes have been
here used, the possible involvement of weights constitutes the
next phase of this research. The availability of a greater number
of test-sites is clearly necessary: consequently, it will be possible
to statistically validate the proposed procedure leading to develop
adjustments to vulnerability assessment.
162
Pearson correlation coefficie
1,00
0,95
0,90
0,85
0,80
0,75
0,70
0,65
Serie1
Serie2
Serie3
Serie4
Serie5
Serie6
Serie7
1 2 3 4 5 6 7 8 9 10
Matching steps
Fig.1 - . Pearson correlation coefficients (ρ) for the seven SINTACS parameters
by couple matrix matching and progressive sliding along x-y axes. Series 3, 5 and
6 (Infiltration, Depth to water and Slope) show minor ρ values.
yy
REFERENCES
CIMINO A., FAUCI F., GRAMMAUTA R., GURRERA D. & OIENI A. (2009) -
Image processing in pollution vulnerability assessment of Sicily
aquifers. Epitome, 3, 26-27.
CIMINO A., COSENTINO C., OIENI A. & TRANCHINA L. (2008a) - A
geophysical and geochemical approach for seawater intrusion
assessment in the Acquedolci coastal aquifer (Northern Sicily).
Environm. Geol., 55, 1473-1482.
CIMINO A., ANDOLINA F., CAPPADONA IGNAZZITTO S. & OIENI A. (2008b)
- Recenti elaborazioni idrogeologiche e geofisiche nella fascia
costiera di Acquedolci - San Fratello (Messina). Acque Sotterranee,
25, 114, 9-23.
CIVITA M. & DE MAIO M. (2000) - SINTACS R5. Pitagora Ed., Bologna,
Italy, 226 pp.
CORNIELLO A. & DUCCI D. (2001) - The risk contamination map of the
aquifer underlying the middle Volturno River plain. Proceedings of
the 3rd International Conference on “Future Groundwater at Risk”
Lisbon (Portugal), June 2001, 25-33.
CORNIELLO A. & DUCCI D. (2005) - Carta della vulnerabilità
all’inquinamento del settore meridionale della Piana del F.
Volturno. 2nd International Workshop Aquifer vulnerability
assessment and mapping - 4th Congress on the Protection and
Management of Groundwater, Colorno, Italy, September 21-23
2005.
DUCCI D. (2010) - Aquifer vulnerability assessment methods: the nonindependence
of parameters problem J. Water Resource and
Protection, 2, 298-308.
6
5
3

Key words: Campania, carbonate aquifers, Conca di Acerno,
groundwater resource evaluation, hydrogeochemistry.
INTRODUCTION
The area concerned is the Acerno basin “Conca di Acerno”,
an intra-Apennine sink, sloping down in the south-western portion
of the Picentini Mountains (SA). The Conca di Acerno is located
at an altitude ranging between 700 and 750 m a.s.l. and it is
extended in direction NW-SE. It is bordered by carbonate mountains:
the Raia-Telegrafo Mts to the west, by the Accellica Mts
(1660 m a.s.l.) to the north-west, by Cervialto Mt to the East, by
the Polveracchio Mt to the South-East.
In the past, the Conca di Acerno was a lake basin, subsequently
filled by river and lake deposits and afterwards cut again
by the surface water. This has determined the existing morphology
which is characterized by terraced surfaces, (one of them
holds the small village of Acerno) and by deep valleys. Between
them, the Tusciano river valley lies to the south of Acerno and
the deep, narrow valley of Isca della Serra crosses the paleo-basin
from North to South.
Along the river-beds of the river Tusciano and the torrent Isca
della Serra, on the outskirts of the village of Acerno, there are
two important groups of springs (total flow rate 800 l/s), tapped
by the Ausino Consortium.
In the last thirty years, several hydrogeological studies were
carried out in the area (BUDETTA & DE RISO, 1982; PISCOPO et
alii, 1993, 2001). Moreover, at the end of the nineties, the Ausino
Consortium, with the aim to tap groundwater supplies on the right
of the river Tusciano, carried out hydrogeological surveys. This
data provided a basis for reviving the interest in the hydrogeological
problems of the area.
Really, all this data, integrated by piezometric, hydrochemical
and isotopic (d 18 O e d 2 H) surveys, has enabled to better define the
_________________________
Overview of the hydrogeology of the “Conca di Acerno” (SA)
ALFONSO CORNIELLO (*), DANIELA DUCCI (*) & GENNARO MARIA MONTI (**)
(*) Department of Hydraulic, Geotechnical and Environmental Engineering
University of Naples Federico II – e-mail: corniell@unina.it; daniela@unina.it.
(**) ISPRA, Roma – e-mail: gennaromaria.monti@isprambiente.it.
Study funded by the PRIN “Nitrate Contamination in Groundwater"
launched in 2007 (National and Local Project Coordinator, Prof. Alfonso
Corniello).
163
different hydrogeological aspects related to the origin of the
springs and it represents the basis for the groundwater flow modelling,
which is already under construction by using the
MODFLOW calculation code.
HYDROGEOLOGICAL SETTING
The most common lithotypes in the study area, included in a
rather complex geological and structural setting (ISPRA), consist
of Mesozoic carbonate rocks. These include older dolomitic
rocks (in the south-eastern sector of the area) and limestones,
outcropping in the eastern sector. Within the “Conca di Acerno”
at the top of the dolomitic rocks, there are river and lake sediments
(Pleistocene), including cemented breccia at the base, an
Fig. 1: Hydrogeological map of the "Conca di Acerno area". 1) Alluvial deposits
(prevalently gravel and sand, with silt). Medium-high permeability; 2)
Slope debris and debris deposits. Medium-high permeability; 3) Marlycalcareous-clayey
deposits. Very-low permeability; 4) Limestone. High-very
high permeability; 5) Dolomitic limestone. High permeability 6) Dolostone.
Medium-high permeability; a) fault; b) groundwater flow divide; c) groundwater
flow direction (dotted symbol represents shallow flow); d) spring.
intermediate silty-sandy level and conglomerate at the top.
Part of the recharge flows towards various small springs
spread over the entire basin; but the larger volume of the recharge
contributes to feed a deep circulation in the dolomitic bedrock of
the Conca di Acerno. The groundwater of this aquifer flows towards
the two above mentioned groups of springs,located at the
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east (Ausino, Ausinetto and Avella group; total flow 400 l/s) and
the at the south (Olevano spring).of the Acerno village. Moreover,
groundwater produces a noticeable increase in streamflow
of the river Tusciano and of the Isca della Serra torrent.
The first group of springs, located on the left of the Isca della
Serra torrent at an elevation between 563 and 569 m a.s.l., is the
outcrop of the groundwater table of the dolomitic bedrock, here
fairly shallow (approx. 50 m), confined by the lake deposits of
the Conca.
Fig. 2: Exploitation of the groundwater leakages through the Tusciano riverbed.
The Olevano spring (200 l/s) is located on the right bank of
the river Tusciano (at approx. 552 m a.s.l.), at the foot of a high
ridge formed by breccia belonging to the river-lake deposits. Still
on the right bank, not far from the spring, there is the above mentioned
significant diffuse leakages of ground water through the
riverbed.
CONCLUSIONS
The study of available and acquired data yielded the following
main results about groundwater flow system in the Acerno
basin (Conca di Acerno), sometimes in disagreement with previous
studies:
• two different groundwater flows have been identified: the
first one in the carbonate bedrock (feeding the Ausino, Ausinetto
and Avella spring group) and the other one in the river and lake
sediments of the basin (feeding the Olevano spring and the leakages
through the Tusciano riverbed;
• a significant flow increase in the Tusciano river has been
identified coming from the right bank of the river Tusciano;
• analyses of chemical, isotopic and piezometric data
showed that occurs an interaction between the two aquifers, and
between these and the hydrographic network;
• the limits of the groundwater basin feeding the Acerno
spring group have been established more accurately, especially
on the basis of the carried out hydrogeological balance. In fact,
164
the area of the groundwater basin has been reduced and, to the
east, brought to correspond with the position of an important tectonic
lineament, located south of the Mt. Raia della Licina;
• level with the river Tusciano, major tectonic lineaments
act as a groundwater flow barrier toward south.
The further step of this study has been to construct a groundwater
flow model to achieve the optimal simulation of the hydrodynamic
characteristics of carbonate aquifers. Pursuing this objective,
and especially the estimation of the surface-groundwater
interaction, the hydraulic characterization of the limestone aquifers
has been carried out also through geostructural analysis of
outcrops.
REFERENCES
BUDETTA P. & DE RISO R. (1982) - Studio idrogeologico delle
sorgenti della conca di acerno (Monti Picentini). Memorie e
note dell’Istituto di Geologia Applicata, 16, 7-27.
PISCOPO V., AQUINO S., GENCO S. & SCIUMANÒ E. (2001) - Sulla
presenza di falde sospese nel rilievo carbonatico del Monte
Accellica (Campania). Mem. Soc. Geol. It., 56, 235-241.
PISCOPO V., CAVALLARO G., PACE G., VITIELLO P., & AQUINO S.
(1993) - Schema idrogeologico dei Monti Accellica e Licinici
(Campania). Geol. Appl. Idrogeol., 28, 611-617.

Monitoring water and underground flow in the gypsum karst areas
of Emilia Romagna region
Key words: Monitoring, gypsum, karst, hydrogeology, chemistry.
INTRODUCTION
Karst areas in Emilia Romagna region are almost exclusively
hosted in evaporites. Although gypsum outcrops occupy less than
1% of the entire regional territory, these areas host almost 600
caves (DEMARIA, 2003). Gypsum karst constitute very important
habitats hosting many plant and animal species that are found
only in these areas. Most of the evaporite outcrops are part of the
Habitat network and are designed as Sites of Communitary
Interest (SIC). These sites are: SIC IT4030009 Triassic Gypsum
(Upper Secchia Valley, Reggio Emilia), SIC IT4030017 Cà del
Vento-Cà del Lupo-Gypsum of Borzano (Reggio Emilia), SIC
IT4050001 Gypsum areas of Bologna-Abbadessa Calanchi
(Bologna), SIC IT4050027 Gypsum areas of Monte Rocca,
Monte Capra and Tizzando (Zola Predosa, BO), SIC IT4070011
Vena del Gesso Romagnola (Faenza/Imola) and SIC IT4090001
Onferno (Rimini)(Figure 1).
The underground water circulation and quality of these areas
has been studied only fragmentarily (FORTI& FRANCAVILLA,
1990), with some karst areas that are particularly well known
from a hydrogeological point of view (e.g. Poiano springs)
(AA.VV., 1988; CHIESI &FORTI, 2009), others that have been
studied moderately in the past (e.g. Spipola and Rio Stella Basino
cave systems, Borzano karst area) (FORTI et alii, 1985, 1989;
FORTI & CHIESI, 2001) and some for which only scarce
information is available (e.g. Gypsum areas of Rontana and
Castelnuovo) (BENTINI &LUCCI, 1999). For many areas there is
almost nothing known on quantity and quality of underground
water in the gypsum karsts.
In the framework of a Project LIFE+, together with a series of
environmental projects, the monitoring of the waters in these
SICs has been programmed in the period 2010-2014 with the aim
_________________________
(*) Italian Institute of Speleology, University of Bologna,
jo.dewaele@unibo.it
Lavoro eseguito nell’ambito del progetto LIFE+ 08 NAT/IT/00369
“GYPSUM” con la collaborazione della Federazione Speleologica della
Regione Emilia Romagna, del Dipartimento di Scienze della Terra e
Geologico-Ambientali (B.
dell’Università di Bologna
Capaccioni) e della Facoltà di Agraria
JO DE WAELE (*)
165
of assessing the quality and quantity of water entering and leaving
the gypsum outcrops ex-ante and ex-post. These chemical and
microbiological data will be useful to assess the quality of these
natural environments and to undertake, if necessary, measures to
mitigate the impact of these habitats.
METHODS
Since May 2010 a sampling campaign has started on a total of
more than 40 sites representing the major sinking streams,
underground streams and karst springs of the 6 SICs. Sampling
will take place once every three months for a total of at least 5
samples (15 months). In 4 of the most important karst systems
(Onferno cave, Rio Stella-Rio Basino karst system, Spipola-
Acquafredda cave system and Tanone della Gaggiolina cave)
weirs have been constructed to allow the continuous monitoring
of water level (and thus flowrate), electrical conductivity and
temperature with a Data logger DLN70 multi.
Three samples are collected at each site (250 ml and 500 ml
of normal water and 100 ml of water filtered with a 0.45 μm
sterile filter and acidified with 1 ml of concentrated HNO3). At
each sampling site pH, temperature and conductivity are
measured in situ with a Hanna Combo portable sensor. The 500
ml bottle is sent for microbiological analyses.
Fundamental metals (Na+, K+, Mg2+ and Ca2+) will be
analysed with an Atomic Absorption Spectrophotometer (AAS),
minor and trace metals and semimetals (Pb, As (tot.), Cu, Zn, Cd
etc.) with ICP-OES instead. Major anions (SO42+, Cl-, F-, Brand
NO3-) will be analysed with Ionic Chromatography, the
nitrogen species (NH4+, NO2-) by Colorimetry, Chemical
Oxygen Demand (COD) through a return titration after oxidation
with Potassiumdichromate.
ATTENDED RESULTS
This monitoring campaign will start to give its first results in
the early summer, after the first samples taken in May 2010 will
have been analysed. By that time also the 4 weir and monitoring
sensors will be in full activity.
The chemical results will allow to identify possible pollution
in some of the monitored sites, and will in general allow to assess
the quality of the waters entering and exiting the karst areas.
Further sampling might reveal variations in the chemical and
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Fig. 1 - Gypsum karst areas in Emilia Romagna region.
microbiological quality of the waters due to sporadic episodes of
pollution.
In the sites in which variations are generally low and there are
no signs of pollution sampling will be reduced after around 15
months (after the 5 th sample) to one sample a year. Some
important stations (e.g. Rio Stella-Rio Basino and Spipola) will
be monitored for the entire 5 years of the LIFE+ project.
REFERENCES
AA.VV. (1988) - L'area carsica dell'alta Val di Secchia,
studio interdisciplinare dei caratteri ambientali. Studi e
Documentazioni, 42. Reg. Emilia Romagna – Prov.
Reggio Emilia, 1-303.
BENTINI L. & LUCCI P. (1999) – Le grotte della Vena del
Gesso Romagnola. I gessi di Rontana e Castelnuovo.
FSRER, 23-26.
CHIESI M. & FORTI P. (eds.) (2009) - Il Progetto Trias: studi
e ricerche sulle evaporiti triassiche dell’alta valle di
Secchia e sull’acquifero carsico di Poiano (Reggio
Emilia). Mem. Ist. It. Spel., s. II, 22, 1-164.
166
DEMARIA D. (2003) – Emilia Romagna. In: Madonia G. &
Forti P. (Eds.), Le aree carsiche gessose d’Italia. Mem. Ist.
It. Spel., s. II, 14, 159-184.
FORTI P. & CHIESI M. (2001) – Idrogeologia, idrodinamica e
meteorologia ipogea dei gessi di Albinea, con particolare
riguardo al Sistema carsico afferente alla Tana della
Mussina di Borzano (Er-RE 2) (Albinea-Reggio Emilia).
In: Chiesi M. (Ed.), L’area carsica di Borzano (Albinea-
Reggio Emilia). Mem. Ist. It. Spel., s. II, 11, 1-139.
FORTI P. & FRANCAVILLA F. (1990) - Gli acquiferi carsici
dell’Emilia-Romagna: conoscenze attuali e problemi di
salvaguardia. At. Parm., Acta Nat., 26 (1-2), 69-80.
FORTI P., FRANCAVILLA F., PRATA E., RABBI E., VENERI P. &
FINOTELLI F. (1985) - Evoluzione idrogeologica dei
sistemi carsici dell’Emilia-Romagna: 1- Problematica
generale; 2- Il complesso Spipola - Acqua Fredda.
Regione Emilia Romagna, Tip. Moderna, Bologna, 1-60.
FORTI P., FRANCAVILLA F., PRATA E., RABBI E. & GRIFFONI
A. (1989) - Evoluzione idrogeologica dei sistemi carsici
dell’Emilia- Romagna: il complesso Rio Stella-Rio Basino
(Riolo Terme, Italia). Atti XV Congr. Naz. Spel., 349-
368.

A multidisciplinary approach for the management of the water
resources hosted in the multi-layer coastal aquifers of Central-
Southern Tuscany
MARCO DOVERI (°), ANDREA CERRINA FERONI (°), SIMONE DA PRATO (°), ALESSANDRO ELLERO (°),
MATTEO LELLI (°), LUIGI MARINI (°)(*), GIULIO MASETTI (°),
BARBARA NISI (°) & BRUNELLA RACO (°)
Key words: Central-Southern Tuscany, geology, hydrogeology,
hydrogeochemistry, water management.
INTRODUCTION
The correct management of subterranean water resources
must be based on the knowledge of their geologicalhydrogeological-geochemical
framework. Stemming from this
axiom, the subterranean water resources hosted in the multi-layer
aquifers below the coastal plains of the Cecina River, Cornia
River, Follonica, Grosseto, and Albegna River (Fig. 1) were
recently investigated through a multidisciplinary approach in the
Fig. 1 – Location of the SSWB (Significant Subterranean Water Bodies) studied.
framework of the Significant Subterranean Water Bodies
(SSWB) Project funded by the Tuscany Region.
167
METHODS
The first step of this investigation consisted in the geometrical
reconstruction of the geological sequences of interest, through the
interpretation of available stratigraphical data, aimed at the
distinction of main aquifer, aquitard, and aquiclude levels (Fig.
2). The total volumes and the percentages of the different grain
sizes were also calculated for each hydrogeological complex.
Fig. 2 – Block Diagram of Hydrostratigraphic model.
The second step was addressed to elaborate the piezometric
surfaces (Fig. 3) during low-flow and high-flow conditions, to
individuate the flow pattern and the most exploited zones of the
multi-layer aquifers. Moreover, considering the saturated zone
and applying an effective porosity (weighed in function of grain
sizes percentages), the amounts of the total water volumes stored
in the aquifer system were estimate.
The third step comprised the hydrogeochemical
characterization of the areas of interest, through the adoption of
both:
(i) a deterministic approach, including the elaboration and
interpretation of diagrams for water classification (Fig. 4), Eh-pH
plots, calculation of water speciation and saturation state with
respect to relevant solid phases, activity diagrams, etc.
(ii) a geo-statistical approach for mapping the most
significant geochemical parameters (Fig. 5), such as the
concentrations of chloride, sulfate, nitrate and boron.
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Fig. 3– Piezometric sketch map.
Fig. 4 – Langelier Ludwig-Cl.
168
Fig. 5 – Example of geo-statistical mapping.

The study of the seawater intrusion in the Versiliese-Pisan coastal
plain (North-Western Tuscany) by means of hydrogeological,
chemical and isotopic tools
MARCO DOVERI (*), ROBERTO GIANNECCHINI (**) & MATTEO BUTTERI (°)
Key words: Hydrochemistry, hydrogeology, Northern Tuscany,
piezometric condition, seawater intrusion, water isotopes.
INTRODUCTION
The multilayered aquifer system of the Versiliese-Pisan
coastal plain is mainly made up of sandy and gravelly horizons.
The aquifers are locally affected by intense exploiting for
drinking, industrial and irrigation uses, which favours seawater
intrusion. In order to study this phenomenon and understand the
mixing mechanism with freshwater, a project co-financed by the
Migliarino-S.Rossore-Massaciuccoli Regional Park is being
carried out since 2005. This project consists in a multidisciplinary
study carried out by means of hydrostratigraphic correlations,
water level measurements and physico-chemical (electric
conductivity-EC, temperature, pH), chemical (principal chemical
elements and Br) and isotopic analysis (18O/16O and 2H/1H
ratios).
The main results regarding the zones between Burlamacca
Canal and Bufalina Ditch (zone A) and between Arno River and
Scolmatore Canal (zone C) are presented (detailed description of
the results are available in Doveri et alii, 2009). In the
intermediate area (zone B) the study is still in progress.
In the zone A the 30 m thick unconfined sandy aquifer was
studied, whereas in the zone C the confined gravelly aquifer (10-
20 m thick) located at a depth between 50 and 100 m below the
sea-level was analyzed. Sampling and field measurements were
carried out both in high and low level conditions and, where
possible (piezometers and wells without pump), for groundwater
of the unconfined sandy aquifer (zone A) sampling was done at
different depths in order to verify the freshwater-seawater
interface.
RESULTS
The unconfined sandy aquifer (Zone A): water level contour
________________________
(*) Institute of Geosciences and Earth Resources (IGG) - CNR, Pisa
doveri@igg.cnr.it
(**) Dipartimento di Scienze della Terra - Università di Pisa
rgiannecchini@dst.unipi.it
(°) Geologist, external collaborator, e-mail butteriit@yahoo.it
169
Fig. Fig. 1 – 1 Oxygen-18 – Oxygen-18 vs. vs. Electric Electric Conductivity. (1 (1 and and 2 - 2well/piezometer - well/piezometer in in
Sept.’05 and and Apr.’06, respectively; 3 and 3 and 4 -4 surface - surface water water in in Sept.’05 and and
Apr.’06, respectively; 5 - 5 seawater; - seawater; 6 -6 mixing - mixing curve curve between local local freshwater and and
Massaciuccoli Lake Lake water; water; 7 - 7 mixing - mixing curve curve between local local freshwater and and
seawater. Labels Labels with with suffix suffix BIS, BIS, TER, TER, etc. etc. are are related related to different to different depth depth samples).
obtained for this aquifer showed low piezometric heads, up to
negative values, in the zone close to the shoreline and in the
internal part of the study area, close to the Massaciuccoli Lake
and the “artificial canals and lakes (quarries) system”. These
piezometric minimums are linked to groundwater pumping,
principally by tourism establishments and nurseries gardening.
Lower (600-800 μS/cm) and higher (up to 17,000 μS/cm) EC
values were found in the high and low water level zones,
respectively. The highest EC was detected in surface water, in
particular in the Burlamacca Canal. Most of the analysed water
samples, that have low EC, are characterized by HCO3-Ca
composition, whereas water with high EC are of the Cl-Na type.
As pointed out in Fig.1, most samples with lower EC have
δ 18 O‰ values between -5.0 and - 6.0, which are compatible with
local rainfall infiltration. Some groundwater and surface water
samples are characterized by higher values of both EC and
δ 18 O‰, plotting along the seawater-freshwater mixing curve.
This behaviour is more evident for groundwater sampled at
higher depths and for the sample collected in the Burlamacca
Canal (BB18). A maximum salt water percentage variable in the
intervals 15-30% (depending of the seasonal period) was
identified. The freshwater-seawater mixing is present both in the
zone near the shoreline and in the internal zone. In the second
case the presence of salt water in the aquifer is connected to
drainage from the artificial lakes and canals, which receive
seawater through the Burlamacca Canal. Analysis of samples
collected at different depths highlighted that the freshwater-
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seawater transition zone is at a depth of about 25 and 20 m near
the shoreline and in the internal side of the studied territory,
respectively.
Massaciuccoli Lake and its emissary (BB47) have very
different features in agreement with the results of BANESCHI
(2006) study, which highlight that the chemical and isotopic
properties of these water bodies are influenced by both anthropic
contribution and a high evaporation rate.
The confined gravelly aquifer (Zone C): the overexploitation
of the gravelly aquifer determines water levels below the sealevel
on most of the coastal territory. Two local and more
accentuated piezometric depressions are present in the S. Piero
and Calambrone zones (Fig.1), where the main farms are present.
In the water-wells belonging to these areas we also recorded
higher EC values (7,000 and 6,460 μS/cm, respectively).
Chemical composition points out that in the study area the
gravelly aquifer is characterized by a water circulation with
prevalently Ca/HCO3-SO4 composition, which evolves towards
Na/Cl composition. Samples with high Cl contents have Na/Cl
and Br/Cl ratios comparable to those of seawater. As regards the
isotopic contents, most groundwater samples are grouped into
values of δ 18 O‰ and δ 2 H‰ of about -6.5/-6.8 and -37/-40,
respectively. Such values are typical of the water circulating in
the confined gravelly aquifer of the internal portion of the Pisan
Fig. 2 – Piezometric sketch map of the confined gravelly aquifer.
Plain (GRASSI & CORTECCI, 2005) and are representative of
recharge altitude higher than the plain. For some samples a shift
of isotopic ratios from the main group toward higher values of
δ 18 O‰ and δ 2 H‰ was observed. This behaviour is particularly
evident for surface water sampled in the Arno River. Comparing
the δ 18 O‰ and Cl contents (Fig.3), we observe that the samples
with higher values of such parameters in some cases belong to the
curve of mixing between gravelly aquifer groundwater and
170
Fig. 3 – Binary diagram?δ 18 O‰ vs. Cl (GG-SW: gravel groundwater-seawater
mixing; SG-SW: sand groundwater-seawater mixing).
seawater, in other cases they stay between this curve and that
representative of the mixing between shallow sandy aquifer
groundwater and seawater. The presence of seawater was verified
in maximum percentages of about 7-9%. Higher fractions of salt
water insist in the two zones where high pumping rates determine
a water level largely below the sea-level. In the first zone, located
in the southern part within 2 km from the shoreline, chemical and
isotopic data clearly show a direct seawater intrusion through the
gravelly aquifer. For the second zone, located near the Arno
River and about 6 km far from the sea, in order to justify the
isotopic behaviour it is necessary to admit that the seawater in the
mixing process derives from the Arno river-shallow sandy
aquifer system, which is, in a limited area, likely in contact with
the gravelly aquifer.
REFERENCES
BANESCHI I. (2006) - Geochemical and Environmental study of a
coastal ecosystem: Massaciuccoli Lake (Northern Tuscany,
Italy). PhD. Cà Foscari University of Venice.
DOVERI M., GIANNECCHINI R., GIUSTI G. & BUTTERI M. (2009) -
Studio idrogeologico-geochimico dell’acquifero freatico
nella zona compresa tra il Canale Burlamacca ed il Fosso
della Bufalina (Viareggio, Toscana). Eng. Hydro. Env.
Geology (Giornale di Geologia Applicata), 12, 101-117.
GRASSI S. & CORTECCI G. (2005) - Hydrogeology and
Geochemistry of multilayered confined aquifer of the Pisa
Plain. Appl. Geochem., 20, 41-54.

Pianosa Island (Tuscan Archipelago, Italy) groundwater:
hydrogeological and hydrogeochemical features
of a very peculiar aquifer
MARCO DOVERI (*), ROBERTO GIANNECCHINI (**), MARIO MUSSI (*), IRENE NICOTRA (***) & ALBERTO PUCCINELLI (**)
Key words: Aquifer, hydrogeochemistry, hydrogeology, Pianosa
Island, Tuscan Archipelago.
INTRODUCTION
The Pianosa Island, one of the 7 islands of the Tuscan
Archipelago, is formed by Neogenic-Quaternary sedimentary
rocks and is characterized by an unusual and peculiar flat
morphology (Fig. 1). This feature, together with good
hydrogeological properties of the bedrock, assures significant
groundwater resources, in spite of the island little extent (just
10.2 km 2 ) and the poor rainfall amount recorded on it (less than
500 mm mean annual precipitation). This situation allowed in the
past of supporting the presence of about 2,000 people.
Pianosa Island
Pianosa
Island
Fig. 1 – Location map of the Pianosa Island.
Elba
Island
_________________________
(*) Istituto di Geoscienze e Georisorse – C.N.R., Pisa, doveri@igg.cnr.it
(**) Università di Pisa - Dipartimento di Scienze della Terra,
rgiannecchini@dst.unipi.it
(***) Provincia di Livorno, i.nicotra@provincia.livorno.it
171
Unfortunately, in the 90’s the intense exploitation of the
aquifer and the land use (partly destined to agricultural activity,
partly to cattle-breeding, associated to the local penal settlement)
caused a progressive deterioration of the water resource,
highlighted by seawater intrusion and pollution.
The closing of the penal settlement (occurred in 1998)
determined a requalification of the groundwater, with raising of
the piezometric level and improvement of the water quality,
although high NO3 values are currently found in some shallow
wells, probably again associated to the past land use.
The aim of this research is the characterization of the aquifer
Fig. 2 – Piezometric map of the Pianosa Island phreatic aquifer.
system of Pianosa Island from a hydrogeological and
hydrogeochemical point of view, by means of a multidisciplinary
approach, using classic hydrogeological methods and
hydrochemical-isotopic methods. In fact, with the exception of
SESSIONE 7

SESSIONE 7
Fig. 3 – Geological cross-section of Pianosa Island (after Sandrelli & Foresi, 2005 modified). Marina del Marchese Fm.: marl and silty marl with calcareniti
interbedded, Burdigalian; Golfo della Botte Fm.: clay with conglomerate and sandstone interbedded, Up. Tortonian-Messinian (?); Pianosa Fm.: calarenite,
Pliocene-Pleistocene (?).
some published papers (e.g. RAGGI, 1983; BARTOLETTI et alii,
2003; NICOTRA et alii, 2010) and unpublished reports (e.g.
Provincia di Livorno, Arpat), the Pianosa aquifer is not so known.
RESULTS
The study highlighted that the groundwater circulation is
Fig. 4 – Piper-Hill diagram of the Pianosa groundwater.
substantially controlled by the hydro-structural conditions of the
aquifer system. The morphology of the water table (Fig. 2) shows
a general W-E flow direction, due to the dip direction of the
contact between the outcropping permeable calcarenite and the
underlying impermeable marly-clayey rocks (Fig. 3).
Nevertheless, the last presents conglomerate and sandstone
intercalations, sometimes in contact with calcarenite. The contact
zones let the continuity of the groundwater circulation, which is
phreatic in the calcarenite, and confined in the conglomerate and
sandstone horizons (the main wells currently used are drilled in
these horizons). These particular hydrodynamic conditions are
also well experienced by the difference analyzed between the
water level measured in shallow and deep wells located in the
same zone.
The groundwater budget points out that the aquifer system
172
recharge occurs in a limited period of the year (January-March),
as confirmed also by isotopic data.
In agreement with the hydro-structural and piezometric
conditions, the hydrogeochemical analyses confirm the recharge
of the confined horizons (conglomerate and sandstone) by the
superficial calcarenite. The isotopic data indicate that the aquifer
system is supplied by direct infiltration of rainfall.
From a chemical point of view, most groundwater samples is
classifiable as intermediate facies, Na-Cl/Ca-HCO3 (Fig. 4),
produced by the combination of two phenomena: the sea spray
and the circulation in a prevalently carbonate aquifer. In the
Eastern portion of the island, clearly Na-Cl groundwater prevails.
The water table conditions and the isotopic data highlight the
seawater intrusion phenomenon in the unconfined aquifer in this
area. Comparing recent and past data, we can note a significant
predisposition to this phenomenon. In fact, the seawaterfreshwater
interface is at present going backwards in comparison
with the past situation, characterized by larger exploitation.
Nevertheless, such regression is not so accentuated, due to the
scarcity of rainfall occurred in the years before this research.
REFERENCES
BARTOLETTI E., BINI A. & RUCCI C. (2003) - Un acquifero in
mezzo al mare: l’Isola di Pianosa. Atti del 4° European
Congress on Regional Geoscientific Cartografy and
Information System, Bologna 17-20 giugno 2003.
NICOTRA I., DOVERI M., GIANNECCHINI R., MUSSI M. &
PUCCINELLI A. (2010) - Risultati preliminari dello studio
della circolazione idrica sotterranea nell'Isola di Pianosa
(Arcipelago Toscano, prov. Livorno). Atti Congresso Codice
Armonico 2010 - III Congresso Regionale di Scienze
Naturali. Castiglioncello (LI), 11-13/03/2010, 96-107.
RAGGI G. (1983) - Le acque del sottosuolo dell’Isola di Pianosa.
Atti Soc. Tosc. Sci. Nat., Mem., Serie A, 90, pagg. 75-84.
SANDRELLI E. & FORESI L.M. (2005) - Carta Geologica 1:10.000
del Foglio 341 – Regione Toscana - Servizio Geologico,
http://web.rete.toscana.it/pta/servlet/Scarica?foglio=341

Translocation of Cr, Co and Pb from soil and water to forage plants
and their accumulation capacity
Key words: Accumulation capacity, chromium, cobalt, lead, soil,
water.
Chromium, cobalt and lead are among the most metalloid and
metals present in the environment. These contaminants are among
the most dangerous heavy metals to humans and the environment,
because of their toxicity towards all living organisms and their
accumulation capability.
When present in soil and water, they can accumulate in living
organisms, enter in food chain and affect human health, due to
their toxicity. In this work we investigated the accumulation of
Cr, Co and Pb by Trifolium repens Huia, Lotus corniculatus,
Festuca Arundinacea Demeter, Dactylis Glomerata, Trifolium
Pratensis, Lolium Perenne Livree, Lolium Multiflorum e Phleum
Pratense, the mix of these seeds for forage is commonly sold.
Soil samples were collected and, after being analyzed, 4
different concentrations of trace elements were added:
for Pb 10 μgL -1 ,100 μgL -1 , 200 μgL -1 and 500 μgL -1 ,
for Cr and Co 50 μgL -1 , 500 μgL -1 , 1000 μgL -1 and 2500 μgL -1
Only Trifolium repens, Lotus corniculatus and Festuca
Arundinacea survived the highest concentration of metals, the
others died after 1 month (62.5%). The concentrations of metals
absorbed or stabilized were determined for shoots of plants, roots
of plants and soil, it is important to evaluate the behavior of each
component.
The metal concentration in biomass was measured for all
plants and the bioconcentration factor (BCF metal concentration
ratio of plant roots to soil) and translocation factor (TF, metal
concentration ratio of shoots to roots) were calculated.
The behavior of each plant depends on the metal and its
concentration in the water. Analyzing the concentration of Pb
equal to 50 times the limit of law, in roots of Trifolium repens
reaches 5 ppb, while in Phleum pratense climax Pb reaches 145
ppb. Pb in other plants is fixed at the roots with a concentration
between 15 ppb and 95 ppb. Pb in the shoots of Festuca
Arundinacea does not reach 10 ppb, in all other plants the
concentration of Pb in the shoots varies between 25 ppb and 55
ppb. Exception is Trifolium pratensis where the concentration of
_________________________
(*) Politecnico di Torino, adriano.fiorucci@polito.it
ADRIANO FIORUCCI (*), ELENA COMINO (*) & STEFANIA MENEGATTI (*)
1
173
Pb in the shoots reached 95 ppb.
The concentration of Co in roots of Trifolium repens,
Trifolium pratensis and Lotus corniculatus reaches 5 ppb, while
in Phleum pratense climax Co reaches 62 ppb. Co in other plants
is fixed at the root with a concentration between 28 ppb and 40
ppb. Co in the shoots of Festuca Arundinacea, del Lotus
corniculatus, della Dactylis Glomerata does not reaches 5ppb, in
all other plants the concentration of Co in the shoots varies
between 10 ppb and 28 ppb. Trifolium repens is the exception,
the concentration of Co in the shoots reached 35 ppb.
In the roots of Dactylis Glomerata, Festuca arundinacea and
Lolium perenne Liveries the concentration of Cr reaches 140 ppb,
while in Lotus corniculatus Cr stops at 10 ppb. Only Phleum
Pratense climax has stabilized to roots the concentration of Cr
equal to 200 ppb. Cr in the shoots of plants has reached the
concentrations between 10 ppb and 30 ppb. Only Dactylis
Glomerata not exceed 5 ppb. Exceptions are the Trifolium repens
and Trifolium pratensis where the concentration of Cr in the
shoots varies between 110 ppb and 142 ppb.
This work is novel because the results show:
the plants can grow in the presence of metals, they can capture
and transfer them to the aerial parts;
special attention has been paid to these crop plants for their
possible use in phytoremediation
expecially to avoid the possible introduction of the metals
accumulated in aerial parts into the food chain when they grow in
contaminated areas.
The metal that moves from soil to plants does not always
reflect the metal entering in the feed and food. We propose for
next studies to analyze the metals present in the food in order to
evaluate a “food chain transfer coefficient”.
SESSIONE 7

SESSIONE 7
Key words: Basic quality, groundwater, hydrochemical facies,
metals, Susa Valley.
INTRODUCTION
The aim of this study is to characterize in hydrogeochemical
terms the unconfined aquifer of an area that extends from the
entrance to the Susa Valley to the City of Bussoleno (Piemonte,
Italy).
The concentrations of the main ions and of some heavy metals
(arsenic, hexavalent chromium, nickel, lead, rubidium, uranium
and vanadium) were determined.
Through diagrams and maps it was possible to identify the
hydrochemical facies of the analysed water, the basic quality of
the water destined for human supply and the pollution due to
metals.
Schöeller’s diagram, along with the characteristic ionic ratios,
have enabled to identify four hydrochemical facies characterized
by the dominance of Bicarbonate and Calcium; in some samples
there was a higher content of chloride and alkaline, while one
sample was detected dominance of Sulphate.
The identified hydrochemical facies depend on the
mineralogical composition and lithology, the trend of the flow
field, the decanting of waters from areas to higher altitudes
especially on the left orographic side, the recharge areas framed
between Reano, Avigliana and Buttigliera Alta and anthropic
influence.
In order to evaluate the possible use of the groundwater
resources from the drinking water point of view, the quality was
evaluated on the basis of certain parameters that cause a
deterioration in the classification of use of the water (electrical
conductivity, chlorides, nitrates, sulphates, ammonium ion, iron,
manganese).
According to the classification set by the Ronchi Decree,
Decree. 152/99, the waters of the unconfined aquifer have a
significant, if not relevant, anthropic impact in most of the study
_________________________
(*) Politecnico di Torino, adriano.fiorucci@polito.it
Hydrogeochemical study of the unconfined aquifer
of Low Susa Valley
ADRIANO FIORUCCI (*) & BARBARA MOITRE (*)
174
area.
The results obtained show how the groundwater of the
unconfined aquifer is unsuitable for human supply; in the
majority of cases, the quality of the water depends on the high
concentrations of iron and manganese dissolved in the
groundwater.
The study of concentrations of major metals, it appears to be
the basis of the aquifer vulnerability with the ability to identify
danger centers. Through the isoconcentration maps it has been
possible to highlight that there are some areas, generally highly
industrialized, where concentrations of metals show maximum
peaks that deviate far from the adjacent areas with rural
settlements.
The trend of the concentration of metals is consistent with the
hydrodynamics of the aquifer and in general presents a maximum
in the left orographic side, where there is a confirmation of the
low quality of water for human supply.
In addition to some main heavy metals such as chromium,
nickel and lead, nitrates also have the same areas with the greatest
concentration, probably due to the presence in the territory of
invasive human activities.

Key words: Hydrochemical, hydrodynamical, springs,
vulnerability of the aquifers.
Some years ago, the Applied Hydrogeologic Work Group of
the Politecnico di Torino installed a series of automatic water
level, temperature and electric conductivity acquiring devices,
and have carried out sampling and chemical analyses at different
springs in the mountainous sector of the Ligurian Alps which are
supplied by aquifers in debris-alluvial deposits.
The main results obtained from four springs that are situated
at heights of between 900 and 1900 m a.s.l., three of which are
presently tapped for drinkable water, are presented in this work.
The four springs are characterised by a rather similar
hydrogeologic situation with aquifers located in rather coarse
sediments belonging to mixed fans of debris and alluvial deposits
over a relatively fractured metamorphic bedrock made up of
meta-vulcanite and quartz. The supply of these aquifers is only in
part due to direct infiltration from meteoric contributions, while a
remarkable loss component prevails below the bedrock in rivers
that flow along the fans themselves. This hydrogeologic situation
is rather common throughout the Piedmontese Alps where many
springs with these characteristics, even with somewhat reduced
discharges, are tapped for drinkable water purposes in order to
supply small sized aqueducts that are widespread and essential
for the economy of the territory. The study of their vulnerability
to contamination is therefore necessary for a correct management
of the water resources
The examined springs are: the Balmetta spring (960 m a.s.l.),
the Fontanas spring (1200 m a.s.l.) and the lower Borello spring
(945 m a.s.l.), which in part supplies the Villanova Mondovi,
Chiusa Pesio and the Langhe and Cuneo Alps Aqueduct
Consortium (CALAC). The Laghetto del Marguareis spring
(1220 m a.s.l.) is in part used to produce electric energy for the
alpine shelter nearby.
All these springs are characterised by a similar discharge
trend with a long winter low water period, and important spring
spate, connected to snow melting, a summer low water period
interrupted by parasitic spates and autumnal spates connected to
the local meteorological trend.
_________________________
Functioning and vulnerability of springs supplied by aquifers in
debris-alluvial deposits (Ligurian Alps – Piedmont, Italy)
ADRIANO FIORUCCI (*), BARTOLOMEO VIGNA (*), CINZIA BANZATO (*) & MASSIMO VINCENZO CIVITA (*)
(*) Politecnico di Torino, adriano.fiorucci@polito.it
175
The Balmetta spring has a discharge that varies between 10
and 40 l/s with somewhat rapid water flow variations, passing
from 10 to 30 l/s in only two hours. The yearly maximum
discharge half time is about three days, thus showing an elevated
degree of vulnerability of the spring. The temperature and electric
conductivity (EC) trends of the water show a “substitution” type
response with maximum EC values of about 125 μS/cm during
the low water periods and a minimum of about 35μS/cm when the
main discharge increases occur. The rapid mineralization
decrease, over a period of some hours, highlights the arrival of
new-infiltration water. The temperatures of the groundwater show
a trend that is generally influenced, with delays of about 1-2
months, by the seasonal conditions, with maximum values of
about 8° C in the months of September-October and minimum
values of about 5° C in April-May. The general trend is disturbed
by temporary increases and decreases of the temperature, of an
order of some tenths of a degree, thus highlighting the direct
supply of new-infiltration water. The hydrochemical data of the
spring water have confirmed an elevated degree of vulnerability
of the aquifer, which was obtained from the yearly maximum
discharge half time
The Fontanas spring (Pesio Valley) is characterised by a very
similar yearly water flow trend to that of the Balmetta spring, but
it has greater discharge variations with values of about 5 l/s
during the winter and summer low water periods and maximum
values of about 60 l/s during the principal infiltration events. The
yearly maximum discharge half time, which is about 2 days,
highlights an elevated degree of vulnerability to contamination.
The temporal trend of the principal natural tracers (temperature
and electric conductivity of the water) also shows a remarkable
similarity with the Balmetta spring and a marked typical
“substitution” response which points out the rapid arrival of the
new-infiltration water in spring. The mineralization of the water
is slightly higher than the previous spring (between 170 and 100
μS/cm), and is conditioned by the presence of carbonate rock
clasts and by the debris-alluvial rock mass.
The Laghetto del Marguareis spring (Pesio Valley) is
characterised by slightly greater discharges that reach values of
about 90 l/s during the spring spates, when the discharge
connected to the snow melting are summed together with the
rainfall contributions. The water flow in the winter months settles
at around 30 l/s and remains relatively constant between the
months of November and March, while the same value undergoes
SESSIONE 7

SESSIONE 7
remarkable increases in the summer-autumn period, reaching a
value of 80 l/s after storms or in the autumnal rainfall periods.
The yearly maximum discharge half time (which is usually
reached in the spring period) is of about 13 days, which
underlines a high degree of vulnerability.
This value is conditioned to a great extent by the type of
infiltration supply, which involves a snow melting process that
continues for several months and which greatly influences the
exhaustion curve of the spring.
The electric conductivity, which in low water periods is about
95 μS/cm, decreases very rapidly after important spate events and
reaches values of even less than 50 μS/cm, again highlighting a
“substitution” response. The temperature of the water, which is
conditioned by the mean height of the supply, that is, above 2000
m, is characterised by very low values of between 3-3.8° C,
which are recorded in the winter and summer low water periods,
and minimum values of about 2.4° C during the spring spates.
Although the temperature values of the water are not very
significant, because of the remarkable height of the examined
system, the rapid variations of the mineralization values in time
indicate that the new-infiltration water arrives in very brief times
and therefore indicate a rather elevated degree of vulnerability of
the aquifer.
The lower Borello spring (Corsaglia Valley) is characterised
by a more constant yearly water discharge trend than the
previously mentioned springs and shows summer and winter low
water values of about 35 l/s and maximum values of less than 80
l/s during the principal infiltration events. The yearly maximum
discharge half time (for the year 2007) furnished a value of about
9 days, thus indicating a high degree of vulnerability. The electric
conductivity is characterised by remarkable oscillations, with
maximum values of 210 μS/cm, recorded in the low water
periods, which fall to 130 μS/cm during the spates. The
fluctuations of the temperature of the water are even greater and
reach values of about 4° C in the winter season and go above 11°
C in the summer period.
These oscillations are closely connected to the way these
springs are supplied; they receive a direct contribution from the
losses from an important river below the bedrock (the Corsaglia
stream) which flows at just a few metres from the spring zone.
Two tests conducted with artificial tracers have confirmed that
the groundwater arrives at the spring in a period of just one hour.
The vulnerability of this aquifer is therefore decidedly elevated.
The examples mentioned above highlight the importance of
continuous monitoring systems in order to evaluate the
vulnerability of the aquifers and, as a consequence, to dimension
the areas of the spring tapped for drinkable water purposes that
have to be respected.
The installation of suitable instrumentation at the tapping
points (multi-parametric probes, which are currently available a
very reasonable prices) would allow data to be acquired that is
indispensable for the subsequent elaborations: with the values of
176
the spring discharge it is possible to calculate the yearly
maximum discharge half time, while it is also possible to gather
other information relative to the functioning and therefore the
vulnerability of a given aquifer from the interpretation of the
yearly trend of the temperature and electric conductivity of the
water.

Hydrogeological and geochemical features of the sandy unconfined
aquifer between Marina di Pisa and Calambrone (NW Tuscany)
affected by seawater intrusion
Key words: Coastal Pisan Plain, geochemistry, hydrogeology,
isotope, seawater intrusion.
INTRODUCTION
The Pisa Plain underground is formed by a complex
hydrogeologic structure, composed by discontinuous superficial
unconfined horizons and a multilayered confined aquifer, whose
main lithostratigraphic, hydrogeologic, piezometric and
hydrochemical features were described by several authors (e.g.
BALDACCI et alii, 1994; GRASSI & CORTECCI, 2005). The
unconfined aquifer, which is more or less continuously present in
most part of the Pisan Plain, in the study area is prevalently
characterized by sand and silty sand (15-17 m thick in the
northern portion, 9-12 m in the southern one). Below a clayey
impermeable basement is recognized. This area is characterized
by a significant anthropogenic pressure, due to the presence of
some tourist resorts, with bathing, sporting structures (golf,
racecourse, sporting centre) and agricultural activities in the
immediate inland. They need of considerable water amount, often
drawn from the unconfined aquifer. This area is therefore
particularly fragile from an environmental point of view. In order
to check the state of the seawater intrusion in the unconfined
aquifer, many hydrogeological and geochemical surveys have
been carried out.
HYDROGEOLOGY
Water table morphology and evolution were examined using
37 piezometers from April to September 2009. There is a general
and expected water table lowering, related to recharge reduction
and pumping rise, with partial reversal of trend already in
September.
During the investigated period high piezometric levels
(always above the sea level) are recognized close to the coastline
_________________________
ROBERTO GIANNECCHINI (*), MATIA MENICHINI (*), BRUNELLA RACO (**) & FEDERICO VITI (*)
(*) Università di Pisa – Dipartimento di Scienze della Terra,
rgiannecchini@dst.unipi.it
(**) Istituto di Geoscienze e Georisorse (CNR di Pisa), b.raco@igg.cnr.it
177
between Tirrenia and Calambrone (dune area). In the remaining
area, the water table is usually below the sea level, with marked
minimums in August and September in the inland between
Tirrenia and Calambrone and in the Marina di Pisa inland.
In Fig. 1 the water table map, obtained in August, is shown.
This period corresponds to the low stage in 2009.
Fig. 1 - Water table map in August 2009.
In April and September 2009 the electric conductivity (EC)
data were also collected, and conductimetric logs in several
piezometers were obtained, providing an indirect and quick
measure of the water salinity. In agreement with piezometric data,
near the coastline EC is lower than the remaining area. This
feature conflicts with that expected referring to seawater intrusion
phenomenon and it could be explained only admitting pumping
that favours the seawater drawing in aquifer. However, the EC
values are not in general so low, with minimums of about 2,000
μS/cm at a depth of -2 m a.s.l. Fig. 2 shows the September EC
map referred to the depth of -10 m a.s.l.: the aquifer is almost
involved in seawater intrusion, with particularly worrying
situation in the Marina di Pisa and Calambrone inlands.
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SESSIONE 7
Fig. 2 - Electric conductivity map (at -10 m a.s.l.) in September 2009.
GEOCHEMISTRY
In order to obtain detailed information about seawater
intrusion in the unconfined aquifer and for a better
comprehension of the hydrogeological setting mentioned above,
three sampling surveys were carried out in September 2008, May
2009 and February 2010. Samples were collected by means of in
situ analyses (physical-chemical parameters), laboratory analyses
of main chemical components (Ca, Mg, Na, K, Cl, SO4, NO3,
NH4, NO2) and some stable isotope ratios ( 2 H/ 1 H and 18 O/ 16 O of
H2O). Based on the Langelier-Ludwig diagram it is possible to
distinguish three main groups of water with distinctive
composition: Ca-HCO3 water, representative of circulation in
alluvial aquifer; Na-Cl water, whose composition is generally due
to the mixing of Ca-HCO3 with seawater; and Na-HCO3 water,
whose composition is probably due to ionic exchange process
between Ca 2+ in solution and Na + in clay minerals. Some samples
show intermediate composition among the above described
hydrochemical facies. Isotopic composition of many samples
collected near the Arno and Scolmatore rivers and the inland
plain indicates the presence of seawater. Using correlation
diagrams and mixing line, the rate between freshwater and
seawater was determined (Fig. 3).
178
δ 18 O ‰
2
0
-2
-4
-6
-8
unconfined aquifer
confined aquifer
Butteri et al., 2009
confined aquifer
RMC1 e RMC2
10 100 1000
Cl (mg/l)
10000 100000
Fig. 3 - Binary diagram 18O versus Chlorine, The mixing line is
reported in red.
DISCUSSION
Based on hydrogeological and geochemical-isotopic
approach, the results confirm that the seawater intrusion occurs
mainly both by direct drawing in aquifer, above all near Arno and
Scolmatore outpouring, and by circulation along the river with
consequent aquifer infiltration. The Marina di Pisa inland, Camp
Darby and Tirrenia sporting centre result particularly fragile
zones. The percentage of seawater in samples collected in this
zone is highest than 50%.
The dune area between Marina di Pisa and Calambrone can
be considered a recharge area by direct infiltration of rainfall.
The confided aquifer usually is separated by unconfined
aquifer, but locally there are hydraulic connections. This is
generally due to bad-completion wells.
REFERENCES
SEAWATER
100%
RMS 51
RMS 46
RMS 50
80%
RMS 53
BALDACCI F., BELLINI L. & RAGGI G. (1994) - Le risorse idriche
sotterranee della Pianura Pisana. Atti Soc. Tosc. Sci. Nat.
Mem., ser. A, 101, 241-322.
GRASSI S. & CORTECCI G. (2005) - Hydrogeology and
Geochemistry of multilayered confined aquifer of the Pisa
Plain. Appl. Geochem., 20, 41-54.
10%
50%

Key words: Advective transport, heat flow, low-enthalpy GWHP,
Turin.
INTRODUCTION
The increasing diffusion of low-enthalpy geothermal openloop
groundwater heat pumps (GWHP) providing buildings air
conditioning requires a careful assessment of the overall effects
on groundwater system, especially in the urban areas (LO RUSSO
&CIVITA, 2009; NAM &OOKA, 2010).
In the present study we discuss the first experimental results
derived by the groundwater monitoring around an injection well
of an open-loop GWHP operating at the Politecnico of Turin.
Through multiparameter probes installed in the injection well
(P4) and into a downgradient piezometer (S2) it is possible to
control the movement of the thermal plume over time. The multitemporal
thermal logs in S2 highlighted the plume thermal
stratification in the aquifer and confirmed the hypothesis about
the prevailing advective transport component for heat flow.
CHARACTERIZATION OF THE AQUIFER
Downhole log data in the study area indicate the presence of
two lithologic zones with distinct hydraulic properties.
Unit 1 – (Middle Pleistocene – Holocene; from the surface to
47 m depth). Continental alluvial cover composed mainly of
coarse gravel and sandy sediments (locally cemented) derived
from alluvial fans aggraded by the Alpine rivers downstreaming
towards the east. The base of Unit 1 (erosional surface) dips
gently (0.5%) towards the north-east, overlaying Unit 2.
Unit 2 – (Early Pliocene – Middle Pleistocene; from 47 m
depth). Fossiliferous sandy–clayey layers with subordinate fine
gravely and coarse sandy marine layers or by quartz-micaceous
sands with no fossil evidences.
The GWHP plant interferes only with the Unit 1 by means of
_________________________
Evidences of advective heat transport related to an open-loop
groundwater heat pump plant (Turin, NW Italy)
(*) DITAG-Politecnico di Torino (Land, Environment and Geo-Engineering
Department), stefano.lorusso@polito.it
This work derives from the research program “Geothermal resources” and
has been partially funded by the Regione Piemonte.
STEFANO LO RUSSO (*) & GLENDA TADDIA (*)
179
an abstraction well (P2) and one injection well (P4). A
piezometer (S2) monitors the aquifer and is located downgradient
respect P4. The respective distances are: P2-P4 = 78 m, P2-S2 =
109 m, P4-S2 = 37 m.
First a step drawdown test was performed in P4 to evaluate
the hydraulic properties of the Unit 1. The test yielded a
transmissivity (T1) of 1.55x10 -2 m 2 /s. The hydraulic conductivity
(K1 = 5.53x10 -4 m/s) was calculated assuming and average
saturated thickness of 28 m. The effective porosity n was e
assumed 0.1. The measured undisturbed hydraulic gradient is
( dh dl ; i= 0.33%). The undisturbed average linear velocity vx
(1.58 m/d) (FETTER, 1999) is thus calculated as follows:
K dh
vx
= ⋅ (1)
n dl
e
Due to the gradient increase (up to 0.4%) during the injection
of warm water in the P4 in the GWHP plant functioning phase,
the actual average velocity slightly grows up to 1.91 m/d
according with Eq.1.
MONITORING RESULTS
The GWHP plant started its operation on May 14th, 2009 and
switch off on September, 20th 2009. Monitoring of hydraulic
levels, electrical conductivity EC and temperature T in P4 and S2
started in February 2009 and ended in November 2009. Analysis
of data clearly highlights three phases (Fig. 1). The phase 1
(February-May) corresponds to the period when the plant had not
yet started. The T in the P4 and S2 is constant around 15°C. The
relative increase in the T P4 (end of March) is connected to a
plant functioning test and is not revealed in the S2. The values of
EC are almost stationary. The phase 2 (May-September)
corresponds to the functioning period. The T and EC values
recorded in the P4 and S2 vary considerably. The oscillations in
the T P4 depends on the daily and weekly cycles of the heat
pump. The maximum recorded value reaches 28.7°C. The T
recorded in the S2 clearly identify the aquifer response to the
passage of the thermal plume with a significant delay (20 days)
respect the injection in the P4. The T increase rate in S2 is
approximately 1°C/day for the first 15 days, then slows down and
levels off to 0.5°C/day during the last part of the increasing
SESSIONE 7

SESSIONE 7
period. The highest T measured in S2 was 22°C (September,
17th). The oscillations in the injection temperature in the P4 are
smoothed but revealed also in the S2. The EC values tend to vary
out of phase with the temperature: when the T increases there is a
reduction of EC.
Fig. 1 – Monitoring data.
The third phase (September-November) corresponds to the
period after the plant closure. The parameter values gradually
tend to restore the baseline. The T P4 decreases sharply while the
T S2 reduces progressively losing about 1°C/week and reaching
the initial temperature (around 15°C) after two months.
THERMAL LOGS
The injection of the hot water in the P4 occurs by means of
discharge in the upper part of the water column in the well.
Therefore the thermal plume is originated by a point source
located on the top of the water table. In order to verify the
presence of a thermal stratification in the plume, one thermal log
has been conducted in the S2 during the phase 1 (natural
conditions). The result has been compared with those derived by
3 thermal logs conducetd during the phase 3. Results highlight the
aquifer thermal stratification (Fig. 2) and the progressive
restoring of the initial conditions several weeks after the plant
closure.
180
Fig. 2 – S2 thermal logs
CONCLUSIONS
Results seem to confirm the prevalence of heat advective
transport component respect the dispersive phenomena. This
hypothesis appears validated by the following evidences.
1) The delay (20 days) in the S2 temperature increase is
compatible with the calculated aquifer average linear velocity
(1,58-1,91 m/d) and the P4-S2 distance (37 m).
2) The thermal stratification in the aquifer is probably linked
to the different values of horizontal and vertical hydraulic
conductivity in the geological layers. Groundwater tend to flow
horizontally. Heat is carried along mainly with the flowing
groundwater.
3) The electrical conductivity appears to vary with an
oscillatory behaviour, out of phase with respect to temperature.
Uniquely difficult to explain, this phenomenon could be
considered as a marker of different geochemical characteristics in
the flowing water and thus a further confirmation of the
prevailing heat advective phenomena in the moving water.
REFERENCES
FETTER C.W. (1999) – Contaminant Hydrogeology. Prentice-
Hall, New-Jersey (USA), 500 pp.
LO RUSSO S. & CIVITA M.V. (2009) - Open-loop groundwater
heat pumps development for large buildings: A case study.
Geothermics 38(3), 335-345.
NAM Y., OOKA R. (2010) - Numerical simulation of ground heat
and water transfer for groundwater heat pump system based
on real-scale experiment. Energ. Buildings 42, 69–75.

Key words: Evaporites, relations between ground and surface
waters, sulphates.
Based on a sampling net of 103 points, the hydrogeochemical
characterization of the Aosta Plain unconfined aquifer has
showed that 80% of the more than 800 groundwaters sampled
from June 2006 to May 2009 has a Ca-HCO3 composition.
Instead, 8,4% of the samples shows sulphates concentrations
higher than carbonate and chlorides ones. This predominant
inversion is detected in a few numbers of wells, located in a
delimited area including the plain zones of tree municipalities. To
establish the hydrodynamic relations between surface waters and
groundwaters, the Dora Baltea River and the main torrents
flowing on the study area are sampled too. Along the Dora Baltea
course the sulphates concentration increases after the confluence
of the Gressan and the Clou-Neuf torrents, highlighting the
sulphates contribution from their drainage basins. The chemical
analysis on the two torrent samples confirms it. The Gressan
torrent influence, in particular, is conditioned by the water
derivation for agricultural uses. In winter time its water is free to
flow into Dora Baltea strongly increasing the amount of sulphates
of the river. On the contrary, in summer time the contribution is
not relevant.
Considering the absence of hazard sources connected to
human activities, it is reasonable to introduce the hypothesis of
natural occurrence of sulphates in ground and surface waters. The
sulphate natural sources in the area are represented by the
Triassic carbonated rocks connected to continental margins and
located between the ophiolits of the Zona Piemontese system.
Some slope collapse phenomena near Pila seem to be connected
to the presence of this kind of rocks and to their dissolution.
Bibliography data confirm high values of sulphates in sources
sampled.
Moreover, the graph showing the amount of SO4 2- versus the
amount of Ca 2+ puts on evidence that for the waters sampled in
_________________________
Natural occurrance of sulphates in ground and surface waters in
Aosta Plain (Italy)
(*) Politecnico di Torino, laurapia.lodi@polito.it
Lavoro eseguito con il contributo finanziario della Regione Autonoma
Valle d'Aosta
LAURA PIA LODI (*), MARINA DE MAIO (*) & ADRIANO FIORUCCI (*)
181
the area of Gressan, Charvensod and Pollein a sulphites oxidation
can be introduced to explain the sulphates input. The weathering
process could involve minerals such as pyrites.
Fig. 1 – the graph shows the amount of SO4 2- versus the amount of Ca 2+ in wells
(red), in Dora Baltea River (yellow) and in torrents (blue). A sulphate input and a
possible sulphite oxidation are introduced to explain the composition of the
waters sampled in Charvensod, Gressan and Pollein areas.
A 60 m deep drilling has been especially set up to describe the
stratigraphic sequence of the slope. It has confirmed the presence
of evaporites and of the dissolution phenomena.
To sum up, the hydrochemical study has confirmed a lateral
input of groundwater from the right slope, characterized by
evaporites rocks, to the plain aquifer and the weathering of
surface glacial deposits partially made by evaporites rocks,
present at the base of the slope.
SESSIONE 7

SESSIONE 7
Hydrochemistry and stable isotope for groundwater hydrodynamics
analysis in a karst aquifer (Alpi Apuane, Italy)
MATIA MENICHINI (*), BRUNELLA RACO (°), ELISSAVET DOTSIKA (°°), LUIGI MARINI (**) & MAURO ROSI (*)
Key words: Apuan Alps, geochemistry, karst, stable isotopes.
INTRODUCTION
Since 1960 isotopic techniques have been increasingly
applied to hydrological studies. Recently, LONGINELLI &SELMO
(2003) have drawn the isotopic map of Italy, based on the data of
77 different locations were composite monthly samples of
precipitations were taken over time intervals ranging from one to
seven years. Although the huge work done by LONGINELLI &
SELMO (2003) represents a giant step forward in stable isotope
geochemistry, its scale is not sufficient for most local studies,
requiring a more detailed knowledge of the isotopic composition
of rain waters in the area of interest, that is: (i) at different
elevations, to quantify the vertical isotopic gradient, and (ii) on
the distinct flanks of mountain chains, if present, to take into
account possible orographic effects. Generally, these data are
obtained by a series of rainfall stations that allow collection of
precipitations for at least a period of three years. Due to the large
fluctuations in the isotopic composition of rains, it is then
essential to compute the weighted mean of δD and δ 18 O values.
When isotopic data regarding rain falls are limited or not
available, is possible to use a different approach to the problem,
focussing on the isotopic characteristics of spring waters of rapid
flow and small circuit, with discharge elevations not very
different from the infiltration altitudes. In addition, it is advisable
to carry out repeated surveys, to take into account possible
seasonal isotopic variations reflecting the isotopic changes of the
rains recharging them. This methodology was used by MUSSI et
alii, (1998) in the Apuan Alps-Garfagnana area.
Recently, we applied this approach in the framework of a
chemical and isotopic study of the groundwaters circulating in the
_________________________
(*) Dipartimento di Scienze della Terra, Università di Pisa,
m.menichini@igg.cnr.it; rosi@dst.unipi.it
(**) DipTerRis., Università di Genova, lmarini@dipteris.unige.it
(°) Istituto di Geoscienze e Georisorse, CNR di Pisa, b.raco@igg.cnr.it
(°°) Institute of Material Science, NCSR "Demokritos" Attiki, Greece,
edotsika@ims.demokritos.gr
182
southern sector of the Apuan Alps, whose preliminary results are
presented in this communication.
Geological and hydrogeological setting
The investigated area is located in the northwestern corner of
Tuscany. The area has notable variations in altitude, with
maximum elevations of 1800 m asl. Rainfall is very high in the
mountains, where it locally reaches values of 3000 mm/a and
even >3200 mm/a on the ridge of the Apuan Alps. In contrast,
precipitation is typically close to 1000 mm/a in the plain near the
seacoast (BALDACCI et alii, 1993). Two main tectonic and
stratigraphic units are present in the study area: the metamorphic
sequence of the Apuan Alps and the corresponding members of
the Tuscan nappe. The Apuan Alps are a metamorphic core
complex outcropping in a tectonic window of the Northern
Apennines nappe cover. This was overthrusted during the Alpine-
Apennine orogeny, which began ~27 Ma and is also responsible
for widespread metamorphic effects in the underlying units
(CARMIGNANI & KLIGFIELD, 1990). The different lithologies,
within an articulated tectonic and orographic context, create a
wide variability in permeability, but on the whole shallow
hydrological circuits have a very rapid circulation. The Paleozoic
basement is characterised by low permeability, whereas high
permeability is typical of the carbonate formations, such as the
Marmi and Grezzoni of the Apuan Alps and the Calcare
Cavernoso and Massiccio of the Tuscan nappe, which are the
main regional water circulation systems.
SAMPLING AND CHEMICAL ANALYSIS
To obtain detailed information about groundwater flowpaths
and spring recharge areas two sampling surveys were carried out
during May and September 2009. In Fig. 1 the location of all the
sampled springs is shown. Water temperature, electrical
conductivity, pH, Eh, total alkalinity and ammonia concentration
were determined in the field. Moreover water samples for
chemical and isotopic analyses were collected. The concentration
of major components (Ca, Mg, Na, K, Cl, SO4, NO3 and SiO2),
selected trace components (B, F, Fe, Mn, Cr, Cu, Ni, Pb and Zn)
and some stable isotope ratios ( 2 H/ 1 H and 18 O/ 16 O of H2O and
13 12
C/ C of Total Dissolved Inorganic Carbon, TDIC) were
determined on all samples.

Fig. 1 – Schematic hydrogeological map of the study, in which permeability units are distinguished. The location and composition of sampled springs is also
shown.
DISCUSSION
Based on the Langelier-Ludwig diagram it is possible to
distinguish three main groups of water with distinctive
composition (Ca-HCO3, CaSO4 and NaCl) and samples with
intermediate characteristics produced through mixing. Ca-HCO3
waters proceed from shallow circuits hosted in fractured and
karstified carbonate rocks and alluvial aquifers; Ca-SO4 waters
are representative of relatively deep circuits in carbonateevaporite
formations, whereas low-conductivity Na-Cl waters are
slightly modified rain waters relatable to rapid flows and shallow
circulation. The plot of δD vs. δ 18 O values suggests that all the
collected waters are of meteoric origin, whereas the different
isotopic ratios mainly depending on the infiltration altitude. High
flow-rate springs related to karstic circuits were neglected,
whereas low-discharge springs (< 0.5 l/s) were selected to
calculate the mean isotopic vertical gradient of the study area,
which resulted to be -0.116‰/100 m. This figure is significantly
lower than that found by LONGINELLI & SELMO (2003) for
different Italian areas, confirming the need for a local calibration
of the isotope-altitude relation. TDIC and δ 13 CTDIC values were
used as chemical and isotopic tracers to evaluate the contribution
of different water components to spring discharge. The rationale
for this exercise is that in the unsaturated zone (UZ) and saturated
zone (SZ) water-rock interactions do not obey the same kinetics.
The mixing rate between water coming from UZ, characterised by
183
a short residence time, and water from the saturated zone SZ,
with a longer residence time, was therefore evaluated. As a
preliminary step to further geochemical modelling, speciation
calculations were performed by means PHREEQC to evaluate the
saturation state with respect to the minerals of interest. Reaction
path modelling of water-carbonate rock-gas interactions will be
used to investigate the release and fate of selected trace
constituents.
REFERENCES
BALDACCI F., CECCHINI S., LOPANE G. & RAGGI C., (1993) - Le
risorse idriche del bacino del fiume Serchio ed il loro
contributo all’alimentazione dei bacini idrografici adiacenti
- Mem. Soc. Geol. It., 49, 365-391.
CARMIGNANI L. & KLIGFIELD R. (1990) - Crustal extension in the
northern Apennines: the transition from compression to
extension in the Alpi Apuane core complex - Tectonics, 9, (6),
1275-1303.
LONGINELLI A. & SELMO E. (2003) - Isotopic composition of
precipitation in Italy: a first overall map -
J. of Hydrology, 270, (1-2), 7 5-88.
MUSSI M., LEONE G. & NARDI I. (1998) - Isotopic geochemistry
of natural water from the Apli Apuane- Garfagnana area,
northern Tuscany, Italy - Miner Petrogr. Acta , 41, 163-168.
SESSIONE 7

SESSIONE 7
Effects of deep saline CO2-rich waters in the shallow aquifers from
the Mazarrón-Gañuelas Tertiary basin (central-southern Spain)
BARBARA NISI (°)(*), ORLANDO VASELLI (*)(°), MARIA JOSÉ GIMENO (**), FRANCO TASSI (*)(°), PATRICIA ACERO (**),
ROBERT J. POREDA (***), JULIO A. RODRIGO-NAHARRO (°°), A. DELGADO HUERTAS (°°°) & LUIS PÉREZ DEL VILLAR (°°)
Key words: carbon and helium isotopes, CO2-rich waters, mixing
process, water and gas geochemistry.
INTRODUCTION
The study area (about 180 km 2 ), located in the Mazarrón-
Gañuelas Tertiary basin (Murcia) (central-southern Spain), is part
of the Alto Guadalentín Valley, which lies in the Betic
Cordilleras (SE Spain), pertaining the eastern sector of the
Alborán Domain. The ENE-WSW Betic Cordillera shapes a W-E
elongated orogenic belt corresponding to the western Alpine
orogenic belt in the Mediterranean area. The Guadalentín Valley
is one of the Late-Neogene to Quaternary sedimentary basins
developed along the set of NE–SW active strike-slip fault
systems of the Eastern Betic Shear Zone. During the Plio-
Pleistocene, compressive tectonics disjointed the Alborán
Domain into sub-basins and E-W and WSW-ENE large folds
were developed, likely representing the zone of crustal thinning
and magmatism. The rifting and accompanying crustal thinning
were part of the tectonics in the western Mediterranean and
related to the formation of the Rhine basin in Germany and both
the Rhone and Algero-Provençal basins in France (SANZ DE
GALDEANO, 1990). In the SE part of the Iberian Peninsula, the
Betic Cordilleras shows hydrothermal activity, which produced
CO2 enrichment in groundwater. For this reason in the eighties, in
_________________________
(°) Istituto di Geoscienze e Georisorse CNR, Pisa (Italy), b.nisi@igg.cnr.it.
(*) Dipartimento di Scienze della Terra, Firenze, vaselli.orlando@unifi.it;
franco.tassi@unifi.it.
(**) Departamento de Ciencias de la Tierra, Zaragoza (Spain),
mjgimeno@unizar.es, patricia.acero@unizar.es.
(***) Dept of Earth and Env. Sciences, Rochester (USA),
rporeda@ur.rochester.edu.
(°°) CIEMAT-Departamento de Medio Ambiente, Madrid (Spain),
julio.rodrigo@ciemat.es; l.pvillar@ciemat.es.
(°°°) Instituto Andaluz de Ciencias de la Tierra CSIC, Granada (Spain),
antodel@eez.csic.es.
This work is funded by MICINN (Spain) and FEDER Funds (UE) in the
framework of the PSE Project (PSE-120.000-2008-6) (Principal Researcher
PhD Del Villar).
184
the Alto Reventón, within the Mazarrón-Gañuelas basin, two
wells (El Saladillo and El Reventón) were drilled for geothermal
energy prospecting at the depth of 535 and 710 m, respectively.
The rocks constituting the main reliefs and its substratum
belong to the Nevado–Filábride Complex (Paleozoic schist and
quartzite as well as Permian to the Upper Triassic quartzite,
micaschist, metabasite and marble formations) and to the
Maláguide Complex (Permo-Triassic sandstone, quartzite, shale,
conglomerate and limestone units) (ALONSO-CHAVES., et aiil
2004).
These formations are overlied by Miocenic sediments (mainly
marls, sand- and limestones and conglomerates) and riodacite
rocks. Plio-Quaternary conglomerate, sandstone, silt and clay
rocks close the stratigraphic sequence. The aquifer of the Alto
Guadalentín is divided into 2 separated horizons: i) a shallow
reservoir within in the Plio-Quaternary rocks, forming the main
aquifer and ii) a deep reservoir within in the Nevado–Filábride
Complex, characterized by secondary permeability. Since 1960,
and especially in the last 20 years, cool-season agriculture has
strongly developed in this area. This has favored a sharp increase
in water demand. The increasing water consumption has resulted
in an overexploitation of the Alto Guadalentín detrital aquifer,
which, consequently, was strongly contaminated by a the deepseated
saline CO2-rich aquifer. This occurrence has forced the
local farmers to abandon the wells or to diluite the well water
with fresh water. In this framework a preliminary investigation on
about 20 waters and dissolved gases collected in the Mazarrón-
Gañuelas basin at different depth (>50 ÷ 300 m) was carried out
with the aim to i) geochemically and isotopically characterize the
effects of the deep-seated CO2-rich saline aquifer with the
shallower ones and ii) assess the geochemical processes deriving
by this mixing in terms of water quality.
RESULTS AND DISCUSSION
Temperature, pH and electrical conductivity of the well
waters were measured in the field during a survey carried out in
March 2010, whereas major and minor ion chemistry were
analyzed in the laboratory by using routine methods. The
dissolved gases were collected after withdrawing the well water
at surface with a bailer, whose lower end was connected via a
silicone tube to a 250 mL pre-evacuated vial that was filled with

the water for about 2/3 of its volume (TASSI et alii, 2008). The
dissolved gas composition and the δ 13 C-CO2 (V-PDB ‰) values
were determined according to VASELLI et alii (2006) and TASSI et
alii (2008). Groundwater temperatures are between 21.4 and 45.7
°C, electrical conductivity was in the range of 886-11,290 μS/cm,
and the pH values are between 6.30 and 8.99. The water
composition is characterized by 5 chemical facies: Na(K)-SO4
(32%), Na(K)-Cl (26%), Na(K)-HCO3 (16%), Ca-SO4 (16%) and
Ca(Mg)-HCO3 (10%) (Fig. 2). This variability is likely favored
by the depth of the fractures affecting the substratum, which
allows the rise of a deep-seated CO2-rich saline aquifer
represented by the two exploration wells: El Reventon and El
Saladillo. Carbon dioxide is the most abundant compound in the
dissolved gases, being the concentration of this gas >80 % by vol.
in >75% of collected samples.
Fig. 2 – Anion and cation ternary diagrams for the Mazarrón-Gañuelas
groundwaters (s.w: sea water)
The N2/O2 ratios, which are higher than those in the air (3.73),
with the exception of 3 samples likely affected by air during
sampling, suggest that O2 is promptly consumed in oxidative
process occurring underground. Accordingly, the O2/Ne
(

SESSIONE 7
Holocene stratigraphy of the south Venetian Plain:
new insight data and correlations
Key words: alluvial ridge, Holocene, palaeochannel, Venetian
Plain
The late Holocene distal tract of the Adige sedimentary
system is bounded to the north by the Brenta River megafan and
to the south by the Po sedimentary system (MURST, 1997;
FONTANA, et alii, 2008). This latter boundary is not well defined,
as branches of the Po River have occasionally intersected the
Adige alluvial plain and, vice versa, Adige channels have crossed
the Po Plain.
The study area is located within the belt where the Adige and
Po rivers have interfingered in the past. This alluvial plain is
characterized by a complex network of alluvial ridges formed by
the aggradation of sandy and silty channel deposits, natural levees
and minor proximal crevasse splays (VEGGIANI, 1972; PERETTO,
1986; MARCOLONGO, 1987; CASTIGLIONI, 2001; PIOVAN et alii
2010). The interdistributary depressions are generally silty-clay,
but frequently show evidence of accumulation of organic deposits
in extensive swamps or are occupied by dense networks of distal
crevasse channels and splays.
High-resolution sedimentological and geochronological data,
here presented, allow the description of major alluvial ridges. As
well, the correlation among stratigraphical elements is shown in a
number of cross-sections.
A stratigraphic marker is provided by a calcic horizon which
has been reached at average depth of 7 m in Cona and Conselve
cross-sections. It can be correlated with the “caranto” palaeosoil
of the Lagoon of Venice (GATTO &PREVIATELLO, 1974; MOZZI
et alii 2003), which formed during the sedimentary hiatus and
sub-aerial exposure of the alluvial plain between the end of the
Last Glacial Maximum and the post-glacial transgression. This
buried soil marks the top of the Late Pleistocene sequence in the
whole Venetian-Friulian Plain (FONTANA et alii, 2008).
Another important element for stratigraphic reconstruction is
a 1 m thick peat layer recognized in the whole study area at the
average depth of 5 m. Chronostratigraphic evidence indicates that
this major organic-rich sedimentary event in the fluvial series
may correlate with the marine maximum flooding surface.
___________________________________________
(*) Dipartimento di Geografia, Università di Padova, silvia.piovan@unipd.it
SILVIA PIOVAN (*) & PAOLO MOZZI (*)
186
The radiocarbon dating of the bottom of this peat layer is
4435±5306 cal BP at Cona and 3557±3699 cal BP at Conselve,
just ca. 1 m above the calcic palaeosoil; this points to condensed
alluvial sedimentation during the early Holocene. Other ages
from the bottom of this layer are 4570±5330 cal BP in Saline and
5595±5754 cal BP in Santa Margherita. The radiocarbon dating
at the top of the peat provided the ages of 3455±4094 cal BP in
Cona, 3201±3354 cal BP in Conselve, 4237±4979 cal BP in
Saline and 3158±3383 cal BP in Santa Margherita cross sections.
Radiocarbon datings evidence that the base of the peat layer is
progressively younger in more landward locations. Peat started to
form around 5700 cal BP in Santa Margherita, the place nearest
to the coastline, at 5300±4400 cal BP in Saline-Cona and 3600
cal BP in Conselve.
After peat deposition, a phase of major aggradation occurred
in the area, which resulted in the formation of alluvial ridges.
Radiocarbon datings on organic clays in natural levee deposits in
Conselve and Santa Margherita cross sections give the ages of
1950±2119 cal BP at 3.53 m depth and 1995±2157 cal BP at 2.5
m depth respectively. This evidences continuous aggradation
until Roman times, mainly related to the Adige alluvial system as
around 3000 BP the Po di Saline-Cona palaeochannel was not
anymore active (PIOVAN et alii, 2010).
REFERENCES
CASTIGLIONI G. B. (2001) - Response of the fluvial system to
environmental variations. In G. B. Castiglioni, and G. B.
Pellegrini (Eds.), Illustrative Notes of the Geomorphological
Map of Po Plain (Italy). Geog. Fis. Dinam. Quat. 4, 165-188.
GATTO P., & PREVIATELLO P. (1974) - Significato stratigrafico,
comportamento meccanico e distribuzione nella laguna di
Venezia di un’argilla sovraconsolidata nota come “caranto”.
C.N.R., Ist. Dinamica Grandi Masse, TR70, 1-45.
MARCOLONGO B. (1987) - Ricostruzione paleoidrografica
attraverso interpretazione di immagini telerilevate. In B.
Marcolongo (Eds.) - Paleoidrografia tardoquaternaria della
pianura veneta sudoccidentale e il suo significato in una
ricostruzione paleo climatica. C.N.R., Padova, 6-9.
MOZZI P., BINI C., BECATTINI R. & MARIOTTI LIPPI M. (2003) -
Stratigraphy, palaeopedology and palynology of Late

Pleistocene and Holocene deposits in the landward sector of
the Lagoon of Venice (Italy), in relation to the “caranto”
level. Il Quaternario, 16(1b), 193-210.
MURST, MINISTRY OF UNIVERSITY RESEARCH AND
TECHNOLOGY (1997) - Geomorphological Map of Po Plain.
MURST-S.El.Ca,3 sheet, scale 1:250000, Firenze.
PERETTO R. (1986) - Ambiente e strutture antropiche nell'antico
Polesine. In AA.VV. (Eds.) - L'antico Polesine.
Testimonianze archeologiche e paleoambientali. Antoniana
s.p.a., Padova, 21-100.
PIOVAN S., P. MOZZI & C. STEFANI (2010) - Bronze Age
palaeohydrography of the southern Venetian Plain.
Geoarchaeology, 25, (1), 6-35.
VEGGIANI A. (1972) - Il ramo del Po di Adria nella tarda Età del
Bronzo. Padusa, 8(3-4), 123-126.
187
SESSIONE 7

SESSIONE 7
Groundwater quality assessment of the Palermo Mts.
ANTONINO PISCIOTTA (*), ANTONIO CONTINO (**), GIOACCHINO CUSIMANO (**) & ROCCO FAVARA (*)
Key words: Groundwater quality, hydrogeochemistry,
hydrogeology, pollution.
The 20st century and the begin of the 21st are characterized
by important global climate changes, most of them phenomena
can be attributed to the emissions of greenhouse gases by human
activities (PATZ et alii, 2000; HAINES et alii, 2004; MCMICHAEL
et alii, 2004; EPSTEIN et alii, 2005). The rainfall reduction and
extermination are playing an important role on the degradation of
the water quality and availability.
The increased water demand and the bad management policy
have further damaged the fragile eco-system with waste and
pollution phenomena, deforestation and desertification processes.
Sicily, located in the Central Mediterranean, is an aridsemiarid
region, the groundwater resources are unequally
distributed in the island and greatly depending from its geological
setting.
The Carbonatic Mesozoic reliefs of the Palermo Mts.
(Western Sicily) were selected in order to investigate
groundwater contamination and spatial relationships among
groundwater quality, topography, geology, landuse and pollution
sources, because these karst aquifers are the main groundwater
resources used for human supply of Palermo, with about 700.000
inhabitants.
The hydrogeological framework of these tectonic unities,
stacked according to the ramp-flat geometries, shows
occasionally an hydraulic connection to the bordering tectonic
unities or to the sea. The groundwater flow is essentially
controlled by the principal tectonic lineations, by the overlapping
plains of the pelitic deposits and by several karstic forms
(CONTINO et alii, 1999; CALVI et alii, 2000).
Chemical analysis results indicate that groundwaters show
wide concentration ranges in major inorganic ions, reflecting
complex hydrochemical processes, dominated by the
calcium/magnesium (Ca 2+ /Mg 2+ ) and bicarbonate (HCO3 - ) ions.
The predominant water type of groundwater samples is the
calcium magnesium carbonate facies in the recharge area.
_________________________
(*) Istituto Nazionale di Geofisica e Vulcanologia, Sezione di Palermo,
f.pisciotta@pa.ingv.it
(**) Dipartimento di Geologia e Geodesia dell’Università di Palermo,
Palermo
Lavoro eseguito nell’ambito del progetto PRIN 2007 con il contributo
finanziario dell’Università di Palermo
188
Moreover the results explained the importance of cation
exchange, mineral weathering, and anthropogenic activities on
groundwater chemistry. It was indicated that cation exchange and
Cl-salt inputs are the major process controlling the water
chemistry on the flat zones. The irrigated agriculture and the
overexploitation of groundwater aquifers are leading to seawater
intrusion and severe deterioration of groundwater quality at
coastal areas, compromising also the main karst aquifers.
REFERENCES
PATZ J.A., MCGEEHIN M.A. & BERNARD S.M. (2000) - The
potential health impacts of climate variability and change for
the United States: executive summary of the report of the
health sector of the U.S. National Assessment. Environ Health
Perspect, 108, 367–76.
HAINES A. & PATZ J.A. (2004) - Health effects of climate change.
JAMA, 291, 99 –103.
MCMICHAEL A. & WOODRUFF R. (2004) - Climate change and
risk to health. BMJ, 329, 1416–1417.
EPSTEIN P.R. (2005) - Climate change and human health. N.
Engl. J. Med., 353, 1433–1436.
CONTINO A., CUSIMANO G. & FRIAS FORCADA A. (1999) - Nuovi
contributi alla conoscenza dell’assetto idrostrutturale dei
Monti di Palermo, Geologi di Sicilia, 2, 3.
CALVI F., CONTINO A., CUSIMANO G., DI CARA A., FRIAS
FORCADA A., HAUSER S. & PELLERITO S. (2000) -
Hydrostructures related to the Piana di Palermo aquifers and
their hydrogeochimical characteristics. In: R. Catalano & G.
Lo Cicero (Eds.), Sicily, a Natural Laboratory, in the
Mediterranean Area: Structures, Seas, Resources and
Hazards. Mem. Soc. Geol. It., 55, 473-481.

Surface water and groundwater monitoring and numerical modeling of
the southern sector of the Massaciuccoli Lake basin (Italy)
RUDY ROSSETTO (*), PAOLO BASILE (*), SILVIA CANNAVÒ (*), CHIARA PISTOCCHI (*), TIZIANA SABBATINI (*),
NICOLA SILVESTRI (**) & ENRICO BONARI (*)
Key words: Groundwater numerical modeling, MODFLOW-
2000, water management and planning
INTRODUCTION AND STUDY AREA SETTING
Investigating the natural system and evaluating a reliable
water budget are fundamental and mandatory steps prior to any
remedial action development that may impact the water cycle.
During a project aimed at defining mitigation schemes to the
eutrophication problem, a detailed quantitative surface- and
ground-water monitoring of the southern sector of the
Massaciuccoli Lake basin was performed. The acquired data were
then processed to build a numerical model of the first aquifer.
The Lake of Massaciuccoli (7 km 2 wide and 1.5/2 m deep)
and its palustrine nearby areas (about 13 km 2 wide) constitute a
residual coastal lacustrine and marshy area. Large part of the
basin has been reclaimed since 1930 by means of pumping
stations forcing water from the drained areas into the lake. In the
study domain two mechanically drained sub-catchments are
present: the Vecchiano and the Massaciuccoli Bonifica (Fig. 1).
An update review of the literature was performed and several
stratigraphical data analysed to provide a hydrostratigraphical
simplified conceptual model. The main hydrostratigraphic unit is
defined by sand deposits which constitute a 30 to 40 m thick
superficial aquifer on the west side, and pinching out on the
eastern margin while passing to sandy to clayey silt unit. These
two units are overlain by recent deposits (few meters thick)
showing a North-South trend moving from the alluvial fan
deposits (silty to clayey sands) of the Serchio River to peaty clay
and then peat. In terms of hydrological boundaries, the
investigated domain is bordered by carbonate to arenaceous
reliefs on the east and by a potentiometric high in the sandy
coastal shallow aquifer on the west. South and North of the
domain, the Serchio River and the Lake Massaciuccoli water
body respectively are hydraulically connected with the superficial
_________________________
(*) Land Lab - Scuola Superiore Sant’Anna, r.rossetto@sssup.it
(**) Dipartimento di Agronomia e Gestione dell'Agroecosistema –
Università degli Studi di Pisa, nsilve@agr.unipi.it
189
Fig. Fig. 1 – Study 1 – Study area area setting.
setting.
aquifer. Hydrogeochemical analysis confirmed the hypothesis on
the conceptual model (PISTOCCHI et alii, 2010).
SURFACE AND GROUNDWATER MONITORING AND
THE GROUNDWATER NUMERICAL MODEL
Surface water discharges of several drains were monitored
monthly to determine baseflow. Measurements were performed
by means of an acoustic digital current meter (OTT ADC; OTT
MESSTECHNIK GMBH, 2008) due to low flow velocities. At the
same time groundwater head in the superficial aquifer was
monitored during several campaign in order to get a deeper
insight on the boundary conditions. On the other hand, this kind
of activities showed that traditional monitoring in reclaimed land
area is not appropriate to represent the groundwater flow field,
because of the presence of several drains, which would require a
large number of monitoring wells. Anyway, they confirm that
recharge to the aquifer occurs also by means of lake seepage, and
from the sand dune aquifer to the Vecchiano Bonifica, while the
carbonate relief aquifer discharges into the Massaciuccoli
Bonifica.
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SESSIONE 7
Then, in order to define the groundwater flow field and to
estimate baseflow to the drainage ditches a groundwater
numerical model by means of the MODFLOW-2000 (HARBAUGH
et alii, 2000) code was implemented. A transient simulation,
using time steps ranging 2.5 to 5 days, was performed and
calibrated for the period July 2008- December 24 2009. The
conceptual model was translated into a numerical one by means
of a grid of 11.9x10.6 km, with 25x25 m cells, and three layers,
the first one representing superficial deposits while the second
and third one the sandy aquifer. Values for hydraulic
conductivities and storage were derived both from site-specific
tests, previous studies and literature data. In terms of boundary
conditions, the lake, the sea and the Serchio River were
represented using a time-variant Dirichlet condition, while
recharge due to meteoric precipitation and inflow from the
eastern carbonate aquifer were simulated by means of a
Neumann’s condition. The drainage network as well as the canals
used for irrigation purposes during the summer period were
reproduced using a Cauchy boundary. Initial conditions were
derived by a steady-state simulation calibrated on low-flow
conditions. Calibration was performed under steady and transient
state by means of automated and trial and error methods using
both heads and surface water flow measurements. Having several
different sets of measurements and two kind of variables to
perform calibration helped in constraining uncertain parameters
and therefore the solution of the flow field.
The implemented model allows to define the groundwater
flow field (Fig. 2), to estimate the baseflow volume drained by
the Vecchiano and Massaciuccoli Bonifica, and to quantify the
relative groundwater contribution to these sub-catchments by the
adjoining areas. These data, compared to the overall water budget
(PISTOCCHI et alii, 2010), shows that nearly 80% of the water
Fig. 2 – Simulated head in the investigated domain at the end of the spring period 2009.
190
raised by the pumping stations from the two Bonifica into the lake
is constituted by groundwater drained form the superficial
aquifer. Hence, the analysis of the transfer processes of pollutants
into the lake due to the reclaimed land shall take in account both
transport processes in the aquifer and physico-chemical processes
in the hyporheyc zone.
REFERENCES
HARBAUGH A.W., BANTA E.R., HILL M.C., & MCDONALD M.G.
(2000) - MODFLOW-2000, the U.S. Geological Survey
modular ground-water model -- User guide to modularization
concepts and the Ground-Water Flow Process. U.S.
Geological Survey Open-File Report 00-92, 121 pp.
OTT MESSTECHNIK GMBH (2008) – OTT Acoustic Digital Current
Meter.
[Accessed June 7 2010]
PISTOCCHI C., BANESCHI I., BASILE P., CANNAVÒ S., GUIDI M.,
RISALITI R., ROSSETTO R., SABBATINI T., SILVESTRI N., &
BONARI E. (2010) - Water quality and agricultural practices:
the case study of southern Massaciuccoli reclaimed land
(Tuscany, Italy). Geophysical Research Abstracts, Vol. 12,
EGU2010-12984-3, 2010 EGU General Assembly 2010.

Groundwater numerical modeling of the Bientina-Cerbaie aquifer
system as a tool for water management
Key words: Aquifer overexploitation, water budget mith,
groundwater numerical modeling
Aquifer mismanagement may have negative impacts on the
quali-quantitative status of the groundwater resource, especially
in areas where severe conflicts on water use among various
stakeholders take place. In this context, relying aquifer
exploitation just on the concept of equilibrium given in the
traditional water balance (sustainable development=rate of
natural recharge) may lead to aquifer overexploitation or even
groundwater mining (“the water budget myth”; Bredehoeft,
2002). This because the increased recharge and decreased
discharge induced by pumping introduces an error related to the
modification of the aquifer steady-state (Zhou, 2009).
Since groundwater numerical modeling allows the evaluation
of response dynamics of groundwater systems, it constitutes a
reliable methodology to rigorously cope with the abovementioned
topic. Groundwater numerical modeling using the
USGS code MODFLOW-2000 (HARBAUGH et alii, 2000) was
applied to the groundwater system of Bientina- Cerbaie (Tuscany,
Italy), where several well fields supply groundwater for drinkable
and industrial uses, within the LIFE06 ENV/IT/255 Action for
Systemic Aquifer Protection project (ASAP, 2010). The study
area presented during the last 10-20 years phenomena such as
continuous water-level drawdown, water quality deterioration,
subsidence; all these indicators may be related to aquifer
overexploitation (CUSTODIO, 2002). The main aim of the analysis
was:
- to evaluate the transient state of the aquifer system,
- to investigate the provenance of the recharge induced by
pumping,
- to estimate the impact of a reduction of pumping rates of the
drinking water wells on the aquifer head,
- and to test the use of the model as a groundwater
management tool.
The geometry and hydrostratigraphy of the aquifer system was
conceptualised analysing about 300 stratigraphic data and
hydrodynamic parameters available from pumping tests (Fig.2).
_________________________
RUDY ROSSETTO (*), PAOLO BASILE (*), OBERDAN CEI (**), NICOLA CEMPINI (**) & MICHELA SODINI (°)
(*) Land Lab - Scuola Superiore Sant’Anna, r.rossetto@sssup.it
(**) Acque Ingegneria Srl, o.cei@acqueingegneria.net
(°) H2O Ingegneria Srl, m.sodini@h2oingegneria.net
191
Several uncertainties arose already at this stage due to the
reliability and distribution of stratigraphic data coming from
different sources, and to the scarce number of hydrodynamic
parameters available compared to the study area vertical and
horizontal extension. Because of that, applying the principle of
parsimony (HILL &TIEDEMANN, 2007) and following previous
interpretation (AGUZZI et alii, 2006; BALDACCI et alii, 1994), the
hydrogeological system was simplified in three main
hydrostratigraphic units (HU):
- HU1: clayey to peaty fine deposits;
- HU2: Conglomerato del Serchio (gravel) and Unità delle
Cerbaie (mainly sands and gravel);
- HU3: silty to gravelly sediments Early Pleistocene to
(Early?) Middle-Upper Pliocene in age.
Fig. 1 – Study domain, stratigraphic data and hydrodynamic parameter
distribution.
No data were available about the depth at which a no-flow
boundary at the bottom of HU3 could be identified. Hence, the
model bottom was set at depth of -150 m a.m.s.l. This assumption
was tested to evaluate any impact of the bottom domain boundary
condition on the outflow due to pumping rates in the study
domain. At such a depth we estimated that it was not affected by
any inflow or outflow bottom boundary.
SESSIONE 7

SESSIONE 7
The conceptual model was translated into a numerical one by
means of a grid of 21.0x17.5km, with 100x100 m cells, refined to
25X25 m in the areas of well fields, and three layers, one for each
HU. Because of the lack of a regional sketch of the groundwater
flow field, assigning boundary conditions was not a
straightforward operation. Based on few field studies and on
hydrological considerations, we inferred the missing
hydrodynamic limits. Boundary conditions were then defined as
following:
- inflow from the Lucca aquifer from the northern limit;
- outflow to the Valdinievole-Fucecchio and the Valdarno
inferiore-Santa Croce aquifer system on the North/East-East side;
- inflow from the Monti Pisani; and
- outflow from the Bientina plain to the Arno River aquifer
system.
Transient simulations, using 15-day time steps, were
performed, calibrated and validated for the period January 2003-
September 2009, starting by a general steady-state simulation
referred to Autumn 2002 (Fig. 2). Results were obtained both for
head distribution in time and space during the investigated period
and the inflow and outflow from the analysed system. The model
solution well represents the groundwater flow field where it was
known by previous studies (ASAP, 2010) and it provides head
distribution for areas where the flow field is still unknown (i.e.
the Cerbaie domain). Results also show that a joint effort in
planning the water use is required in some part of the domain, as
i.e. in the Porcari area. A 10% reduction in pumping rates at the
Cerbaie well field produced a simulated head raise of about 0.3-
0.5 m. The latter was in good agreement with head values
monitored during the ASAP project, when a real pumping rate
reduction took place.
Anyway, because of all the above-mentioned uncertainties
within the conceptual model, quantitative flow evaluations may
only be considered as preliminary outcomes. Defining reliable
and validated boundary conditions, especially on the eastern side
of the domain, becomes a crucial step in estimating the water
budget or prior to perform predictive simulations, i.e. at Porcari
or Cerbaie well field area. Then, before setting any water
management scheme, based on unrealistic assumptions, it is
necessary that governing authorities finance field work (mainly in
terms of hydrostratigraphic and hydrodynamic investigations), as
large part of the domain is still not known by an hydrological
point of view.
This study shows that we require modeling tools, not only to
get quantitative estimates useful for water planning, but also to
guide further hydrological investigations and to get the maximum
from data obtained by direct or indirect field investigations.
Thanks to its capability, groundwater modelling should be an
ordinary methodology applied by the water authorities to plan
and to manage the water resource, especially in areas where
complex withdrawal schemes are present and a continuous new
equilibrium is reached.
192
Fig. 2 – Computed head in the steady state simulation related to a
general condition of the groundwater flow field in Autumn 2002.
REFERENCES
AGUZZI M., AMOROSI A., CASTORINA F., RICCI LUCCHI M., SARTI
G. & VAIANI S.C. (2006) - Stratigraphic architecture and
aquifer systems in the eastern Valdarno Basin, Tuscany.
GeoActa, 5, 2006, pp. 39-60.
ASAP (2009) - [WWW]
[Accessed June 7 2010].
BALDACCI F., BELLINI L. & RAGGI G. (1994) – Le risorse idriche
sotterranee della pianura di Pisa. Atti Soc. Tosc. Sci. Nat.,
Mem., Serie A, 101, pp.241-322.
BREDEHOEFT J. D. (2002) - The water budget mith revisited: why
hydrogeologist model. Ground Water 40 (4), 340-345.
CUSTODIO E. (2002) - Aquifer overexploitation: what does it
mean? Hydrogeol. J., 10, 254-277.
HARBAUGH A.W., BANTA E.R., HILL M.C., & MCDONALD M.G.
(2000) - MODFLOW-2000, the U.S. Geological Survey
modular ground-water model -- User guide to modularization
concepts and the Ground-Water Flow Process. U.S.
Geological Survey Open-File Report 00-92, 121 pp.
HILL M.C. & TIEDEMANN C.R. (2007) - Effective Groundwater
Model Calibration: With Analysis of Data, Sensitivities,
Predictions, and Uncertainty. John Wiley and Sons, Inc.,
Hoboken, New Jersey, US.
ZHOU Y. (2009) – A critical review of groundwater budget mith,
safe yield and sustainability. J. Hydrol., 370, 207-313.

SID&GRID: hydroinformatics system for the management of the
water resource
RUDY ROSSETTO (*), IACOPO BORSI (**), CLAUDIO SCHIFANI (°), ENRICO BONARI (*),
PAOLO MOGOROVICH (°) & MARIO PRIMICERIO (**)
Key words: DBMS and GIS, hydrological models, water
management and planning
The water resource is facing a growing pressure due to
anthropogenic impact and varying climate conditions. Hence, the
management of such a resource constitutes one of the most
important environmental problems to deal in the next years
(UNESCO, 2003). Recommendations have then been issued by
the European Environment Agency focusing on the need for the
implementation of new tools and technologies (EEA, 2009).
If we consider the Italian example, several authorities are
governing the water resource (Regione, Provincia, Autorità di
Bacino, etc.), while, usually, shared companies (private and
public) supply water and services to several stakeholders for
farming, industrial production, and drinking water. Nowadays,
the absence of shared tools that allow the integrated management
leads to a qualitative approach only, raising conflicts among
stakeholders difficult to manage for the various institutions.
Another problem is related to the traditional separation in the
quantitative analysis of the water cycle between surface- and
ground-water, which finally leads to: hard integration of the
analysis performed and unreliable assessment of water resource
availability and of the impacts due, i.e., to land cover
modification and climate change.
The research project SID&GRID, started April 2010, aims to
develop a Decision Support System (DSS) defined by a
framework based on open source and public domain solutions for
the planning and management of the water resource to be share
by the final users of the project partnership (e.g. river authorities
and water service companies). It will consist in watershed-scale
model able to simulate surface and subsurface flow in a threedimensional
domain. The SID&GRID solution will be able to
connect the DataBase Management System (DBMS), catchment
models and GIS interface by Open Source applications and
_________________________
(*) Land Lab - Scuola Superiore Sant'Anna, r.rossetto@sssup.it
(**) Dip. Mat. U. Dini - Università di Firenze, borsi@math.unifi.it
(°) Istituto ISTI - CNR, Claudio.Schifani@isti.cnr.it
The project is financed by the Regione Toscana under the POR-FSE 2010-
2013.
193
library, choosing the most effective and efficient integration
approach (Fig. 1).
The project will last 3 years and it is divided in 7
workpackages (WP). A technical review on the state of the art
about the integration between Geographic Information System
(GIS) and hydrological models constitutes the core activity of the
first WP and it is a present ongoing task. It involves the collection
and review of previous and current experiences from National
and International research program.
This study phase showed three macro approaches in national
and international experiences: the first is based on the OpenMI
standard implementation into GIS core system to exchange and
run OpenMI compliant model (OPEN MI ASSOCIATION, 2006); the
second approach provides an algorithms models integration into
GIS analysis tools (for example, 2D and 3D Ground Water
Model in GRASS GIS 6; Carrera-Hernandez and Gaskin, 2004);
the third and last approach is based on the USGS application
solution (MARKSTROM & KOCZOT, 2008) to customize, run,
calibrate and visualize models and their output data supported by
an Object User Interface (with a map window for spatial data).
During the first year, the DBMS (Data Base Management
System) and the GIS architecture will be designed and developed
to pre-process, process and output data model (spatial and no
spatial) visualization.
Physically based hydrological models rely on the solutions of
general conservation equations of fluid mechanics and associated
boundary conditions. They may fall into three categories based on
(BITTELLI et alii, 2010): domain simplification (i.e., SHE model;
BATHURST &CONNELL, 1992); simplified domain (i.e.: Sutra;
VOSS &PROVOST, 2002; Modflow; MCDONALD &HARBAUG,
1988); replacement of physical equations with simplified semiempirical
models (i.e.: SWAT; ARNOLD et alii, 1999). The
review of such models will allow the knowledge of the potential,
flexibility and weakness of each of them. Once this review will be
accomplished, our main goal will be the coupling of explicit
codes solving subsurface flow with those solving the surface
flow. Attention will be posed in the development and/or
improvement of the simulation of particular hydrological
processes (i.e. evapotranspiration processes).
Further WP include the development of the DBMS and GIS
architecture (WP 2), and of the following coupling hydrological
code (WP 3). The software Graphical User Interface (GUI) is due
SESSIONE 7

SESSIONE 7
Share and
Interoperability
Web
OGC
Interface
Pre-processing Simulation Post-processing
GIS Engine Hydro-code
SID&GRID
to be completed at the end of WP 4. The developed tool will be
tested starting by the second year of the project on the test site of
the Lucca plain hydrological system (WP 5). Finally,
dissemination activities (workshops, seminars, free lectures, as
well as an educational package) are the main task of WP 6. WP 7
is a huge workpackage of coordinating and administrative
actions. To be updated about such events, please, follow us at the
website: http://ut11.isti.cnr.it/SIDGRID/
REFERENCES
ARNOLD J.G., WILLIAMS J.R., SRINIVASAN R. & KING K.W.
(1999) - Soil and Water Assessment Tool. Model description.
Technical report Texas Agricultural Experiment Station,
USDA-ARS, Grassland, Soil and Water Research Laboratory-
Agricultural Research Service Blackland Research Center.
BATHURST J.C. & CONNELL P.E.O. (1992) - The system
hydrologique Européen. Hydrol. Process., 6, 265–77.
BITTELLI M., TOMEI F., PISTOCCHI A., FLURY M., BOLL J.,
BROOKS E.S. & ANTOLINI G. (2010) - Development and
testing of a physically based, three-dimensional model of
surface and subsurface hydrology. Adv. Wat. Resour., 33,
106–122.
CARRERA-HERNANDEZ J. J. & GASKIN J. S. (2004) - GMT: a
groundwater modelling tool for integrated water
management in FEM-MODFLOW and more. Proceedings of
the conference held at Karlovy Vary: Czech Republic.
Graphical User Interface of Control System
194
GeoDBMS
Cloud GeoDBMS
Fig. 1 - SID&GRID logic infrastructure.
Output
Data
Analyzer
EEA (2009) - Water resources across Europe – confronting
water scarcity and drought. EEA Report n. 2, 2009.
MARKSTROM S.L. & KOCZOT K.M. (2008) - User’s Manual for
the Object User Interface (OUI): An Environmental Resource
Modeling Framework. U.S. Geological Survey Open-File
Report 2008-1120, 39 p.
MCDONALD M.G. & HARBAUGH, A.W. (1988) - A modular threedimensional
finite-difference ground-water flow model: U.S.
Geological Survey Techniques of Water-Resources
Investigations, Book 6, Chap. A1, 586 pp.
OPEN MI ASSOCIATION (2006) - [WWW] [Accessed 18 May 2010]
UNESCO (2003) - The World Water development report water
for people, water for life. UNESCO publishing.
VOSS C.I. & PROVOST A.M. (2002) - Sutra, a model for saturated–
unsaturated variable density ground-water flow with energy or
solute transport. US Geological Survey, Open-file report 02-
4231, 250 pp.

Key words: Arno plain, channel stacking patterns, fluvial
architecture, late Holocene, palaeohydrography.
During the last decades in response to a worldwide rising
demand of clean drinking water, researches concerning
management and conservation of water resources in coastal and
alluvial plains have attracted an increasing attention. Since
aquifer systems structures and distribution reflect facies patterns
and sediment-bodies geometries, realistic models of groundwater
circulation must rely upon detailed subsurface stratigraphic
reconstructions.
The Quaternary successions buried beneath present coastal
plains are characterized by a vertical stacking pattern of
transgressive-regressive sequences falling within the
Milankovitch (100ka) band. Thus, fluvial deposits show different
depositional architectures and trends depending on their position
in the sedimentary cycle. Regionally extensive amalgamated
fluvial bodies (channel belts) formed during relatively low
accommodation phases, induced by regressive glacial conditions.
On the contrary, thinner and lenticular fluvial-channel sands
within predominant mud-prone floodplain deposits usually
occurred during the late stages of sea-level rise under interglacial
high-accommodation conditions (highstand systems tract).
Late Holocene fluvio-deltaic successions buried beneath
present alluvial and coastal plains represent a good basis for
better understand sand bodies distribution and geometries within
the highstand successions.
A large georeferenced subsurface database was used for the
first time to provide a high-resolution reconstruction of the fluvial
architectural elements recorded within the mid-late Holocene
succession of the Arno plain and evaluate impacts of climate and
human activity on river dynamics. Our attention was focused
around the city of Pisa, characterized by an elevated
concentration of subsurface data (cores and penetration tests) and
archeological sites spanning from the Iron Age to Late Medieval
times.
_________________________
Fluvial architecture of the Holocene succession
in the Arno coastal plain
VERONICA ROSSI (*), ALESSANDRO AMOROSI (*), GIOVANNI SARTI (**) & ROBERTA ROMAGNOLI (*)
(*) Dipartimento di Scienze Geologiche e Ambientali, Università di Bologna,
alessandro.amorosi@unibo.it, veronica.rossi4@unibo.it
(**) Dipartimento di Scienze della Terra, Università di Pisa, sarti@dst.unipi.it
195
Fluvial architectural elements composing the late highstand
succession are reconstructed through several stratigraphic
sections oriented transversal to the present Arno River course.
Above laterally extensive lagoonal deposits locally known as
“pancone”, the fluvio-deltaic succession is composed of isolated
to amalgamated channel sand bodies, of variable thickness,
within predominant flood-basin fine-grained deposits.
Using upper boundaries of channel bodies as stratigraphic
markers, four channel-belts (Units I-IV) are identified.
Chronology of fluvial deposits is established integrating absolute
radiocarbon ages with archaeological artifacts.
Units I and II, respectively dated to the pre-Roman and
Roman period, are composed of locally amalgamated, 2-8 mthick
channel bodies. Despite an overall aggradational trend,
Units I and II erode the underlying lagoonal deposits down to 4
m. Proximity of Pisa to the coast suggests a possible control
driven by small amplitude sea-level fall; however, a significant
contribution of climate and human activity can not be excluded.
More isolated and relatively thinner fluvial channel bodies
compose Units III and IV, deposited during the post-Roman
period.
In addition, stratigraphic data have been synthesized to
produce four palaeogeographical maps, reporting the main
modifications that affected the drainage network of the Arno
plain from late Neolithic-Eneolitic time to present. Between the
pre-Roman age and the XII century AD, the Arno plain shows a
complex palaeohydrographic system characterized by several
active palaeochannels (Units I-III). According to historical
sources and geomorphological maps, our data clearly document
the confluence between Arno and an old branch of Serchio River
(known as Auser) in correspondence of the city of Pisa. Only one
active fluvial course almost coinciding with the present Arno
River flows in the study area during the past 800 years (Unit IV),
due to the embankment of the Auser.
Our results confirm that fluvio-deltaic successions developed
under interglacial, high-accomodation conditions are
characterized by isolated to locally amalgamated channel-belt
units, with vertical dimension generally exceeding horizontal
extension. These deposits also hold the potential for developing
detailed reconstructions of deltaic and alluvial plain
palaeohydrography, including past hydrological events occurred
in response to climatic fluctuations and changes in land-use.
SESSIONE 7

SESSIONE 7
Detecting incised valleys in the subsurface of the Metaponto coastal
plain (Southern Italy)
LUISA SABATO (*), MARCELLO TROPEANO (*), MARCELLO BIANCA (**), ANTONIETTA CILUMBRIELLO (*), MARIA
ROSARIA GALLIPOLI (***), ANTONIO GRIPPA (*) & MARCO MUCCIARELLI (**)
Key words: Coastal plain, incised valley, Metaponto.
The stratigraphic architecture of the Metaponto coastal
plain subsurface (Southern Italy) was obtained from a data set
composed of twenty continuously cored boreholes and over 350
drills, 50-120 m deep. In particular, sedimentological,
biostratigraphical and chronostratigraphical analyses were
performed on four continuously cored boreholes.
Furthermore, some profiles, parallel and transversal to the
present-day shoreline, permitted correlations between the
stratigraphic logs obtained from all boreholes. Thanks to the
recognition of two discontinuity surfaces of regional extent, the
Metaponto buried succession may be subdivided into three
units.
The middle-upper(?) Pleistocene lower unit (“substratum”),
at least 60 m thick, is made up of silty and clayey-silty shelftransition
deposits passing upward and landward to sandy and
sandy-gravelly deltaic deposits.
The upper boundary of this lower unit is represented by a
very irregular surface which locally deepens up to 90 m and
this can be related to incised valleys formed during time spans
of subaerial exposition induced by relative fallings and lowstands
of the sea level.
These “paleovalleys”, mainly filled by estuarine deposits,
developed during two time spans comprising between the
Marine Isotope Stage 4 (MIS 4) and the Last Glacial Maximum
(LGM). The middle unit, called unit MP1 (Metaponto Plain 1),
lying on the substratum discontinuously, is late Pleistocene in
age and has a thickness of 15 m.
However, this thickness reaches 60 m when a paleovalley is
filled. The unit MP1 is composed in the first case of sandygravelly
fluvial and/or deltaic deposits; in the second case, the
paleovalley is filled with silty-sandy estuarine to deltaic
deposits. The upper unit, called unit MP2 (Metaponto Plain 2),
lying either on the unit MP1 or on the substratum, is late
Pleistocene and Holocene in age. The unit MP2 has a thickness
of 30 m. However, when
_________________________
(*) Dipartimento di Geologia e Geofisica, Università "Aldo Moro" di Bari
(**) Dipartimento di Strutture, Geotecnica, e Geologia Applicata,
Università della Basilicata, Potenza
(***) IMAA-CNR, Tito Scalo, Potenza
l.sabato@geo.uniba.it, m.tropeano@geo.uniba.it
196
paleovalleys are filled, thickness may reach 90 m. In the first
case the unit MP2 is made up of silty-clay offshore-transition
deposits passing upward to silty-sandy deltaic deposits and
finally to sandy fluvial deposits; in the second case, the
paleovalley fill, is composed of sandy-gravelly fluvial deposits
passing upward to silty and sandy estuarine deposits.
The non-invasive and low cost geophysical method of the
H/V spectral ratio (HVSR) of microtremors was tentatively
employed in order to draw the 3-D surface of unconformities
recognized through sedimentological analyses and 2-D
lithostratigraphic correlations. A 4-layers model of the
Metaponto coastal plain subsurface was used in the geophysical
investigation.
The inversion of the HVSR data has been performed using
the velocities of the shear waves calculated by some down-hole
tests, and the main geophysical unconformity was recorded
below the uppermost unit (MP2), corresponding to the topmost
two layers of the 4-layers model. A 3-D view of this main
geophysical unconformity shows a surface with the occurrence
of some deeper, narrow, and sinuous zones running roughly
perpendicularly to the present-day coastline and at depths of up
to 90 m below present-day sea-level.
These narrows likely correspond to paleovalleys developed
during the LGM and buried below the Metaponto coastal plain.
The satisfactory fit obtained by the comparison of geophysical
sections to geological ones highlights the reliability of the
HVSR method for reconstructing the geometry of buried
paleomorphologies characterized by an appreciable contrast of
seismic impedance between “substratum” and “cover”.

Fig. 1 – a) Schematic geological map of the Southern Italy; b) study area with location of wells used to realize the geological cross-section of Fig. 2. Trace of
sections in Figs 2 and 3 are also shown. .
Fig. 2 – Cross section parallel to the present-day shoreline showing the stratigraphic architecture of buried Metaponto coastal plain succession (see Fig. 1b for
location).
Fig. 3 – Comparison of geophysical with geological data along the same cross-section (see Fig. 1b for location).
197
SESSIONE 7

SESSIONE 7
Natural contamination by arsenic and other trace elements in
Northern Latium volcanic aquifers: a serious problem for drinking
water supply management
Key words: Arsenic, groundwater management, Latium
volcanic aquifers.
The district of Viterbo is located in the northern area of
Latium italian region and includes 61 municipalities for a
population of about 285.000 inhabitants and a total surface of
about 3700 Km2 (ISTAT, 2001).
The drinking water demand is predominantly met by
springs and wells both exploiting the confined aquifers of
volcanic substratum; this is a remarkable difference with the
other four Latium districts, fed prevalently by huge adduction
networks exploiting the pre-Appenninic carbonatic springs.
The geological sketch shows wide volcanic lithologies
outcrops, due to the intense activity of three main districts
Sabatino, Cimino-Vicano and Vulsino (BALDI et alii, 1974;
LOCARDI et alii, 1976; CAPELLI et alii, 2005) that involved the
region between the Pliocene and Pleistocene epochs.
From a hydrogeological point of view, the volcanic
formations host many aquifer horizons with some local
hydraulic connections among them and major
groundwater/surface water exchanges; the hydrographical
network is prevalently made by young streams with a radial
trend around the volcanic complexes hosting the two lakes of
Bolsena and Vico. The first one is the greatest volcanic lake in
Europe, having a surface of about 113 Km2 and a mean depth
of about 80 m with a top of 150 m.
Recent studies identified in the area 11 different
hydrogeological basins with total groundwater availability, in
term of direct rainfall recharge, of about 400 Mm3/a (CAPELLI
et alii, 2005).
Still today, a big groundwater amount is withdrawn, for
drinking purposes, by hundreds of water wells scattered on the
territory that symbolize the inheritance of the past management
system, ran on municipality’s base and actually converged on
_________________________
(*) Università di Roma “La Sapienza” Dipartimento di Idraulica, Trasporti e
Strade, Facoltà di Ingegneria,
giuseppe.sappa@uniroma1.it, matteo.rossi@uniroma1.it
Lavoro eseguito nell’ambito della Convenzione tra il DITS “Sapienza”
Università di Roma e la Regione Lazio
GIUSEPPE SAPPA (*) & MATTEO ROSSI (*)
198
the single responsibility of the Integrated System Service (SII)
Manger, according to the national Law 152/06.
As widely reported in literature (AIUPPA et alii, 2003;
CONIO et alii, 2004; VIVONA et alii, 2007), also in this case the
geochemical features of these volcanic groundwater show a not
negligible presence of important toxic elements like Fluorum,
Vanadium, Selenium and, above all, Arsenic.
Moreover, the Italian laws evolution in environmental field,
following the European Framework Directives, lead to an
actual situation where the most part of groundwater exploited
still today in the Viterbo district for drinking usage are now
outlawed due to the more strict limits for the above mentioned
elements concentrations.
For example, the old government ordinance Dpr 236/88
provided a threshold for the As concentration of 50 μg/l; in
2001, the new ordinance D.Lgs.31/2001, following the EU
Directive 98/83/CE concerning the drinking water quality
parameters, updated this threshold to 10 μg/l causing many
illegal situations on the whole country.
The possible derogations included in these ordinances are
going to expire in 2010 producing a critical situation for the
SII Managers which have to consider the treatment plants
installations or some other alternative water management
scenario.
In this context and in the framework of a Scientific
Agreement between the DITS “Sapienza” of Rome and the
Latium Region, with the purpose to better understand the
contamination state of the art and to define different strategies
for the drinking water supplying for the Viterbo district, a fine
study about the spatial distribution of the Arsenic and the other
elements on drinking sources have been started.
The present work shows the first results of data
elaborations related to the monitoring campaigns conducted in
2008-2009 on 160 wells and 80 springs in order to assess the
concentrations of As, F, V and Se; besides the spatial elements
distribution in groundwater sources and the statistical analysis
performed to study the different elements correlations, some
general suggestion to take this emergency situation in account
in a medium-long period are presented.

Fig. 1 – Drinking water monitoring network distribution.
REFERENCES
AIUPPA A., D’ALESSANDRO W., FEDERICO C., PALUMBO B. &
VALENZA M. (2003), The aquatic geochemistry of arsenic
in volcanic groundwater from southern Italy, Applied
Geochemistry 18, 1283-1296.
BALDI P., DECANDIA F.A., LAZZAROTTO A. & CALAMAI A.
(1974) – Studio geologico della copertura vulcanica
laziale nella zona dei laghi di Bolsena, Vico, Bracciano,
Mem. Soc. Geol. It., 13, 575-606.
CAPELLI G., MAZZA R. & GAZZETTI C. (2005) – Strumenti e
strategie per la tutela e l’uso compatibile della risorsa
idrica nel Lazio – Gli acquiferi vulcanici, Pitagora Ed.,
Bologna.
ISTAT (2001) – Censimento della popolazione.
LOCARDI E., LOMBARDI G., FUNICIELLO R. & PAROTTO M.
(1976), The main volcanic group of latium (Italy):
relations between structural evolution and petrogenesis.
Geol. Romana, 15, 279-300.
199
PREVITERA D. (2002) – La presenza di vanadio nelle acque
destinate al consumo umano dell’area catanese, Boll.
Chim. Igien., 53, 309-326.
VIVONA R., PREZIOSI E., MADÈ B. & GIULIANO G. (2007) -
Occurrence of minor toxic elements in volcanicsedimentary
aquifers: a case study in central Italy, Hydr.
Journ., 15(6), 1183-1196.
SESSIONE 7

SESSIONE 7
Key words: Aquifers, Arno coastal plain, Late Quaternary
stratigraphy, Tuscany.
INTRODUCTION
The increasing importance of water resources and aquifer
pollution are a priority in densely populated areas such as coastal
plains. The need for a better understanding of groundwater
circulation and transport processes in aquifers of modern alluvial
and coastal plains requires a very accurate reconstruction of their
subsurface sedimentary architecture. A realistic 3D representation
of the subsurface architecture needs a reliable chronostratigraphic
framework, where the relationships among lithofacies are forced
within a coherent depositional evolution in terms of space and
time. In this study we propose a reconstruction of the
multilayered aquifers from the subsurface of the subsiding Arno
coastal plain (Tuscany, Italy), characterized by the presence of
multiple incised valley-fill sequences, 3 to 7 km wide and up to
35 m thick, prevalently constituted by fine grained-deposits.
The study area comprises the southern sector of the Viareggio
Basin, which developed along the Tyrrhenian margin since Late
Tortonian, due to the opening of the Tyrrhenian Sea and the
counter-clockwise migration of the chain foredeep-foreland
system. The Viareggio Basin is bounded by the Versilia coastal
plain and Pisani Mountains to the north, and by Pisa and Leghorn
hills to the south.
METHODS
A multidisciplinary study (sedimentological, stratigraphic and
micropalaeontological) of 33 continuous cored boreholes,
integrated with a large georeferenced data base consisting of
about 2600 well logs, allows the detailed subsurface stratigraphy
reconstruction of the uppermost 100 m of Late Quaternary
_________________________
Reconstruction of multilayered aquifers from the Late Quternary
succession of the Arno coastal plain (Tuscany, Italy)
GIOVANNI SARTI (*), ALESSANDRO AMOROSI (**), VERONICA ROSSI (**) & SERENA GIACOMELLI (*)
(*) Dipartimento Scienze della Terra Università di Pisa, sarti@dst.unipi.it
(**) Dipartimento di Scienze Geologiche e Ambientali Università di Bologna,
alessandro.amorosi@unibo.it, veronica.rossi4@unibo.it
Lavoro eseguito nell’ambito del progetto di ricerca tra Università di Pisa e
Comune di Pisa per la realizzazione della carta del tetto delle argille
compressibili
200
Deposits (AGUZZI et alii, 2007, AMOROSI et alii, 2008). The
lateral and vertical facies relationships, within a
chronostratigraphic framework derived from 14 C isotope and
pollen profiles, yield the primary data for stratigraphic
correlation, and consequently the geometric reconstruction of the
aquifers.
RESULTS
An alternation of marine and alluvial deposits constitutes the
Arno valley subsurface. Two transgressive-regressive sequences
(T-R) are identified in the uppermost 100 m of the study area
(AGUZZI et alii, 2007). Sandy-to-muddy coastal shallow-marine
sediments deposited under rising and highstand sea-level
conditions (OIS 1 and 5e?) constitute the lower part of each T-R
sequence. Fine-to-coarse grained alluvial sediments, related to
falling and lowstand sea-level conditions (OIS 4–2 and 6,
respectively), developed between these two marine sequences.
During OIS 3-2 transition, a 35-40 m deep and 5-7 km wide
incised-valley was formed. Subsequently, the valley was filled by
transgressive muddy estuarine to coastal plain deposits since
about 12 kyr BP (AMOROSI et alii, 2008). The stratigraphic
architecture beneath the Lateglacial-Holocene valley bodies
evidences that multiple fluvial incision and subsequent valley
filling cycles occurred in response to late Quaternary sea-level
fluctuations. Below the LGM fluvial deposits, older estuarine
clays are recognized at depths ranging from 40 to 90 m. The
physical correlations with nearshore deposits imply that this
valley fill is related to an older phase of generalized fluvial
incision, probably occurred during OIS 6-5 transition. The
definition of a stratigraphic architecture model for the uppermost
100 m of the Pisa coastal plain subsurface enables the
identification of a sand-gravel multi-layered confined aquifer,
Late Pleistocene- Holocene in age, that becomes unconfined in its
shallow portion.
On the basis of facies characterization, late Quaternary
aquifers of fluvial origin (OIS 4–2 and 6) are characterized by a
lenticular geometry, wedging out away from the channel axis,
whereas aquifers within coastal-marine sands (OIS 1 and 5e)
constitute laterally extensive sedimentary bodies displaying a
landward-wedging geometry.
The high silt/clay ratio within the fine-grained overbank units
and shallow-marine muddy deposits that separate sand and gravel
channel bodies and transgressive and highstand sands

espectively, suggests that these sediments do not probably form
true aquicludes, and consequently that aquifers could be locally
interconnected.
The presence of two incised valley systems, 5 to 7 km wide,
cutting aquifers of fluvial origin, hinders their three-dimensional
representation and consequently the elaboration of realistic
models of groundwater circulation and transport. Since the valley
fill consists of about 35-40 m thick muddy estuarine deposits,
working as a permeability barrier, they constitute an interruption
of the continuity of water circulation.
A conceptual model for the Arno coastal plain multilayered
aquifers is here proposed taking into account all of the factors
described above. The predictive value of this model might be
validated by progressive data implementation by means of
additional continuous cored boreholes and geophysical analyses,
given the significance of the definition of a 3D palaeogeographic
reconstruction of the palaeovalleys. Thus, the model might be
confirmed, modified or improved in order to increase its value as
a basic tool to set up fluid circulation models progressively more
reliable, necessary to the proper management of water resources.
The likely allocyclic (subsidence and climatic) control on the
depositional architecture of the Pisa plain subsurface suggests
that other subsiding coastal plains might have experienced the
formation of multiple incised valleys. Consequently, this
occurrence might imply aquifer systems characterized by such
complex geometry, which is probably underestimated.
REFERENCES
AGUZZI,M.,AMOROSI,A.,COLALONGO, M.L., RICCI LUCCHI,M.,
ROSSI, V., SARTI, G. & VAIANI, S.C., (2007) - . Late
Quaternary climatic evolution of the Arno coastal plain
(Western Tuscany, Italy) from subsurface data. Sediment.
Geol. 211, 211–229.
AMOROSI A., SARTI G.,ROSSI V. & FONTANA V. (2008) –
Anatomy and sequence stratigraphy of the late Quaternary
Arno valley fill (Tuscany, Italy). In: A. Amorosi, B.U. Haq
and L. Sabato, (Eds)- Advances in Application of Sequence
Stratigraphy in Italy. Geoacta Spec. Pubb., 1, 55-66.
201
SESSIONE 7

SESSIONE 7
Mapping of a highly compressible lagoonal horizon in the Holocene
of the Arno coastal plain: implications for proper urban planning in
the city of Pisa
Key words: Highly compressibile lagoonal horizon, Holocene,
pancone, contouring maps, Pisa plain.
INTRODUCTION
Over the last decades an increasing interest toward the recent
evolution of present alluvial and coastal plains has been recorded,
due to their widespread socio-economic significance and intense
anthropogenic pressure. A proper land use, which includes the
monitoring of subsidence-related processes, water resource
management, archaeological and building conservation, must rely
upon a detailed reconstruction of the subsurface stratigraphic
architecture and characterization of sedimentary units with
peculiar geotechnical properties.
In the subsurface of the Arno coastal plain, around the city of
Pisa, a homogenous highly compressible clayey layer (known as
“pancone”) is recorded within the upper 20 meters of the
Holocene succession. This horizon with peculiar
sedimentological characteristics represents an important
geotechnical weak point, as evidenced by the structural failure of
the leaning tower, which made the city of Pisa famous all around
the world. Thus, detailed knowledge of its spatial distribution
patterns and geometry represents an issue of paramount
importance for a reliable Pisa urban planning.
METHODS
Detailed mapping and facies characterization of pancone was
carried out on the basis of a multidisciplinary approach, involving
the University of Pisa and Comune of Pisa. A large georeferenced
database consisting of about 2600 well logs was investigated,
with particular attention to 33 continuous cores which were
carefully described in terms of sedimentological characteristics
_________________________
GIOVANNI SARTI (*), ALESSANDRO AMOROSI (**), VERONICA ROSSI (**), SERENA GIACOMELLI (*), LETIZIA
FUSANI (*) & MIRIAM POTENZA (**)
(*) Dipartimento Scienze della Terra Università di Pisa, sarti@dst.unipi.it
(**) Dipartimento di Scienze Geologiche e Ambientali Università di Bologna,
alessandro.amorosi@unibo.it, veronica.rossi4@unibo.it
Lavoro eseguito nell’ambito del progetto di ricerca tra Università di Pisa e
Comune di Pisa per la realizzazione della carta del tetto delle argille
compressibili
202
(mean grain size, texture, colour, sedimentary structures and
accessory materials). The high-resolution stratigraphic analysis of
the subsurface database was integrated with microfossil
investigations performed on four reference cores, guaranteeing an
accurate facies characterization. The soft horizon under
examination was chronologically constrained on the basis of three
radiocarbon dating, integrated with pollen interpolated ages
(AMOROSI et alii, 2009) and a radiocarbon age published in
BENVENUTI et alii (2006).
RESULTS
The high compressibility of pancone facilitates its distinction
from normally or overconsolidated clays recorded at different
stratigraphic levels within the Holocene succession. This peculiar
geotechnical characteristic makes pancone a stratigraphic marker,
supporting its identification and mapping in the subsurface of the
Arno coastal plain.
As a whole, pancone marks the transition from the Arno valley
fill to the post-valley fill succession (AMOROSI et alii., 2008)
around 8,000-6,000 cal yr BP and is composed of two different
Fig. 1 – Homogeneous lagoonal clays with Cardium shells (P1 lithofacies)
from a working-face close to Pisa railroad station.
lithofacies (named P1 and P2). East of Pisa, this soft horizon
shows a total thickness of about 10 meters and consists of
predominant lagoonal clays (lithofacies P1, Fig.1) sandwiched

etween soft backswamp fine-grained deposits (lithofacies P2).
Around the city of Pisa and at more seaward locations, pancone
is almost entirely made up of 10-15m thick lagoonal clays
laterally passing to backswamp deposits, restricted to the
interfluvial areas of the Arno paleovalley.
Across the entire study area, the lower boundary of the marker
shows a rather linear trend; on the contrary, the upper boundary is
more irregular, recording a complex delta and alluvial plain
progradation. Aggradation of soft backswamp or normal
consolidated fine-grained deposits occurred alongside the
erosional superposition of distributary and fluvial channel sands
onto lithofacies P1, documenting localised deep channel
incisions. As a consequence, total thickness of pancone varies
and locally decreases up to 5 meters. particularly around the city
of Pisa, where a complex drainage network occurred since the
first stages of progradation. Therefore, the foundation stability
problems in the Arno coastal plain are influenced not only by the
presence of pancone and its total thickness, but also by the
complex relationships with the overlying deposits.
The realization of contouring maps regarding the spatial
distribution of bottom and top of pancone allows to identify the
most vulnerable areas and develop a proper urban planning. This
work testifies that the high-resolution stratigraphic analysis of
coastal plain areas could represent a useful tool for a good land
management.
REFERENCES
AMOROSI A., RICCI LUCCHI M., ROSSI V. & SARTI G. (2009) –
Climatic signature of millenial-scale parasequences from
Lateglacial-Holocene transgressive deposits of Arno valley
fill (Tuscany, Italy). Palaeogeogr. Palaeoclim. 273, 142-152.
AMOROSI A., SARTI G., ROSSI V. & FONTANA V. (2008) –
Anatomy and sequence stratigraphy of the late Quaternary
Arno valley fill (Tuscany, Italy). In: A. Amorosi, B.U. Haq
and L. Sabato, (Eds)- Advances in Application of Sequence
Stratigraphy in Italy. Geoacta Spec. Pubb., 1, 55-66.
BENVENUTI M., MARIOTTI-LIPPI M., PALLECCHI P. & SAGRI
M.E. (2006) – Late-Holocene catastrophic floods in the
terminal Arno River (Pisa, Central Itlay) from the story of a
Roman riverine harbour. Holocene, 16, 863-876:
203
SESSIONE 7

SESSIONE 7
Groundwater resource of the Geropotamos coastal aquifer
of Crete, Greece: hydrochemical and isotopic analysis
FRANCESCO SDAO (*), SERENA PARISI (*), DESPINA KALISPERI (**) & PANTELIS SOUPIOS (°)
Key words: Geropotamos basin, Greece, groundwater, sea water
intrusion, water quality
INTRODUCTION
In Greece, most of the groundwater recourses are generated
and widespread into deep carbonate and coastal aquifers, many of
which are subject to significant quality degradation processes
caused by salination of the water. This degradation quality, as
confirmed by SDAO et alii, 2009 is generated by sea water
intrusion processes. As reported from this study, the main coastal
aquifers of the Crete island, are affected by sea intrusion
processes, creating many problems with water supply of the
island. Particularly, with regard to the large amount of
groundwater flowing within the final part of the Geropotamos
River basin, is increasingly subject to significant quality
degradation processes generated both by the widespread human
activities and especially from the phenomena of water salination.
The study area is located on the northern part of Geropotamos
River basin, about 30 km eastern of Rethymnon city covering an
area of about 40 km 2 . The most recent census conducted in 2001
came from the General Secretariat of National Statistical Service
of Greece and shown that 4,665 people live in the investigated
area. Occupations of the local population are mainly agriculture,
stock farming. The farming consists mainly of sheep and goats.
Finally, tourism is an important part of the local economy, too.
GEOLOGICAL AND HYDROGEOLOGICAL FEATURES
The Geropotamos Basin represents an important aquifer
system of the northern coast of the Crete region. Most of the
groundwater flows in wide and deep carbonate aquifers. The
central and the western sectors are characterized mainly by
Miocene biogenic limestones, marls, clays and conglomerates.
The Tripolis and Ionion nappes of the bedrock, constituted by
clastic limestones and dolomites outcrop in the eastern part of the
area. Karst water-bearing carbonate rocks of Late Triassic to
_________________________
(*) University of Basilicata; francesco.sdao@unibas.it
(**) Institute for the Environment, Brunel University, UK
(°) Technological Educational Institute of Crete, Greece
204
Early Cretaceous age (Tripolis carbonates) overlying the Ionion
Nappes and Permian Plattenkalk Limestones. The south-western
sector consists of Neogene sediments while Quaternary deposits
cover the older nappes. The Phyllite-quartzite nappe is the oldest
rock of the study area lays on the northern part of Geropotamos
basin (KALISPERI et alii, 2008). The permeability of the aquifer
host rocks is very different from the coast sector to the central
part of the Geropotamos Basin. The main recharge of the study
aquifer is expected to come from a) the mountainous area at the
eastern and southern sectors which consists of highly permeable
formations and b) leakages from the dense river banks (network).
The principal hydrogeological complex is represents by the
carbonate karstic host rocks, of the Tripolis and Ionian nappes,
with high-medium permeability values.
SAMPLING AND METHODS
For the present study 22 public drills (9 drills for potable
water, and 13 used only for irrigation) and 2 springs have been
selected. For the physical parameters determination, as well as for
the major ions analysis three samplings took place during 2008.
The chemical analyses were performed at the Laboratory of
Environmental Chemistry and Biochemical Processes of TEI of
Crete (Branch of Chania). The stable isotopes analysis were
carried out at the National Institute of Oceanography and
Experimental Geophysics – OGS – Trieste, Italy. Some physicchemical
parameters (i.e., pH, Electrical Conductivity, Alkalinity,
Cl - , NO3 - ),were made upon sampling. Standard procedures for
water chemical were carried out as reported in “Standard
Methods for the examination of water and wastewater” (2005)
handbook. The stable isotopes concentration (δ 18 O, δD) were
measured using a common equilibration techniques with a
Finnigan MAT Delta-S mass spectrometer equipped with two
equilibration units for the online determination of hydrogen and
oxygen isotopic composition (MEYER et alii, 2000). The isotopic
concentration given, for the isotopic analysis of δ 18 O and δD,
performed in the present study, in units Standardization, is based
on international reference materials V-SMOW (Vienna Standard
Mean Ocean Water).
RESULTS AND DISCUSSION
The analyzed groundwater are characterized by temperature
values ranging from 18.1 to 22.9 °C. A slightly basic pH with
values ranging from 6.7 and 8.07 were found. High electrical

conductivity, ranging from 726 and 6470 μS/cm, were detected,
while the values of total dissolved solids (TDS) are between 270
and 3700 mg/l. The TDS values are strongly correlated with the
water conductivity (r 2 =0.99), indicating that the main dissolved
species are present as ions. The Geropotamos groundwaters
generally display a trend from a bicarbonate alkaline-earth, to
chloride-sodium compositions. These different chemical
compositions are related to simple water interaction with host
carbonate rocks and probably to the sea water intrusion
processes, respectively. From the geochemical data results that
groundwater flowing within the carbonate and karstic host rocks
of the Tripolis and Ionian nappes ranges in composition from
bicarbonate alkaline to bicarbonate alkaline-earth, with a
particular enrichment in SO4. The different hydrogeochemical
compositions were found closest to the coast area where the wells
are drilled within the Neogene and Quaternary deposits. These
groundwater as higher TDS values are Na-Cl sulphatebicarbonate
alkaline in composition. Their particular enrichment
in Na, Cl, and SO4 is likely due to a salty intrusion. During
seawater intrusion in coastal aquifers mainly two kinds of
hydrochemical processes take within the aquifer system: a)
mixing processes and b) ion exchange phenomena. In many cases
conventional hydrogeochemical studies are not sufficient to
characterize groundwater hydrodynamics or to detect recharge
areas and source areas of recharged water.
Very often the stable isotopic composition of water is
modified by processes like evaporation, evapotranspiration,
condensation, even sea water intrusion and hence the recharge
water in a particular environment will have a characteristic
signature that represents a natural tracer for water flow
movement. Specially, oxygen ( 18 O) and hydrogen ( 2 H) isotopes of
waters are ideal conservative tracers of water sources because
they are parts of the water molecule itself. The mean isotopic
concentration of the groundwaters collected during the present
study, ranged from -5.6‰ to -6.4 ‰ for δ 18 O and from -29 ‰ to -
35 ‰ for δD. All the samples fall between the EMMWL (GAT &
CARMI, 1971) and the GMWL (CRAIG, 1961). As reported by
CRAIG (1961) several processes can modify the isotopic
composition of the meteoric waters, leading to shifts of the
isotopic composition with respect to the GMWL. In the studied
case the original isotopic composition of the rain water is
modified by different factors. In fact, the groundwater isotopic
composition displayed a shift from the GMWL toward the
WMMWL due to the more arid vapor source, falling within the
variation range that is characteristic for the coastal areas at the
low altitudes. The δD values shows a slightly variation indicating
at least one meteoric water sources, probably the EMMWL.
Based on the oxygen and hydrogen isotope data and the general
water chemistry, it is proposed that the groundwaters enriched in
18 O and 2 H, flow within the regional carbonate and karst aquifers.
The water samples collected closest to the coast sector shown an
isotopic composition in 18 O and 2 H which is also enriched in
205
heavy isotopes, consists with a seawater dilution. The
investigated groundwaters should therefore be considered as a
mixture in various proportions of a sea-water component and a
freshwater component.
CONCLUSIONS
Groundwaters from Geropotamos River Basin exhibit a high
salinity caused by the dilution in various proportion of salty
intrusion. The distribution of the salinity is sometimes
independent from the coastal sector. The dilution effect is likely
to be related to the geometry of the fault network that guides the
freshwater from the mountain ranges surrounding the aquifer
system toward the Geropotamos River Basin itself. The seawater
component trapped in the investigated aquifer is probably mixed
with different fresh groundwaters from karst aquifer of the
Tripolis and Ionian nappes or the shallow aquifer of the basin
(Neogene sediments and Quaternary deposits covering the older
tectonic nappes). The evidence presented in the previous chapters
is best interpreted that the saline water is due to seawater
intrusion. This disproves previous works. Hence, during the
winter period precipitation (mainly snow and rain), falling mostly
in the mountains (Psiloritis Mountain and Talea Ori Mountain),
either runs off surficially (creating Geropotamos River), or soaks
into the ground as infiltration (replenishment of deep aquifer -
plattenkalk nappe, or phreatic aquifer - Neogene sediments).
During summer season, seawater intrudes inland through faults
with NE-SW direction, contaminating the fresh groundwaters
quality.
REFERENCES
CRAIG H., (1961) - Isotopic variation in meteoric waters.
Science, 133, 1702-1203.
GAT J.R. & CARMI H., (1971) - Evolution of the isotopic
composition of atmospheric waters in the Mediterranean Sea
area. J. Geophys. Res., 75, 3039–3040.
MEYER H., SCHÖNICKE L., HUBBERTEN W.H. & FRIDRICHSEN H.,
(2000) - Isotope studies of hydrogen and oxygen in ground
ice. –Experiences with the equilibration technique. Isotopes
Environ. Health Stud, 36, 133-149.
SDAO F., PARISI S., KALISPERI D., PASCALE S., SIMANTIRIS N.L.,
KERSHAW S., MONGELLI G., SOUPIOS P. & PATERNOSTER M.,
(2009) - Groundwater high salinity in Geropotamos basin
(Crete, Greece): sea water intrusion or Miocene Evaporites
water interaction processes? Supplement to Geochim.
Cosmochim. Ac., 73 (13).
SESSIONE 7

SESSIONE 7
Key words: Alluvial plain, Emilia Romagna, subsurface aquifers.
During the last twenty years studies and researches done by
Emilia-Romagna Region Geological Survey permitted to achieve
a detailed framework in geology and aquifers distribution in the
Emilia-Romagna alluvial plain.
Thanks to the availability of many subsurface geological maps
published at different scale in geological and hydrogeological
project, now we set up a detailed information on three
dimensional geometry of coarse and fine deposits in the
subsurface.
Other information, consisting in more than hundred geological
sections, are in http://www.regione.emiliaromagna.it/wcm/geologia/canali/cartografia/sito_cartografia/web
_gis_sezioni_geo.htm.
These knowledge in aquifers and aquitards or aquicludes
distribution permitted to support management of water resources
at a regional and local scale, starting from the implementation of
Water Framework Directive (2000/60 EC), and Groundwater
Directive (2006/118 EC).
Other application now in progress is related to drought and
salt intrusion in costal aquifers.
This topic was approached one years ago with drilling of
thirty piezometers along the Adriatic cost in both unconfined and
confined aquifers.
The survey of electrical conductivity was performed every
two months in every site and shows different evolution of salt
intrusion phenomena.
_________________________
(*) Geological Seismic and soil Survey Emilia-Romagna Region,
PSeveri@regione.emilia-romagna.it
Geology and subsurface aquifers in
Emilia-Romagna alluvial plain – Italy
PAOLO SEVERI (*)
206

Hydrogeological modelling for groundwater resources management: a case
study for the industrial water supply
Key words: Groundwater resources management,
hydrogeological model.
INTRODUCTION
The groundwater balance and the dynamics of the
groundwater flow depend on several factors such as the
hydrogeological properties of the rocks, the aquifer structure and
geometry, the recharge and the outflow motion, the interaction
with other surface or sub-surface water bodies.
The application of flow models in hydrogeology provides a
useful tool for the groundwater circulation analysis because they
allow all the hydrodynamic factors to be taken into account and
to better understand the direct effects of many external pressures
on the groundwater system.
Therefore the hydrogeological models are usually applied for
the groundwater resources evaluation and for its management
strategies definition.
In this study the three-dimensional, finite difference
MODFLOW model was applied in order to optimize the
groundwater pumping distribution in a well field for the water
supply of an industrial pole.
CONCEPTUAL MODEL AND NUMERICAL MODEL OF
THE AQUIFER
The study site is located in a central sector of the Tavoliere di
Puglia alluvial plain, closed to Foggia, which is characterized by
a wide alluvial heterogeneous aquifer (MAGGIORE &
PAGLIARULO, 2003). The aquifer is not too deep and the
groundwater level depth varies all over the area.
The aquifer texture is quite heterogeneous because it is
constituted by gravel, clay, sand and silt levels, even if they are
discontinuously present in the subsoil and the aquifer are
_________________________
(*) C.R.A. – Unità di Ricerca S.C.A., Bari, donato.sollitto@entecra.it
The present study was carried out during the PhD school in Geomorphology
and Environmental Dynamics (XVIII ciclo), in the Geologic and
Geophysics Department of the University of Bari.
DONATO SOLLITTO (*)
207
hydraulically connected to each other, so that the groundwater
system may be considered as a single layer aquifer.
The aquifer permeability is also heterogeneous, ranging from
10 -4 to 10 -5 m/s in the study site.
In some cases the aquifer may be over 30 m thick, closed to
Foggia, whereas some times the thickness is considerably reduced
due to the presence of clayey and silty layers (Fig.1).
The aquifer is confined by the presence of a silty layer on the
top, which strongly reduce the surface recharge of the aquifer in
the alluvial plain, so that it is fed by water infiltrating from the
upstream sectors of the hydrogeological basin (TADOLINI et alii,
1989).
The groundwater flow is mainly directed from NO to SE, with
the piezometric level ranging from about 150 m to 50 m a.s.l.,
with a 0,4-0,6 % piezometric gradient.
The flow model was set up as a single layer model of type 3,
that is with convertible flow conditions from confined to
unconfined. The hydrogeological system was discretized into
34594 cells with a base mesh of 100 m, passed to a 5 m mesh
closet to the pumping wells.
Dirichlet boundary conditions with variable potential head
were used on the upstream and downstream edge of the model
area, whereas no flow boundaries were located on the boundaries
parallel to the main groundwater flow direction. The well
package was also activated in 30 cells to simulate groundwater
pumping from the well field.
The groundwater model was calibrated in both steady state
and transient conditions, by using the weighted least squared
objective function, in order to minimize the differences between
the numerical solution and the real head values. The calibrated
model was then applied to simulate different groundwater
conditions in order to define the effect of the pumping wells on
the groundwater circulation.
RESULTS AND DISCUSSION
Some simulations were carried out by using the numerical
solution in the forward mode to simulate the natural conditions of
the aquifer, without water abstraction, and the actual perturbation
due to pumping conditions. These simulations have pointed out
the presence of a wide depression of the piezometric surface,
which falls about 5 m below the undisturbed conditions.
The application of the model in the inverse mode allowed to
SESSIONE 7

SESSIONE 7
Quota (m s.l.m .)
120
100
80
60
40
20
0
0 1000 2000
Distanza (m)
LEGENDA
better understand the reason of the greater productivity of some
wells with respect to the others, mainly due to their location along
the groundwater flow direction.
The critical conditions for the pumping wells were simulated
by fixing the water level in the wells as a critical target, below
which the productivity of the wells is compromised, and
calculating the maximum pumping rate for each wells.
The situations were simulated by assuming these critical
conditions in order to evaluate their effect on the total pumping
rate, such as to deepen the pumping structure in the wells, to
activate some wells instead of some other wells or to change their
locations.
Inverse modelling provided the best pumping rate distribution
by considering the actual settings of the well field, with a total
rate of 229 l/s was estimated.
Moreover, by simulating a different location for the pumping
wells the model has proved an increased well productivity by
placing the wells perpendicularly to the groundwater flow
direction. In this condition the total pumping rate increased to
over 250 l/s, allowing the industrial site to be satisfactory for
their water supply.
REFERENCES
MAGGIORE M. & PAGLIARULO P. (2004) – Circolazione idrica ed
equilibri idrogeologici negli acquiferi della Puglia. Atti del
convegno “Uso e tutela dei corpi idrici sotterranei pugliesi”,
allegato alla rivista Geologi e Territorio, 1, 13-35.
TADOLINI T., TULIPANO L. & ZANFRAMUNDO P. (1976) – La
falda idrica compresa tra Vico del Gargano e Ischitella
(Puglia): caratteristiche ed equilibrio idrologico. Giornale
del Genio Civile, 10.
P54
208
Foggia Stabilimento industriale
P71 P46 P22 P25 P27
Argille grigio - azzurre Argillesabbiose Argilleelimiargillosigialli Ghiaieesabbie
Fig. 1 – Geolithological cross-section of the aquifer.
P57

Key words: Aquifer recharge, GIS, hydrogeology, Python.
Water has become a resource to preserve and protect; we live
in a world by now polluted and deeply exploited where search for
water is like a gold quest in some global reality.
For years it has worked to definition and protection of water
resources available correctly. In this view from the eighties
through the model called "Hydrogeological inverse assessment”
(CIVITA, 1983) has tried to define and quantify the aquifers
recharge. The aquifer recharge is the starting point for a proper
definition of the available resources and delineation of protection
areas. The method over the years has evolved and improved
(CIVITA &DE MAIO, 2001). But in a context of global use this
method is implemented in Python script because it could run in a
GIS environment.
Python was born in Amsterdam in 1989, thanks to Guido van
Rossum, this is now one of the most popular open source
languages in the world. The introduction, in ESRI ArcGIS
environment, of the possibility of integrating Python, it has
opened the possibility of developing methodologies to implement
these long and difficult operation in short passages and it has
reduced the time of analysis and scenarios construction.
The inverse hydrogeological balance method (CIVITA et alii,
1995; CIVITA &DE MAIO, 2001) allows an estimation to be made
of the infiltration rate, in an area in which the hydrogeological
limits are known, by making use of a series of normally available
parameters of a climatic nature, such as rainfall and temperature,
and of a topographic nature, such as elevation height and slope
dip, together with parameters of a hydrogeological nature, such as
the ground and outcropping rock permeability characteristics.
Verification of the obtained results can usually be carried out
by comparing the estimation of the thus obtained specific active
recharge (input) with any available data of a bibliographic or
experimental nature relative to the water potentialities in the
study area (output).
_________________________
A GIS Tool to apply the hydrogeological inverse assessment
(*) Politecnico di Torino, enrico.suozzi@polito.it,
marina.demaio@polito.it, massimo.civita@polito.it
ENRICO SUOZZI (*), MARINA DE MAIO (*) & MASSIMO CIVITA (*)
209
Once the hydro structural limits of the area and the general
relations that are valid for the entire area of interest have been
established, the methodological approach foresees a subdivision
into square cells (square finite elements or EFQ) with sides that
must be defined on the basis of the extension of the area under
examination and of the density of the available data.
The use of GIS allows continuous data update, its display as
well as its internet consultation.
REFERENCES
CIVITA M. (1995) - Sul “rischio derivato” dall’impatto delle
catastrofi naturali. Atti XIII Giornata dell’Ambiente: “Eventi
Estremi: previsioni meteorologiche e Idrogeologia”, Atti dei
Convegni Lincei, 129, 131-136.
CIVITA M., COCOZZA T., FORTI P., PERNA G. & TURI B. (1983) -
Idrogeologia del bacino minerario dell'Iglesiente (Sardegna
Sud Occidentale). Mem. Ist. Ital. Speleol., 2, 2, 137 pp.
CIVITA M. & DE MAIO M. (2001) - Average ground water
recharge in carbonate aquifers a GIS processed numerical
model, 7 th conference on Limestone Hydrology and Fissured
Media. Besançon, 20-23 sept. 2001, 93-100.
SESSIONE 7

SESSIONE 7
Hydrodynamics, geochemistry, and vulnerability of springs fed by
highly karstified aquifers (Ligurian Alps – Piedmont, Italy)
Key words: hydro-chemistry, hydrodynamics, karstic springs,
vulnerability of aquifers.
In the Ligurian Alps sector, there is a series of springs fed by
highly karstified aquifers that are characterized by impressive
variations in their flow-rate and modest mineralization. Several
years ago, an applied hydro-geology team that works at the
Polytechnic University of Turin installed a series of automatic
detectors to record the water level, temperature, and electric
conductivity values.
The team has also collected samples, carried out chemical
analyses at the different points where the water emerges, and
conducted tests with artificial tracers that have allowed them to
characterize the springs being studied.
Among the many springs in the area, the functioning of two
main groups will be illustrated: the springs known as Sorgenti
delle Vene-Fuse, fed by the massif of Monte Mongioie, and the
Sorgenti del Pesio-Pesio 18 springs, fed by the massif of Monti
delle Carsene. The aquifers that feed these springs are
characterized by recharg areas composed of ample glacial-karstic
valley at heights ranging between 2000 m and 2600 m above sea
level; they lack covering but do have numerous micro-forms and
sinkholes that allow a very rapid infiltration of the water.
The rocky cluster, which is part of the succession of the
Brianzonese Ligure, is composed of an impermeable
metamorphic basal complex (meta-vulcanite and permo-triassic
quartzite) followed by a carbonatic succession with limestone,
dolomite limestone and Triassic dolomite, pure Jurassic
limestone, and cretaceous arenaceous limestone. The carbonate
succession is locally covered with low-permeability strips of
slates from the Cretaceous-Eocene.
The geometry and height of the impermeable basement
heavily affect the run-off of underground waters towards the
springs area where they emerge in the proximity of a defined
permeability limit that exists between the metamorphic basement
and the carbonatic cover. The carbonatic cluster presents a
limited fracturing and a highly developed karstification with
important collectors that can rapidly drain the penetration waters.
The underground circulation is characterized by a large
number of vertical cavities, temporarily active due to infiltration
_________________________
BARTOLOMEO VIGNA (*), ADRIANO FIORUCCI (*), CINZIA BANZATO (*) & MASSIMO VINCENZO CIVITA (*)
(*) Politecnico di Torino, Bartolomeo.vigna@polito.it
210
deposits, with differences in level exceeding 500-800 m. These
vertical cavities reach large sub-horizontal ducts where full-load
morphologies and vadose entrecement forms can be found. These
ducts act as important free surface run-off pathways that alternate
with short full-load sections in the absence of a traditional
saturated zone.
This flow network organization is typical of systems with a
“dominant main conduit” that heavily condition the waters’
hydro-dynamics and geochemistry. The variations in the flow-rate
of these emerging waters are very prominent and strongly
conditioned by the local meteorological regimen. After a
prolonged low-flow winter, characterized by minimum values that
range between 20 and 50 L/s, there is an important flood due to
the snowmelt that is characterized by daily oscillations of
hundreds of liters per second.
The minimum values are recorded between 12 pm and 1 pm
and the maximum values are seen between 9 pm and 10 pm.
Thus, there is a very fast response to the daily infiltration event.
Spring showers provide a further contribution to the increase in
the flow-rate that can reach thousands of liters per second.
The contribution provided by the snowmelt decreases slowly
until June-July, when daily variations in water flow can still be
recorded. In summer and autumn, flow rates reach quite low
values, lower than 50 L/s, but there are violent flood episodes
wherein the maximum yearly values are reached for brief, 1-2 h,
time periods (Vene spring 3500 L/s, Fuse spring 2900 L/s, Pesio
spring 3300 L/s, Pesio 18 spring 64 L/s).
The flood increases in water flow are very rapid and pass
from minimum to maximum values within 1-2 h. The decreases
are also rapid, with half-time values for maximum flow rate
ranging from 8 h to 10 h.
The trend of water flow for the Pesio 18 spring is totally
distinct, characterized by a much more constant yearly regimen
and a maximum flow-rate half time of 39 days.
The behavior of this spring, which is located below the Pesio
spring, depends only on the morphological characteristics of the
karstic reticulate in the area facing the emerging waters. Tests
performed with tracers and on the water chemistry have shown
that Pesio 18 belongs to the same karstic system as the Pesio
springs.
Continuous monitoring of water flow rate, electric
conductivity, and temperature shows a typical “prevailing
substitution” marked by a rapid decrease in mineralization values

during floods. Electric conductivity values are halved within a
few hours during a flood event, demonstrating that recent
penetration waters reach the spring in a very short time without
any swabbing phenomenon. As the flow peak decreases, the
electric conductivity gradually returns to ordinary values. Tracer
tests also reveal different water flow velocities, with values
exceeding 150 m/h during floods and values being reduced to 15
m/h during shortages.
Aquifers fed by the Pesio-Pesio 18 and Vene-Fuse springs are
extremely vulnerable to pollution, even though their vulneration
is quite limited given the almost complete absence of dangerous
centers in their supplying areas, with the exception of limited
pasture areas in summer, in correspondence of argillaceous schist
outcrops.
Applying the methodology of the half-time of the maximum
yearly flow rate with periods in the range of 8-10 h with water
flow velocity values obtained using tracers (maximum velocity >
150 m/h), the Vene-Fuse springs and Pesio springs yielded
similar results. The Pesio 18 spring is an exception: there, the
half time shows a medium degree of vulnerability, while the
tracer tests show that the time to reach the two springs are very
rapid, differing by only 3 h.
Also the hourly electric conductivity recordings, measured for
a few years at the Pesio and Pesio 18 springs, show similar values
and trends for the two emerging waters, highlighting a strong link
between the two springs. The inconsistency between the results
obtained was due only to the specific hydro-geologic situation in
the area facing the emerging point.
In conclusion, both hydro-dynamic and hydro-chemical
monitoring systems are important in studies of spring functioning
and vulnerability. In particular, we would like to point out the
need to reduce the acquisition time to approximately 1 h in order
to show in an extremely detailed way the behavior of a hydrogeological
system.
Furthermore, precise knowledge of a spring’s hydrogeological
regimen makes it possible to collect the most useful
water sampling data which need to be analyzed from the most
representative moments.
211
SESSIONE 7

SESSIONE 7
212

SESSIONE 8
Acquisizione - rappresentazione - gestione e
condivisione delle informazioni geologiche
CONVENERS
Mauro De Donatis (Università di Urbino)
Simone Sterlacchini (CNR Milano)
Fabrizio Piana (CNR Torino)
Andrea Taramelli (Servizio Geologico d'Italia Roma)
Serafino Angelini (LAC Firenze)
Maurizio Pignone (INGV Grottaminarda)
213
SESSIONE 8

SESSIONE 8
Gravitational instabilities on the continental slope off the Campania
Region: two case histories in the Naples and Salerno Bays
(Southern Tyrrhenian sea)
Key words: Continental slope, Naples Bay, Salerno Bay,
submarine slides.
INTRODUCTION
The study of the submarine gravity instabilities represents a
research line of increasing interest, mainly for its implications in
the monitoring of the deep and coastal environment in terms of
definition of geological and environmental hazard. In the last
years, the acquisition of large-scale morpho-bathymetric data on
the submerged portions of the volcanic edifices and, as a general
rule, in the oceanic basins and in the seas, has furnished
interesting data, giving a new impulse on the knowledge of the
structure and the geological evolution of the oceans. Relatively to
the Italian seas, the recent realization of Multibeam bathymetric
data in the Tyrrhenian sea (MARANI & GAMBERI, 2004) has
furnished important geological data both in the areas surrounding
both the emerged (Aeolian islands, Ischia, Ustica) and the
submerged volcanic edifices (Vavilov, Marsili, Palinuro and
submerged volcanoes of the Aeolian Arc), collecting new
morpho-bathymetric evidences on volcanic, tectonic and
gravitational processes at several scales.
The continental slopes and the submarine shelves surrounding
the Campania Region are characterized by different
morphologies, varying depending on the geologic setting of the
adjacent mainland which controls, together with other sectors, the
type of submarine gravity instabilities. The knowledge of these
geological processes is subordinated to the use of up-to-date
geophysical survey techniques, as the high resolution
multichannel and single-channel seismics, the Subbottom Chirp
profilers, the magnetic survey and the single-beam and
Multibeam bathymetry.
Geophysical and geological data have been collected to
improve the knowledge of submarine instabilities offshore the
Campania Region. This allowed for a discrimination between
“slow” submarine instabilities (creeping, slumping, deep
gravitational deformations) and “fast” submarine instabilities
_________________________
(*) Consiglio Nazionale delle Ricerche
gemma.aiello@iamc.cnr.it
GEMMA AIELLO (*) & ENNIO MARSELLA (*)
214
(debris avalanches, rock falls, roto-translational slidings).
The chronostratigraphic framework of the submarine
instability events is finalised to their correlation with the
triggering geological processes at a regional scale (seismicity,
volcanism, tectonic activity in correspondence to significant
faults).
On the submarine slopes off the Campania Region the
gravitational instabilities have been detected both on the
submerged flanks of the volcanic edifices (for example in the
Ischia island) and on relic volcanic morphologies (Nisida,
Pentapalummo and Miseno Banks in the Naples Bay; Forio and
Ischia Bank in the Ischia island). Moreover, they occur in
correspondence to steep and tectonically-comtrolled sedimentary
slopes (southern slope of the Sorrento Peninsula, slope of the
Gulf of Policastro) or in correspondence to slightly inclined
ramps, surrounding wide continental shelves (Salerno Bay). Some
case histories of submarine instabilities in the Naples and Salerno
Bays, located both in the Ischia island and on the continental
slope south-westward of the Salerno Valley are here discussed.
SUBMARINE GRAVITY INSTABILITIES: CASE
HISTORIES IN THE ISCHIA ISLAND AND IN THE
SALERNO VALLEY
The submerged sectors of the Ischia island are the site of
important submarine instability processes, having both
catastrophic instantaneous (debris avalanches) and continuous
character (accelerated erosion along submarine canyons or
channels, detritic fluxes along channels and creeping). The first
category of submarine instabilities includes the debris avalanches,
originated as a consequence of the volcano-tectonic uplift of the
Monte Epomeo block during the last 30 ky. The most important
debris avalanche is the “Ischia Debris Avalanche”, showing a
southern dispersal axis, with a transport of blocks up to 40-50
kilometers from the island (CHIOCCI & DE ALTERIIS, 2006). This
is suggested by the wide scar of the southern flank of the island
localised in correspondence to M.te Epomeo block, well evident
on the Multibeam bathymetry (AIELLO et alii, 2009a). The sketch
geomorphological map of fig. 1, constructed based on the
interpretation of Multibeam bathymetry, allows for the
localisation of the main hummocky facies, corresponding to
chaotic deposits, localised respectively northwards, westwards
and southwards of Ischia island. The main canyon’s heads are

localised in the north-western sector of Ischia (“Testata di Punta
Cornacchia”, “Canalone di Forio”). A strong erosion along
canyons and channels occurs mainly in the southern offshore,
characterized by steep slopes, incised in volcanic deposits. Main
channels engrave the slope between Punta Imperatore and Punta
S. Angelo, starting from the retreating shelf break, located at –
100 m of water depth. The NE-SW trending of the channels
indicates a possible structural control on their development. The
canyons offshore the Maronti Bay show a N-S trending and start
from wide scallops of the platform margin, more retreated than
those ones of the adjacent sectors of the southern offshore. The
chaotic deposits related to the debris avalanches do not seem
related to onshore slide scars (fig. 1).
Three important submarine slides along the northern sector of
the Salerno Bay have been identified and studied (fig. 2; AIELLO
et alii, 2009b). The northernmost one (A in fig. 2) develops at
water depths ranging from – 180 m and – 560 m, for a total
length of 3 kilometres. The second one (B in fig. 2) shows a
length of about 3.5 kilometres and covers an area located between
the water depths of – 200 m and – 440 m. The third slide (C in
fig. 2) shows a scar large about one kilometer, located at a water
depth of – 430 m and corresponds to slide deposits higher than 30
m at – 700 m of water depth. Two study examples of submarine
slides located on volcanic and sedimentary slopes have been here
presented. During a successive phase of the research project we
plan to construct regional and detailed geomorphological maps of
the main submarine instabilities, reporting both the
morphological lineaments related to instabilities and the
submarine instability areas, where significant slides of the sea
bottom have been detected (creeping, mud flow, slumping). The
rock falls, triggered by regressive erosion involving the coastal
sea cliffs, incised in carbonatic, volcanic and siliciclastic rocks,
together with seismic shocks and volcanic activity, will also be
accounted. e di crollo. It will be consequent the construction of
maps of geological hazard in coastal and deep sea environments,
furnishing useful indications for a correct planning of the marine
coastal environment.
Fig. 1: Sketch geomorphological map of the Ischia island.
215
Fig. 2: Shaded-relief detailed map, showing three important submarine slides
localised in the northern sector of the Salerno Gulf.
REFERENCES
AIELLO G. MARSELLA E. & PASSARO S. (2009a) - Submarine
instability processes on the continental slopes off the
Campania region (Southern Tyrrhenian sea, Italy): the case
history of Ischia island (Naples Bay). Boll. Geof. Teor. Appl.,
50 (2), 193-207.
AIELLO G., MARSELLA E., DI FIORE V. & D’ISANTO C. (2009b) –
Stratigraphic and structural styles of half-graben offshore
basins in Southern Italy: multichannel seismic and Multibeam
morpho-bathymetric evidences on the Salerno Valley
(Southern Campania continental margin, Italy). Quaderni di
Geofisica, 77, 1-34.
CHIOCCI F.L. & DE ALTERIIS G. (2006) – The Ischia Debris
Avalanche: first clear submarine evidence in the
Mediterranean of a volcanic island prehistorical collapse.
Terra Nova, 18, 202-209.
MARANI M. & GAMBERI F. (2004) – Distribution and nature of
submarine volcanic landforms in the Tyrrhenian sea: the arc
vs. the back-arc. Mem. Descr. Carta Geol. D’Italia, 64, 97-
108.
SESSIONE 8

SESSIONE 8
Geothematic data sharing of the Tuscany municipal plans by means
of Geographical Information Systems (GIS)
ITALO BELLU (*), ANDREA DEL SARTO (*), ILARIA NOEMI FRAU (*), MASSIMO PERNA (**), ALTAIR PIRRO (*),
FABIO PUGNAGHI (*) & ANDREA RINDINELLA (*)
Key words: Geothematic data, GIS, municipal plan.
The increasing availability of geographic information has
risen the need to develop storage and classification
methodologies in order to be able to share a massive amount of
data between public administrations. The management and
processing of geographic data are some main aspects for the
planning, safeguard and mitigation policies of environmental
critics.
The national and regional rules have well point out significant
aspects like the availability, delivery and interoperability of the
geographic data for an integrated and efficient territorial planning
(Legge Regionale Toscana 1/2005). These rules underline
Geographic Information Systems (GIS) help regional and local
administrations in the arrangement, implementation and control
of territorial planning means.
Currently local planning policies of Tuscany Region
regarding the municipal administrations are set out in strategic
development plans referred to as Piano Strutturale (PS) and
Regolamento Urbanistico (RU). These municipal plans are aimed
to set out requirements and strategies for the operative planning
in order to safeguard and value the natural resources (PS) and
manage the urban and land use changes (RU).
In the last years the Tuscany Region has undertaken a series
of activities oriented to favour the availability and access of
geothematic data to a number as large as possible of users in
order to carry out a unique web portal browsable and updatable
by means of geothematic databases. Currently these data are
spread through paper and digital archives stored in the regional,
provincial, communal and other local administration offices that
perform operational and territorial control activities. This article
will describe the activities relative to the scientific agreement
between the Consortium “Laboratorio di Monitoraggio e
_________________________
(*) Centro di GeoTecnologie (CGT), Università degli Studi di Siena,
rindinella@unisi.it
(**) Consorzio LaMMa, perna@lamma.rete.toscana.it
Lavoro eseguito nell’ambito dell’accordo di collaborazione scientifica
“Banche dati tematiche, geologiche e pedologiche e procedure informatiche
– operative” tra il CGT e il Consorzio LaMMa – Fondi PRAA Toscana
2007-2010
216
Modellistica ambientale per lo sviluppo sostenibile” (LaMMa)
and the Centre for GeoTecnologies (CGT) of Siena University
for the production of a digital archive of geothematic
investigations (geological, geotechnical, geophysical and
hydrogeological investigations), derived generally from the
environmental overview reported in the PS. In particular, this
work is interested in the geological-technical cartography and
geotechnical investigations reported in a PS.
The collection and implementation of all the available
municipal plans in a digital archive is aimed to: a) perform a local
scale overview of the geotechnical and hydrogeological
knowledge of the overall territory of the Tuscany Region, b) link
the geothematic data to the existed or in progress geological
databases and c) define a collaboration with the local authorities.
The main unit of the digital archive is a source project that is
represented in this work as a synthesis overview of the
investigations carried out for the geological-environmental
knowledge of the territory. The source project is identified by a
unique identification number according to the structure of other
existed geographic databases of the Tuscany Region (e.g.,
Database of Subsoil and Hydric Resources) and INSPIRE
(INfrastructure for SPatial InfoRmation in Europe) legislation
(Directive 2007/2/CE of the European Parliament and of the
Council of 14 March 2007).
The digital archive is based on a ESRI personal
geodatabase data model that represents a single-user relational
geographic database. This model exploits the DBMS Microsoft
Jet Engine® system used from Microsoft Access® for the
management of vector (feature class and feature dataset) and
raster data, tables, topological rules and relationships (association
between objects in a geodatabase) in order to be able for a object
of a class to access to the attributes of another object of a
different class (ATZENI et alii, 2009).
The main steps of the project will be described for the
implementation of geothematic data in the digital archive. In the
collection and acquisition step of the data for each source project
it has taken into account the positional and general information
(e.g., type and depth of investigation) of the geothematic
investigations. Currently the geotechnical parameters of the
investigations can be showed by digital attachments
geographically linked to geometric features. The position of a
feature (referred by a regional identification number) is showed

Fig. 1 – Overview of the municipal plans available in the geodatabase
categorized in: PS with geotechnical data, PS without geotechnical
data, Regolamento Urbanistico, other municipal plans, other
databases, not available.
Fig. 2 – Graph of the geotechnical investigations reported in the
geodatabase. CPT = Cone Penetration Test, SPT = Standard
Penetration Test, DP = dynamic penetration test, SDP = static/dynamic
penetration test, SA = geotechnical test, SO = geotechnical drilling
survey, PZ = wells, SG = spring, PL = laboratory tests, PD =
dilatometer Marchetti test, DH = down-hole and cross-hole geophysical
tests, PS = seismic profiling, SEV = geoelectric profiling survey, ai =
other investigations (permeability test, georadar, pumping test, etc.)
by geometric primitives (point and polyline) linked to
geothematic investigations and relative attachments by one-tomany
cardinality. Moreover, there is a direct relationship between
each source project and its investigations in order to select them
not only spatially but also by the project attributes. The technical
documentation of each source project is arranged by digital
217
attachments through many-to-one relationships.
The collection and implementation of the paper technical
documents (geothematic cartography and technical reports of the
in-situ tests, such as Cone Penetration Test CPT, geophysical
prospecting and geotechnical drilling survey, and laboratory
tests) require their conversion in digital format, classification and
denomination according to prefixed indices. The digital
conversion procedures have been performed by specific
requirements in order to homogenise the quality and size of the
attachments within the geodatabase addressed to web publication.
The Fig. 1 shows the spatial distribution of the municipalities
classified on the basis of type of plan providing geothematic data
(PS, RU, other municipal plans and databases). The figure points
out 187 municipal plans have geotechnical data attached within
PS, RU and other source projects, 73 plans do not provide these
data and the remaining 27 plans are not available because are in
progress or in evaluation phase by qualified control authorities.
The Fig. 2 shows the geotechnical investigations reported in
the geodatabase. The more numerous group consists of
penetration tests (35% of CPTs and about 27% of dynamic tests).
The remaining investigations are divided into stratigraphic logs
from geotechnical drilling surveys (about 20%), wells (7%) and
other geotechnical tests (6%), laboratory tests (about 3%) and
other in-situ geotechnical tests (e.g., dilatometer test, seismic
profiling, geoelectric profiling survey, permeability test, etc).
A disadvantage of the integration activities between different
data provided from archives with various format is their
inhomogeneous arrangement (stratigraphic logs, graph
elaborations, etc.), which limits their spatial correlation.
The development of procedures for the implementation in
suitable tables of all the stratigraphic logs and geotechnical
parameters could be advisable in order to enable the dynamic
management of geographical data by the GIS query tools. A
organic and efficient outline of the environmental setting may
help local authorities in the safeguard of the natural resources and
mitigation of risk due to potential landscape phenomena
(landslides, flooding, etc).
REFERENCES
ATZENI P.,CERI S., PARABOSCHI S. & TORLONE R. (2009) – Basi
di Dati: Modelli e linguaggi di interrogazione. McGraw-Hill
Italia, 462 pp.
DIRECTIVE 2007/2/CE of the European Parliament and of the
Council of March 14 th 2007 establishing an INfrastructure for
SPatial InfoRmation in the European Community (INSPIRE).
LEGGE REGIONALE TOSCANA January 3 rd 2005, n. 1 - Norme per
il governo del territorio, updated and coordinated text with
L.R. n. 41 of July 27 th 2007, B.U.R.T., 23 August 3 rd 2007.
SESSIONE 8

SESSIONE 8
Soil-landscape map of Arno River basin – a multidisciplinary
approach
NADIA BIANCONI (*), FILIPPO BONCIANI (*), IVAN CALLEGARI (*), LORENZO GARDIN (**), ROBERTO MAGGIORE (*),
RICCARDO MARI (°), FABRIZIO MERCATI (**), DOMENICO MORINI (°), ROBERTO MOSCARDINI (**),
JACOPO NEVINI (**) & ROBERTO NEVINI (**)
Key words: Geopedology, GIS, soil-landscape, soil-sampling.
INTRODUCTION
This project has as its purpose the creation of a soil-landscape
map of the Arno river basin (1:10,000 scale) through a soil
survey carried out in some sample areas of the basin.
Simultaneously seeks the creation of an information layer of
detail on regional soils, their physical and chemical
characteristics and their functional behavior, the content
information of the geological map at 1:10,000 scale and other
databases of detail found in regional Sit.
The project, also based on innovative methods of
environmental analysis, is a recurrence to increasing transaction
accuracy of identification of soil types present in the region, their
geographical location to an appropriate scale, their distribution in
the landscape and the variability of their spatial characteristics.
The project follows some priority criteria dictated by necessity
and urgency of solving regional problems in certain geographical
contexts.
Survey of soils, from analytical data collected from
processing, was made possible result after multiple themes for
different applications and information deepen knowledge on
specific topics.
The detection of the sample areas was based on photo
interpretation and subsequent implementation of some landscape
units, and is the realization of the notes on the characteristics
inherent to the landscape, then the lithology, morphology and
land use, the characteristics of soils of the landscape units
identified, by to be implemented and the implementation of a
geographic database of points of view, and archive photography.
The survey is complemented by the acquisition in the field of the
point coordinates measured with GPS system. The coordinate
_________________________
(*) Centro di Geotecnologie, callegari@unisi.it
(**) Soildata
(°) Regione Toscana, mauro.grassi@regione.toscana.it
218
system reference geographic database is the Gauss-Boaga
(Roma40). The database is only one feature class of points. Each
point collects the data of each drilled soil run. The database has
been compiled directly on netbooks during campaign activities.
The editor has requested the inclusion of surveys with related
data, placing directly on a topographic point in the reference
system Gauss-Boaga.
The structure and fields of the table follow those contained in
a standard table of soil sampling. Some fields in the table provide
precise values encoded as defined in the "Guida alla descrizione
dei suoli in campagna e alla definizione delle loro qualità" of the
Tuscany Region, other areas, however, provide for the insertion
of text or numeric fields unencrypted. Surveys activities started in
October and ended in May: 44 sample areas were detected within
about 1200 surface surveys on the landscape characteristics - soil
themselves.
The "Draft Charter of the Tuscany Region Soils", is
implemented with the Geological Survey of the region by a
working group composed by the Regione Toscana and the Centre
of Geotechnologies, University of Siena.

Key words: INSPIRE, Metadata, Portal, WMS.
The Geographic Portal of Geological Survey of Italy (ISPRA)
available at http://sgi.isprambiente.it/geoportal was planning
according to standard criteria of the INSPIRE directive. ArcIMS
services and at the same time WMS and WFS services had been
realized to satisfy the different clients.
For each database and web-services the metadata had been
wrote in agreement with the ISO 19115 (2005). The management
architecture of the portal allows it to encode the clients input and
output requests both in ArcXML and in GML language. The
web-applications and web-services had been realized for each
database owner of Land Protection and Georesources Department
concerning the geological map at the scale 1:50.000 (CARG
Project) and 1:100.000, the IFFI landslide inventory, the
investigations into the subsoil ex Law 464/84, the large-scale
geological map and all the raster format maps.
The portal initially published at the experimental stage,
through the development of a new graphical interface has now
reached the final version.
The WMS and WFS services including metadata will be redesigned.
The validity of the methodology and the applied standards
allow to look ahead to the growing developments.
In addition to this it must be borne in mind that the capacity of
the new geological standard language (GeoSciML), which is
already incorporated in the web-services deployed, will be allow
a better display and query of the geological data according to the
interoperability.
The characteristics of the geological data demand for the
cartographic mapping specific libraries of symbols not yet
available in a WMS service. This is an other aspect regards the
standards of the geological informations. Therefore at the
moment were carried out:
_________________________
The interoperability skill of the Portal of the
Geological Survey of Italy
VALENTINA CAMPO (*), LOREDANA BATTAGLINI (*), ROBERTA CARTA (**), CARLO CIPOLLONI (*),
MARIA PIA CONGI (*), DANIELA DELOGU (*), BENEDETTO PORFIDIA (°), MAURO ROMA (*),
RENATO VENTURA (*) & CLAUDIO ZONETTI (*)
(*) ISPRA Dip. Difesa del Suolo – SUO-MAP (Servizio
Cartografico), loredana.battaglini@isprambiente.it
(**) ISPRA Dip. Difesa del Suolo – SUO-CARG (Servizio CARG)
(°) ISPRA Dip. Difesa del Suolo – SUO-GFI (Servizio Geofisica)
219
- a library of geological symbols to be used for printing, with
a sketch of system colors and a library for displaying data on
video, which almost completely solves the problems of the
coverage point and area data (also directed) but that still
introduces problems for the linear data (solutions: ArcIMS
services from Arcmap projects or a specific SLD implementation
for WMS services);
- an update of “Guidelines for the supply of geological data”
in a short time will be published;
- the Geological Survey of Italy is officially involved in the
IUGS-CGI working group for the processing and experimentation
on the new GeoSciML language with the WMS/WFS services.
The collected metadata in catalogs are structured in a standard
(ISO 19135). The catalogs are a ‘common’ interface to locate,
view and query data and metadata services, web services and
other resources.
Then, while working in a growing sector of the environmental
knowledgement the focus is to collect the participation of other
subjects that contribute to the enrichment of the informative
content available, so as to be able to arrive to a real portal of
national interest especially in case of disaster management.
The geological survey’s data
More in detail the Portal allows access to the following data:
- CARG Project – Geological map of Italy at the scale
1:50.000, relatively sheets now available with their databases;
- IFFI Project - is the first uniform and updated inventory of
Italian landslides;
- Geological Map of Italy at the scale1:100.000;
- Archive investigations into the subsoil ex Law 464/84 -
deeper than 30 meters, generally applied to water research and /
or used for research in mining and hydrocarbons;
- Deep wells - which displays the deep drilling by the Ministry
of Economic Development made for oil exploration;
- Geophysics: Geophysical digital cartography - Gravimetric
Map of Italy at the scale 1:1.000.000 and 1: 250.000;
- ReNDiS Project - in which there are data of interventions for
mitigation of hydrogeological risk and resources involved in the
field of soil conservation;
- GeoIT 3D - 3D models for consultation of different areas of
Italian territory;
- ITHACA Project - which collects all available information
SESSIONE 8

SESSIONE 8
on the capable faults, with particular attention to the tectonic
processes that could cause natural hazards;
- Lithology Map of Italy - produced by reworking of the
geological map of Italy at the scale 1:100.000, assigning a
lithological class to a specific formation and other parameters
such as the genesis, the learning environment of the rock, the
structure of training structure and texture of the rock;
- OneGeology Project - for direct consultation through a
geographic data portal geological maps of the world;
- GeoSciML data model Project - on the compilation of a
language for transmitting information produced by the geological
community of Earth Sciences through display maps and data
services on the web;
- Sinkhole Project - database of the natural phenomena of
subsidence in plain areas of Italy;
- Other Data - including orography, hydrography,
administrative limits, roads, topography and settlements, etc,
available at Geological Survey.
REFERENCES
EN ISO 19115 (2005) - Geographic information – metadata.
ISO 19115:2003, http://www.iso.org.
220

A shared geodatabase for a landslides and Quaternary cover map of
the Regione Toscana
ALICE CIULLI (*), GIOVANNI MASSA (*), LAILA GIANNETTI (*),ELIA PASQUA (*), MASSIMO PERNA (**),
FRANCESCO MANETTI (**), NATALIE MARSICO (*), MARIA FILOMENA BASTONE (*), ENZO COCCA (*),
FEDERICO PANNACCI (*), SEBASTIANO SCACCHETTI (*) & ALTAIR PIRRO (*)
Key words: Geodatabase, geothematic data, GIS, landslide.
The increasing availability of geographic information has
risen the need to develop storage and classification
methodologies in order to be able to share a massive amount of
data between technicians, researchers and environmental
freelancer. The management and processing of geographic data
are some main aspects for the planning, safeguard and mitigation
policies of environmental critics, like flooding prediction and
relative emergency management via simulation systems, or
landslide hazard prevention with automated analysis on
geological and geomorphological data. Mainly for these type of
analysis you need to extract landslide and Quaternary cover data,
taken back on the geological and geomorpohological maps.
The national and regional rules have well point out significant
aspects like the availability, delivery and interoperability of the
geographic data for an integrated and efficient territorial planning
(Legge Regionale Toscana 1/2005). These rules underline
Geographic Information Systems (GIS) help regional and local
administrations, scientific community and the freelancers in the
arrangement, implementation and control of territorial planning
means.
Till now the Tuscany Region share the information needed for
the above mentioned activities through the official geological and
geomorphological regional cartography, published in her
geographical web site as raster or vector format, like 728
different tiles at the scale 1:10000. These data are derived from
different survey, in various periods, made by scientific
committees of disparate Tuscan Universities. Consequently the
data are really accurate but not so up to date and, in particular,
not so homogeneous long the whole Regional area. For these
reasons, there are some area that are too difficult to study,
because the data can come from different tiles that don’t
_________________________
(*) Centro di GeoTecnologie (CGT), Università degli Studi di Siena,
pirro@unisi.it
(**) Consorzio LaMMa, perna@lamma.rete.toscana.it
(***) CNR-IGG, masetti@igg.cnr.it
Lavoro eseguito nell’ambito dell’accordo di collaborazione scientifica
“Banche dati tematiche, geologiche e pedologiche e procedure informatiche
– operative” tra il CGT e il Consorzio LaMMa – Fondi PRAA Toscana
2007 2010
221
interfaces each other, with consequent problems to interpret them,
and maybe can have different age, so they don’t have the same
meaning.
In the last years the Tuscany Region has undertaken a series
of activities oriented to favour the availability and access of
geothematic data to a number as large as possible of users in
order to carry out a unique web portal browsable and updatable
by means of geothematic databases. This article will describe the
activities relative to the scientific agreement between the
Consortium “Laboratorio di Monitoraggio e Modellistica
ambientale per lo sviluppo sostenibile” (LaMMa) and the Centre
for GeoTecnologies (CGT) of Siena University for the production
of a geodatabase representing a unique, continuous and total
landslides and Quaternary cover dataset (Fig. 1).
Fig. 1 – Overview of landslide interpretation and acquisition on the database.
SESSIONE 8

SESSIONE 8
The collection and implementation of all the above data
perform a local scale overview of the slope instability hazard and
flooding scenario of the overall territory of the Tuscany Region,
through a homogeneous geothematic dataset consistent with the
geological database that it will be at the end of the year 2010.
The main unit of the geodatabase are two polygonal layers
representing all the Quaternary covers and landslides updated in a
previous stereo-photogrammetryc interpretation of a 2005 areal
photos.
The data model and its metadata are according to the structure
of other existed geographic databases of the Tuscany Region
(e.g., Database of Subsoil and Hydric Resources) and INSPIRE
(INfrastructure for SPatial InfoRmation in Europe) legislation
(DIRECTIVE 2007/2/CE of the European Parliament and of the
Council of 14 March 2007).
The digital data have stored in a ESRI SDE geodatabase
data model that represents a multi-user relational geographic
database, using the ArcGIS/ArcInfo editing powerfull and the
scalability of a Open Source Data Base Management System
(DBMS) like POSTGRESQL 8.3, to manage vector (feature class
on feature dataset) and raster data, tables, topological rules and
relationships (association between objects in a geodatabase) in
order to be able for a object or a class to access to the attribute of
another object of a different class. (ATZENI et alii, 2009).
A enterprise data acquisition architecture (Fig. 2), as that one
provided from ArcSDE (Spatial Database Engine) technology,
gives the chance to increase the map production, with a articulate
workflow based on a large number of user who can edit the same
dataset, the same area too and, furthermore, exactly on the same
feature.
GIS clients
Enterprise ArcSDE
Technology
DB2
Enterprise
Geodatabase
GIS data
9.3
Supported DBMS
platforms
DB2
Informix
Oracle
SQL
Server
Fig. 2 – Overview of the ArSDE architecture (with courtesy of ESRI).
This capability it’s really useful to edit a continuous and very
accurate dataset, with a lot of features, that must be edited,
updated and deleted simultaneously, without data and acquisition
fragmentation.
222
All these properties can warrant a unique data consistency,
excluding not needed redundancies, with a real productive
concentration of the data editing operation and managing,
through a series of tools dedicated to check every possible
violation by the users that overrides defined constraint. In fact
there are more scenarios in which the editors can work in this
kind of system but, in every case, the system detects always
potential conflicts (Fig. 3) that can amendable from the Database
Administrator (DBA), with a reconciliation with the stable state
Fig. 3 – A example of conflict detection during editing on ArcMap and
the solution choose interface (with courtesy of ESRI).
of the data.
The whole above consideration are relevant to explain the
particular carefulness to create a big and important geothematic
dataset thought to provide a relevant tool for the risks prevention
and environmental planning.
REFERENCES
POSTGRESQL GLOBAL DEVELOPMENT GROUP (1996-2010),
PostgreSQL Documentation, http://www.postgresql.org/.
ATZENI P., CERI S., PARABOSCHI S. & TORLONE R. (2009) – Basi
di Dati: Modelli e linguaggi di interrogazione. McGraw-Hill
Italia, 462 pp..
DIRECTIVE 2007/2/CE of the European Parliament and of the
Council of March 14 th 2007 establishing an INfrastructure for
SPatial InfoRmation in the European Community (INSPIRE).

Key words: Anti Atlas, cartography, geological maps, Morocco.
The Moroccan Ministry of Mine, Energy, Water &
Environment is carrying on a program of systematic coverage of
standard geological maps at the scales of 1:50,000 and 1:100,000
for the whole Country. The project is accomplished by internal
resources of the Ministry and by awarding contracts to external
organisations.
In 2003, a contract for five sheets at 1:50,000 scale was
awarded to a Group formed by two Italian firms, Geomap Srl and
S.EL.CA. Srl, both based in Florence, and by a Moroccan firm,
Geomine Sarl, based in Casablanca and Marrakech.
To carry out the project, the Group has availed itself of the
collaboration of Italian and Moroccan scientists and experts
belonging to research institutions, universities and specialized
firms, namely:
the Institute for Geosciences and Georesources (IGG) of the
Italian Council of Research (CNR), based in Pisa, Florence and
Turin,
the Department of Earth Sciences of the University of Pisa,
the Department of Earth Sciences of the University of Padua,
the LTS (Land Technology & Services) Srl of Treviso and
Padua,
the Faculty of Sciences Semlalia of the Cadi Ayyad
University of Marrakech,
the Faculty of Sciences of the Hassan II Aïn Chock University
of Casablanca.
Scientific coordinators of the project were: Giorgio Vittorio
Dal Piaz (University of Padua) and Abdelmajid El Boukhari
(University of Marrakech) for the precambrian basement,
Giovanni Musumeci (University of Pisa) and Kamal Taj-Eddine
(University of Marrakech) for the sedimentary covers.
The project has covered all the phases for the realisation of
the five geological maps, from the field survey and remote
sensing interpretation, the laboratory analyses, the preparation of
the topographic base maps, the organisation of all data into a data
bank, to the final editing and offset printing of the five sheets and
of the explanatory notices.
The five sheets of the project are located in the north-eastern
_________________________
Geological mapping in Morocco – A contribution from Italy
(*) Geomap Srl – Firenze, dainelli@geomapsrl.it
(**) S.EL.CA. Srl – Firenze, segreteria@selca-cartografie.it
PIETRO DAINELLI (*) & AUGUSTO PERSICO (**)
223
part of the Anti Atlas, across the north-eastern tip of the Jebel
Saghro and the south-western half of the Jebel Ougnat, the Anti
Atlas representing a part of the deformed northern margin of the
western African craton. The northern part of the area involves
also part of the mesozoic-cenozoic domain (alpine) of the High
Atlas.
The oldest Saghro basement outcrops in the window of
Imiter-Boumalne and is characterized by two complexes of the
middle Neoproterozoic or Cryogenian : i) the sandy-pelitic
metasediments, metamorphosed and folded at a regional scale
during the panafrican orogeny ; ii) the calc-alkaline intrusive
bodies at low metamorphism. This basement is unconformably
covered by thick volcanic and volcano-clastic formations (Group
of Ouarzazate) and cut by subvolcanic and intrusive bodies
which, non metamorphosed nor folded, can be related to the
upper Neoproterozoic or Ediacaran. The upper neoproterozoic
magmatism forms a post collisional sequence characterized by
high K calc-alkaline content. The Saghro-Ougnat Precambrian is
cut by a system of faults, frequently mineralized, and by dykes of
basalt, andesite and rhyolite.
The northwestern part of the precambrian basement includes
the large underground and open-air mine of Imiter, a
hydrothermal deposit at Ag-Hg related to an E-W fault zone and
to the emplacement of rhyolitic bodies of uppermost
neoproterozoic age.
In the north-eastern part, the substratum is made out of
volcanic formations of upper neoproterozoic age, in which two
different complexes have been distinguished : the Ougnat
rhyolitic complex, belonging to the middle NP3 and which has by
far the largest outcrops, and the Ougnat pyroclastic complex
(upper NP3), much more limited.
The Paleozoic consists of sedimentary sequences ranging in
age from Lower Cambrian to Carboniferous (Visean). Its basis
unconformably rests on a rough paleomorphology developed on
the precambrian basement.
The sedimentary and tectonic analysis indicates a sedimentary
context of a silico-clastic passive margin, controlled
predominantly by eustatic changes, and by local tectonic
movements (extensive). This double control is at the origin of
several local stratigraphic hiatuses (lower Cambrian, Siluro-
Devonian, upper Carboniferous), or regional (upper
Cambrian/Tremadocian, upper Ashgillian), and of a sequential
stacking, often of the third order. The tectonic control is due to a
system of faults, probably inherited from the Proterozoic,
organized in a main network trending ENE-WSW to E-W, a
secondary system NE-SW to NNE-SSW, and a minor one NW-
SESSIONE 8

SESSIONE 8
SE. The extensive block tectonics gives place, from the upper
Devonian, to a strong displacement of this northern margin of the
paleozoic platform. After the upper Visean, the sequence is
involved in a regime of polyphasic hercynian tectonics, in which
the major phase causes the inversion of the pre existing paleozoic
faults and some south-verging detachments, but without large
displacement.
The meso-cenozoic sequence is made of marine and
continental sediments which indicate well defined
paleogeographic and structural environments. They outcrop in the
northern part of the project area, along the northern margin of the
Anti Atlas. The lower part of the sequence, jurassic in age,
carbonatic and deposited in a marine environment, represents the
filling of basins formed in the “Atlasic“ rifting phase, while the
upper part, Cretaceous to Pliocene in age, represents both the
cover of the High Atlas and the filling of the Ouarzazate basin.
A hiatus separates the jurassic from the cretaceous deposition,
which starts in the Cenomanian with a continental sequence
extending in the turonian ocean. In the upper Cretaceous the
sequence indicates syntectonic characters and corresponds to an
alternation of continental and marine platform formations
deposited at variable depths. The upper paleocene to middle
eocene sediments, which unconformably lie on the middle-upper
cretaceous continental-marine sequence, are characterized, in the
majority, by coastal marine sediments. In the upper Eocene, the
sediments are predominantly continental.
At present, due to the alpine orogeny, the Ouarzazate basin
rests at the front of the High Atlas, which limits and partially
overthrusts it at its northern edge. The cretaceous to quaternary
formations that fill it towards the South, lie unconformably on
paleozoic and precambrian rocks of the Anti-Atlas.
224

SESSIONE 9
Il contributo del progetto CARG alla conoscenza della
geologia dell'Italia - Cartografia geologica
CONVENERS
Raffaele Pignone (Regione Emilia-Romagna)
Nicola Perilli (Università di Pisa)
Guido Giordano (Università di Roma TRE)
225
SESSIONE 9

SESSIONE 9
Key words: CARG, Coltre della Val Marecchia, foredeep,
Miocene-Pliocene.
INTRODUCTION
The biostratigraphic researches, carried out mainly in CARG
project, have been focused on the analyses of the calcareous
nannoplankton and planktonic foraminifera assemblages retrieved
in the sediments of central and southern Apennine chain. These
studies were performed to provide the biostratigraphic constrains
of the cinematic evolution of chain and to identify new and more
useful bio-events for the Mediterranean area.
BIOSTRATIGRAPHIC SCHEMES AND USEFUL
BIOEVENTS
Because of the characteristics of the sediments analyzed, often
poor and affected by intense frequent reworking,
preparation of nannofossils slides was carried out by
centrifugation (AMORE et alii, 1988: BOWN, 1999; DE CAPOA et
alii, 2003; AMORE et alii, 2005) is generally preferred to use the
events of FO (First Occurrence) and not those of LO (Last
Occurrence). Regarding planktonic foraminifera the
biostratigraphic scheme frequently used for Neogene
Mediterranean is that proposed by IACCARINO et alii (2007),
which is a summary of the various schemes proposed by several
authors in recent years, including SPROVIERI et alii (2002),
HILGEN et alii (2000), IACCARINO et alii (2004), DI STEFANO et
alii (2008). Regarding calcareous nannoplankton assemblages the
schemes are: for Oligocene and early Miocene FORNACIARI & RIO
(1996); for Middle Miocene FORNACIARI et alii (1996), with
modifications of SPROVIERI et alii (2002) and DI STEFANO et alii,
2008. The scheme of THEODORIDIS (1984), using the FO of
Minylitha convallis and the FO of Amaurolithus primus is used
for the Tortonian / Messinian. The scheme of IACCARINO et alii
(2001) was also considered useful because report events, such as
the FO of Amaurolithus delicatus, the FO of Discoaster
quinqueramus and the FO of Discoaster surculus. D.
_________________________
Biostratigraphic dating as a useful tool for the reconstruction of
Central and Southern Apennine evolution
(*) DSGA Università degli Studi del Sannio, f.amore@unisannio.it
FILOMENA ORNELLA AMORE (*), UBALDO SANTINI (*) & ITALO SGROSSO (*)
226
quinqueramus is a symmetrical 5-arms species, and has its FO in
the Atlantic Ocean, just above the FO of D. berggrenii, which
occurs at 8.3 Ma (BACKMAN & RAFFI, 1997; RAFFI et alii, 1998).
D. surculus has its FO in the Indian Ocean and the Equatorial
Pacific Ocean, sporadic and discontinuous in the CN8 (BUKRY,
1973). The species is present, however, continuously and with
typical specimens from the base of the zone CN9, just above the
appearance of D. berggrenii (RAFFI et alii, 1995). These species,
although quite rare in the middle latitudes and the Mediterranean
Sea (THEODORIDIS, 1984; IACCARINO et alii, 2001; RAFFI et alii,
2003), however, were sometimes recognized in the Apennine
sequences and in the Maltese series (MAZZEI, 1985; AMORE,
1992; CIPOLLARI & COSENTINO, 1995; FORESI et alii, 2001,
among others). Although not particularly abundant these species
are useful as the phenomena of reworking, the inability to achieve
a high resolution sampling and lack of ability to use the LO
already greatly reduce the biostratigraphic resolution.
INVESTIGATED AREAS
We discuss, here, dating performed on Miocene deposits in
stratigraphic contact with the most important structural units that
are recognized in this portion of Apennines, in order to date the
most important moments of their kinematic evolution. These
moments are: a) Miocene “para-conformity” transgression; b)
drowning of the platform; c) start of arcose- silicoclastic
sedimentation (mature fore-deep phase); d) first discordant
stratigraphic contact (first thrust top basin); e) possible second
discordant stratigraphic contact (second thrust top basin). The
main formations, about which we discuss the biostratigraphic
dating, are: Flysch del Bifurto, Piaggine Formation, M. Sierio
Formation, Flysch di Castelvetere, Arenarie di Caiazzo, Brecce di
S. Massimo. These biostratigraphic data are connected each
other, as they represent the deformation that moves through time
and space, affecting more and more external domains. We believe
it is useful to clarify the views on these dates, used in mapping
CARG and in geodynamic and paleogeographic reconstructions
recently proposed.

REFERENCES
AMORE F. O. (1992) – Studi biostratigrafici dei sedimenti
miocenici del bacino molisano: nannoplancton calcareo. Tesi
di Dottorato in Geologia del sedimentario, Università
“Federico II” di Napoli.
AMORE O., CIAMPO G., DE CAPOA P. & RUGGIERO E. (1988) –
Problemi biostratigrafici dei sedimenti terrigeni
nell’Appennino centro-meridionale. Mem. Soc. Geol. It., 41,
pp. 621-625.
AMORE O.F., BONARDI G., DI STASO A., CIAMPO G., DE CAPOA
P., MORABITO S., RUGGIERO E. & SGROSSO I. (2005) - The
progress of knowledge about the miocene successions of the
southern Apennines following Selli’s papers of 1957 and
1962. Boll. Soc. Geol. It., 4, 37-44.
BACKMAN J. & RAFFI I. (1997) - Calibration of Miocene
nannofosil events to orbital tuned cyclostratigraphies from
Ceara Rise. Proc.ODP Sci. Results, 154, 83-99.
BOWN P.R. (1999) - Calcareous nannofossil biostratigraphy.
Kluwer Academic Publishers, Cambridge Univ. Press,1 –
314.
BUKRY D. (1973) – Low-latitude coccolith biostratigraphic
zonation. Init. Rep. DSDP, 15,685-703.
CIPOLLARI P. & COSENTINO D. (1995) – Miocene unconformities
in the central Apennnines: geodynamic significance and
sedimentary basin evolution. Tectonophysics, 252, 375-389.
DE CAPOA P., DI DONATO V., DI STASO A., GIARDINO S. &
RINALDI S. (2003) - Preparation techniques and
methodological approach to calcareous nannofossil analysis
in silico- and calciclastic turbidites. Cour. Forsch Inst.
Senckenberg, 244, 105-127.
DI STEFANO A., FORESI L.M., AMORE F.O., DI STEFANO E.,
IACCARINO S., LIRER F., MAZZEI R., MORABITO S.,
SALVATORINI G., TURCO E., ABDUL AZIZ H., KRIJGSMAN W.
&HILGEN F. (2008) - Calcareous plankton high resolution
biostratigraphy for the Langhian of the Mediterranean. Riv.
It. Pal. e Strat., 114, 56-72.
FORESI L.M., IACCARINO S., MAZZEI R., SALVATORINI G. &
BAMBINI A.M. (2001) – Il plancton calcareo (Foraminiferi e
nannofossili) del Miocene delle Isole Tremiti. Paleont. Italica,
88,1-64.
FORNACIARI E., DI STEFANO A., RIO D. & NEGRI A. (1996) –
Middle Miocene quantitative calcareous nannofossil
biostratigraphy in the Mediterranean region.
Micropaleontology, 42 (1), 1 - 36.
FORNACIARI E. & RIO D. (1996) – Latest Oligocene to early
middle Miocene quantitative calcareous nannofossil
biostratigraphy in the Mediterranean region.
Micropaleontology, 42 (1), 1 - 36.
227
HILGEN F.J., IACCARINO S., KRJIGSMAN W., VILLA G., LANGEREIS
C.G. & ZACHARIASSE W.J. (2000) - The Global Boundary
Stratotype Section and Point of the Messinian stage
(uppermost Miocene). Episodes, 23, 172-178.
IACCARINO S., FORESI L.M., MAZZEI R. & SALVATORINI G. (2001)
– Calcareous plankton biostratigraphy of the Miocene
sediments of the Tremiti Islands (Southern Italy). Rev. Espan.
Micropal., 33 (2), 237-248.
IACCARINO S., LIRER F., BONOMO S., CARUSO A., DI STEFANO A.,
DI STEFANO E., FORESI L. M., MAZZEI R., SALVATORINI G.,
SPROVIERI M., SPROVIERI R. & TURCO E. (2004) -
Astrochronology of late Middle Mediterranean sections. In:
B. D'Argenio et alii (eds) - Ciclostratigraphy: An Essay of
Approaches and Case Histories . SEPM Spec. Publ., 81, 25-
42.
IACCARINO S. M. & PREMOLI SILVA I., BIOLZI M., FORESI L.M.,
LIRER F., TURCO E. & PETRIZZO M.R. (2007) – Practical
Manual of Neogene Planktonic Foraminifera. Perugia 19-23
February.
MAZZEI R. (1985). – The Miocene sequence of the Maltese
islands: biostratigraphic and chronostratigraphic reference
based on nannofossils. Atti Soc. Tosc. Sc. Nat., Serie A, 92,
165-197.
RAFFI I., RIO D., D’ATRI A., FORNACIARI E. & ROCCHETTI S.
(1995) – Quantitative distribution patterns and
biomagnetostratigrapfy of middle and late Miocene
calcareous nannofossils from equatorian Indian and Pacific
Oceans (Leg 115, 130, and 138). Proc. ODP Sci. Results,
138, 479-502.
RAFFI I., BACKMAN J. & RIO D. (1998) – Evolutionary trends of
tropical calcareous nannofossils in the late Neogene. Mar.
Microp al., 35,17-41.
RAFFI I., MOZZATO C, FORNACIARI E., HILGEN F.J. & RIO D.
(2003) – Late Miocene calcareous nannofossil
biostratigraphy and astrobiochronology for the
Mediterranean region. Micropaleontology, 49 (1), 1-26.
SPROVIERI R., BONOMO S., CARUSO A., DI STEFANO A., DI
STEFANO E., FORESI L.M., IACCARINO S.M., LIRER F., MAZZEI
R. & SALVATORINI G. (2002) – Integrated calcareous
plankton biostratigraphy and biochronology of the
Mediterranean Middle Miocene. In: Iaccarino S. (Ed.)
Integrated stratigaphy and paleoceanography of the
Mediterranean Middle Miocene. Riv. Ital. Paleontol .S., 108
(2), 337-353.
THEODORIDIS S. (1984) – Calcareous nannofossil biozonation of
the Miocene and revision of the Helicoliths and Discoasters.
Utrecht Micropaleontological Bullettin, 32, 1 - 271.
SESSIONE 9

SESSIONE 9
Lithological and palaeontological records of the Maiolica Formation
in Umbria-Marche Apennines (Italy)
Key words: Biostratigraphy, calpionellids, calcareous
nannofossils, Italy, Maiolica, Umbria-Marche Apennine.
This study is aimed to compare lithological and
palaeontological differences between the Maiolica Formation
deposited above the Jurassic pelagic carbonate platforms and
within troughs of Umbria – Marche Domain. The development of
distinct pelagic carbonate platforms (PCP of SANTANTONIO,
1994) and trough successions ceased in Umbria–Marche during
the latest Tithonian with Maiolica deposition (CENTAMORE et
alii, 1971; FARINACCI et alii, 1981). However, topographic
gradients on the sea bottom, though less pronounced than in the
Jurassic, persisted in the Early Cretaceous as demonstrated by
LOWRIE &ALVAREZ (1984). The pelagic carbonate platforms
were surrounded by deep troughs characterized by different facies
and thicker successions.
A crucial tool to constrain the sedimentary evolution of the
Maiolica Fm. is the study of calpionellids and calcareous
nannofossils. The calpionellids, calcareous microplankton
protists, characterize the Tithonian–Hauterivian interval in the
Tethyan realm, with a potential biostratigraphic application from
the Upper Tithonian to the Upper Valanginian. Fossils of
calcareous nannoplankton have been found in limestones and
chalks since the Jurassic and allow to improve the dating of
Meso-Cenozoic sedimentary successions. The study successions
(Fonte del Giordano and Campo al Bello sections) outcrop on the
south-western slope of M. Nerone (Umbria - Marche Apennines).
The studied interval at Fonte del Giordano section is represented
by cherty limestones (8 metres) belonging to Calcari Diasprigni
Unit and light brownish to whitish limestone with chert belonging
to Maiolica Fm. (104 metres). The calpionellid assemblages are
quantitatively abundant and Crassicollaria and Calpionella and
Calpionellopsis and Calpionellites Zones are recorded. The
Microstaurus chiastius, Nannoconus steinmannii steinmannii and
Cretharhabdus angustiforatus calcareous nannofossil Zones have
been recognized based on the first occurrence of Nannoconus
_________________________
(*) Università degli Studi di Perugia, Dipartimento di Scienze della Terra,
paleodot@unipg.it
GLORIA ANDREINI (*) & GUIDO PARISI (*)
228
steinmannii steinmannii and Cretharhabdus angustiforatus,
actually the first occurrence of Nannoconus steinmannii minor
allow us to recognize also the Nannoconus steinmannii minor
Subzone whilst the appearance of Percivalia fenestrata has not
been recognized (ANDREINI et alii, 2010). This succession
suggest that this area was part of a trough located on the southern
margin of Monte Nerone.
The Campo al Bello section corresponds to PCP area (CECCA
et alii, 1990) and the Maiolica Fm. lies in stratigraphic succession
to Bugarone. This section is represented by light brownish to
whitish limestone with chert belonging to Maiolica Fm. (6,40
metres). The texture ranges by packstones / wackestones with
Globochaete, Saccocoma, radiolaria and aptychi, until mudstones
with calpionellids. Calpionellid biostratigraphy recorded
Crassicollaria Zone (remanei and intermedia subzone) and
Calpionella Zone (alpina and remanei subzone). Calpionellids are
scarce and characterized by low diversity.
With respect to the previous dating achieved during the
realization of the Geological map of Italy (scale 1:100.000), this
study shows that the integrated biostratigraphy based on
calcareous nannofossil and calpionellid events is an important
tool to refine the dating of this units and to characterize the
sedimentary features of the Maiolica Formation in Umbria-
Marche Domain.
REFERENCES
ANDREINI G., DE ANGELIS A., PARISI G., PERILLI N. & SPERANZA
F. (2010) - Integrated magneto - biostratigraphy across
Tithonian - Valanginian time interval fron Fonte del
Giordano Section (Umbria - Marche Domain, central Italy).
The Colors of Cretaceous and Paleogene Oceans (Attribute to
Isabella Premoli Silva), Abstract Book, 17
CECCA F., CRESTA S., PALLINI G. & SANTANTONIO M. (1990) - Il
Giurassico di Monte Nerone (Appennino Marchigiano, Italia
Centrale): biostratigrafia, litostratigrafia ed evoluzione
paleogeografica. Atti II Convegno Internazionale “Fossili,
Evoluzione, ambiente”, Pergola 1987, 63-139.
CENTAMORE E., CHIOCCHINI M., DEIANA G., MICARELLI A. &
PIERUCCINI U. (1971) - Contributo alla conoscenza del
Giurassico dell'Apennino umbro-marchigian. Studi Geol.
Camerti, 1, 7-89.

FARINACCI A., MARIOTTI N., NICOSIA U., PALLINI G. &
SCHIAVINOTTO F. (1981) - Jurassic sediments in the umbromarchen
Apennines: an alternative model. Proc. “Rosso
Ammonitico Symp.”. Tecnoscienza, 335-398.
LOWRIE W. & ALVAREZ W. (1984) - Lower Cretaceous magnetic
stratigraphy in Umbrian pelagic limestone sections. Earth Pl.
Sci. Lett., 71 (2), 315-328.
SANTANTONIO M. (1994) - Pelagic carbonate platforms in the
geologic record; their classification, and sedimentary and
paleotectonic evolution. AAPG Bulletin, 78 (1), 122-141.
229
SESSIONE 9

SESSIONE 9
Contribution of the CARG Project to the reconstruction of the mode
and time of the emplacement of the “Coltre della Val Marecchia”
Key words: CARG, Coltre della Val Marecchia, foredeep,
Miocene-Pliocene.
INTRODUCTION
The detailed geological map survey of the area between Badia
Tedalda and the upper Foglia River, in the Marecchia Valleyupper
Montefeltro, and the relative 1:50,000 scale cartography
produced for the CARG Project and for regional cartographic
projects (Marche and Emilia Romagna), allowed to examine the
relationships between tectonics and sedimentation of the
successions of such outer sector of the Northern Apennines
foredeep. The main goal has been the development of a new
evolutive framework for this sector of the orogen during
Messinian-early Pliocene. Several new informations about the
geological-structural setting and stratigraphy come out from the
new geological maps. These are overall sustained by stratigraphic
evidences, which suggest time and modalities of the “Coltre della
Val Marecchia” (CVM) allochthonous emplacement within the
Messinian-early Pliocene foredeep sedimentation.
GEOLOGICAL FRAMEWORK
The CVM represents the outermost allochthonous Ligurian
rocks of the Northern Apennines. It shows the opportunity to
observe the advancing front of the Ligurian units during the postevaporitic
phases of development of the orogen. The CVM is
formed by several embricate slices, bordered by arcuate-shape
tectonic contacts, with convexity toward NW or WNW and
moderate SW dip (Fig. 1). The slices forming the CVM are
structured with strongly deformed-plastic lithologies of the
Argille Varicolori Fm. at the bottom and upward more competent
_________________________
FILIPPO BONCIANI (*), GIANLUCA CORNAMUSINI (*°), IVAN CALLEGARI (*),
PAOLO CONTI (*°), LUCA MARTELLI (**) & LUIGI CARMIGNANI (*)
(*) Centro di Geotecnologie, Università di Siena, cornamusini@unisi.it
(°) Dipartimento di Scienze della Terra, Università di Siena
(**) Servizio Geologico, Sismico e dei Suoli, Regione Emilia Romagna
230
formations (Sillano Fm. and Monte Morello Fm.) or directly the
epiligurian formations, through angular unconformity. The
epiligurian formations form competent layers always lying onto
the Argille Varicolori Fm., through the Oligocene-Burdigalian
formations for the inner part of the CVM and through the
Messinian formations for the outer part. The paleoautochthonous
and neoautochthonous substrata are formed by the whole pre- and
syn-evaporitic “Umbro-Marchean-Romagnan Succession” and
“Padan-Adriatic margin post-evaporite Succession”, sedimented
respectively during late Burdigalian to late Messinian and from
this to Pleistocene. The two above successions are divided by an
unconformity of regional significance, linked with the intra-
Messinian tectonic phase. The bottom surface and distribution of
the CVM resulted to be influenced by the general
paleophysiography and by the morphostructural lineaments
occuring during the emplacement phases.
EMPLACEMENT OF THE “COLTRE DELLA VAL
MARECCHIA”: A MODEL WITH TWO FLOWS
The analysis of the geometrical relationships among the
mapped tectono-stratigraphic units draws a regional geological
framework of great interest for the interpretation of the relative
chronology of the depositional and tectonic events involving this
sector of the foredeep during late Miocene up to middle
Pleistocene. In particular, two main flow-transport directions for
the CVM have been detected. They are distinct on the basis of the
age of the paleogeographical set, so to emphasize two distinct
gravitational flow-bodies, which are the CVM1 and the CVM2
(Fig. 2), joined with tectonic events and lineaments showed in the
geological maps. The first CVM event (late Messinian) followed
the Tortonian Ligurian Units thrust onto the Marnoso-Arenacea
along the apenninic front of the Mt. Fumaiolo and the
sedimentation of the foredeep turbidites (Sant’Agata Feltria
Sandstones) closed with the several precursory
Ligurian/Epiligurian olistoliths and olistostromes. The antiapenninic
Sant’Agata Feltria transversal fault (FSA) was already
active during this event, constraining the morphological
conditions to drive the turbidite flows before and the Ligurian
allochthonous bodies after, along the northern alignment (Fig.

Fig. 1 – Gelogical-structural sketch map of the Val Marecchia area with on evidence the distribution of the CVM (its northernmost part is not showed). Green
colours indicate the Ligurian fms of the CVM. The brown-pink formations on the top of the CVM belong to the Epiligurian succession.
2A). The foredeep basin appear to be subdivided in a
northwestern part, which is characterized by a sedimentary
succession typical of a structural/morphological high
(resedimented gypsum lithofacies belonging at the Tetto Fm.) and
in a southeastern part characterized by a deep basin succession.
The above two parts are separated by a depression zone
coincident with the FSA direction, where the turbidites, the
olistostrome bodies and the CVM1 flowed. The totally infilling of
the northern basinal depression is also documented by the
sedimentation of the very shallow marine environment Perticara
Sandstones. The second event is of early Pliocene age, with the
231
emplacement in the basin of the more thick southern
allochthonous body (CVM2, Fig. 2B). It flowed through a more
complex morphological depression, which was aligned with the
Molino di Bascio transversal fault (FMB). It results to be
confined to north by the northern CVM1 body and to south by the
Macerata Feltria structural high. The body of the CVM2 through
its flow trajectory (Fig. 2B) shows the avoidance of such
structural high, as demonstred by the geometry and convexity of
the allochthonous slices of the CVM2.
Fig. 2 – Phases of emplacement of the CVM. A – Late Messinian first phase (CVM1); B – Early Pliocene second phase (CVM2).
SESSIONE 9

SESSIONE 9
The Passignano sul Trasimeno sheet of the 1.50.000 scale Geological
Map of Italy: new insights about the Northern Apennine geology from
CARG Project results
ARNALDO BOSCHERINI (*), MASSIMILIANO BARCHI (**), LUCA GASPERINI (°), MICHELE MARRONI (°°), ANDREA MOTTI (*),
LUCA PANDOLFI (°°), LEONSEVERO PASSERI (*), PATRIZIA ARGENTI (**), ANGELA BALDANZA (**), MARCO BARSELLA (°°),
LUCA GIORGIO BELLUCCI (°), ROBERTO BIZZARRI (**), GIOVANNI BORTOLUZZI (°), FLAVIA BOTTI (°°),
ALESSIO CHECCONI (**), GLORIA CIARAPICA (**), FRANCESCA MENEGHINI (°°), SILVIA PALANDRI (°°),
CRISTINA PAUSELLI (**), FAUSTO PAZZAGLIA (**), FRANCESCO PONZIANI (*),
GIANLUIGI SIMONE (*) & FEDERICO VENTURI (**)
Key words: CARG Project, geological mapping, Northern
Apennine, Trasimeno lake.
INTRODUCTION
The goal of the geological mapping in the frame of the CARG
(CARtografia Geologica) project is represented not only by a
new cartography, devoted to be an useful tool for the country
planning, but consists also in an impressive collection of new data
about the investigated area.
An example of mapping associated to a production of new
data is provided by Passignano sul Trasimeno sheet of the
1.50,000 scale Geological Map of Italy. During this project, new
data about the sedimentology and stratigraphy of the Plio-
Pleistocene deposits, as well as about the geological structure of
the Trasimeno lake and the foredeep successions from Tuscan,
Rentella and Umbro-Marchean units have been collected.
GEOLOGY OF THE PASSIGNANO SUL TRASIMENO
AREA
The Passignano sul Trasimeno area is characterized by a
NW-SE striking stack of the Tuscan, Rentella and Umbro-
Marche tectonic units where Mesozoic to Tertiary ramp foreland
and foredeep deposits are well preserved. The stratigraphic and
tectonic features of these deposits are the result of the progressive
migration of the compressive deformation fron toward the eastern
domains of the Adria plate during the Miocene.
The stack of tectonic units is unconformably covered by Plio-
Pleistocene sediments (Tiberino and Val di Chiana
_________________________
(*) Servizio Geologico e Sismico, Regione Umbria, aboscherini@regione.umbria.it
(**) Dipartimento di Scienze della Terra, Università degli Studi di Perugia
(°) Istituto di Geologia Marina – ISMAR,CNR
(°°) Dipartimento di Scienze della Terra, Università degli Studi di Pisa
232
supersynthemes) deposited in fault-bounded basins developed
during the extensional tectonics that followed in space and time
the compressive one. The Pliocene sediments, that crop out in the
western side of the Trasimeno Lake, are regarded as marine
environment deposits, whereas the eastern side is characterized
by continental to lacustrine Pleistocene sediments. In this frame
the Trasimeno lake, a ~10 km diameter, shallow (

233
SESSIONE 9

SESSIONE 9
Key words: CARG project, geological map, geothematic
cartography, Regione Umbria.
Geological mapping of Italy at scale of 1:50000 started and
quickly improved after Law n. 305 of 28/12/1989 dealing with
long term financial planning of Ministry of Environment. One of
the purposes of this law was to promote the sound use of the
environment with the creation of CARG project (where CARG
stands for CARtografia Geologica, the geological mapping of
Italy at scale of 1:50,000).
At the same time Regione Umbria starts a program of
restoration of buildings and places hit by the earthquake of
19/09/1979 and with the budget of another law (Regional Law n.
25/89 art. 22) started geological mapping of Valnerina at
1:10,000 scale.
Regione Umbria realized, both with the help of new budget
from Ministry of Environment and the project at 1:10.000 scale
geological mapping, the CARG project at scale 1:50.000, a
technical and scientific project of great importance for
environmental purposes and more specific than the earlier
1:100.000 geological maps.
At present Regione Umbria Geological sheets at scale of
1:50,000 are: n. 289 "Città di Castello", n. 299 "Umbertide", n.
336 "Spoleto", n. 310 "Passignano sul Trasimeno", n. 324
"Foligno" where new scientific criteria were applied, for instance
divisions between continental deposits in UBSU (Unconformity-
Bounded Stratigraphic Units) and for turbiditic successions the
creation of “membri” as lower level litostratigraphic units.
Detailed geological cartography has become an essential
instrument of research for environmental and applicative
purposes for analysis of hot-spots, such as hydrogeological and
hydraulic damage, the protection of underground water resources
and definition of local seismic hazard. Case studies are
represented by landslides affecting roads and cities like Orvieto,
Valnerina valley also in relation with geological characteristics
and their displacements.
Finally, geological cartography at 1:10.000 scale has revealed
_________________________
(*) –
geologicoesismico@regione.umbria.it
Geological and geothematic cartography of Regione Umbria:
the impulse of CARG project and its application
ARNALDO BOSCHERINI (*), ANDREA MOTTI (*), NORMAN NATALI (*) & GIANLUIGI SIMONE (*)
234
itself of the utmost importance for planning new road or railway
routes, to point out the importance of geosites like S. Venanzo’s
volcanic apparatus, Marmore’s fall, Dunarobba’s fossil forest; for
its contribute to underground water research in times of the water
emergency that led government to publish the act “O.P.G.R. n.
48/04” as well to hydrogeological case study of Amerini
mountains and Volsinii volcanic apparatus or to the analysis of
underground water resources in North Eastern Umbria, a project
called “Hydrogeology of Mt. Cucco and Gualdo’s mountains”.
Without the CARG Project, detailed study of the environment
and hazard planning would have been more difficult or worse
never could start.

Key words: Geological map, geothematic cartography, Regione
Umbria.
Geological and Seismic Survey of Regione Umbria planned
the geothematic cartography with the contribution of professional
geologists aimed to give the most detail information about the
geological, seismic and hydrogeological hazards.
Among thematic cartography, of great importance some
oriented in localizing and in land-use planning, the
hydrogeological cartography projects at various scale map and
the local seismic hazard geothematic cartography, at scale
1:10.000.
On July 2010 Regione Umbria coverage was completed with
the geothematic cartography and it’s now available a very
detailed seismic analysis with localization of seismic
amplifications, due to different stratigraphic and/or
morphological conditions, which are likely to happen.
There are 5 possible situations:
1) areas not interested by seismic amplification;
2) unstable areas (split into 4 different categories) where,
active or not, landslides or condensations of soils are mapped and
can be reactivated or exploited by seismic shocks;
3) areas (split into 2 different categories) with particular
morphological characteristics which can lead to amplifications of
ground shaking or to local collapsing due to increasing seismic
waves;
4) areas (split into 3 different categories) where seismic
ground shaking is likely to happen due firstly to difference of
seismic characteristics between bedrock and soft rock and latter
then to geometry with subsequential effects on concentrations of
seismic waves;
5) areas where ground shaking with different amplitude and
_________________________
Geothematic cartography applications in Regione Umbria
ARNALDO BOSCHERINI (*), ANDREA MOTTI (*), NORMAN NATALI (*) & GIANLUIGI SIMONE (*)
(*) Regione Umbria – Servizio Geologico e Sismico,
geologicoesismico@regione.umbria.it
235
frequencies are likely to happen just where geologic elements
with high contrast of physical or mechanical properties overlap.
The set of geothematic cartography realized by Geological
and Seismic Survey of Regione Umbria, is intended to be an
essential support to the end user for responsible planning in
respect of the natural resources of which Umbria is so rich, as
well as their preservation for the next generation.
SESSIONE 9

SESSIONE 9
Unconformity Bounded Stratigraphic Units of the Plio-Pleistocene
basins of the upper catchment of the Arno (Tuscany): a proposal
Key words: Northern Apennines, Pleistocene, UBSU
INTRODUCTION
The geomorphology of the upper catchment of the Arno is
characterized by wide tectonic basins (form South to North: Val
di Chiana, Arezzo, Casentino and Valdarno, Fig. 1) related to the
Plio-Pleistocene collapse of relevant crustal blocks of this sector
of the Northern Apennines chain. During their subsidence the
overall length and wideness of the basins were controlled by
prevailing NW-SE oriented normal faults and by NE-SW
trending faults and/or structural highs. These latter tectonic
features limited the longitudinal extension of the basins and
complicated their floor morphology. The collapse of the basins
induced a significant change of the previous hydrographic
network (MAZZANTI & TREVISAN, 1978) and promoted the
formation of new and differentiated depositional environments,
such as alluvial fans, flood plains, lakes and swamps. The basins
have long been areas of subsidence and were filled by relatively
thick clastic sedimentary successions. However, the oscillations
of the base level did prevail the erosion during some time
intervals and the stratigraphic continuity of the sedimentary
successions was interrupted by wide erosive surfaces, i.e. by
surfaces of unconformities.
Unfortunately the no uniform completion of the CARG
project does not allow new age determinations of these
unconformity surfaces. Therefore, their age, stratigraphic position
and areal extension can only be inferred from literature, field
reconnaissance and consultation of the 1:10,000 geological maps,
freely available online by the “Regione Toscana-Progetto di
Cartografia Geologica” (cfr. MORINI &BRUNI, 2004). Moreover
the project has been attended by several research groups that
proposed different stratigraphic and structural reconstructions.
The UBSU architecture illustrated in this contribute (Fig. 2) is
derived from field controls and by the compilation of a new
geological map at 1:50,000, which summarizes and homogenizes
the 1:10,000 geological maps available on line for the examined
area. The stratigraphic proposal and the chronologic
correlations must be considered provisional.
___________________
(*) Dipartimento di Scienze della Terra, Università di Firenze,
bruni@geo.unifi.it
PIERO BRUNI (*) & GIOVANNA CECCHI (*)
236
THE UBSU ARCHITECTURE OF THE PLEISTOCENE
SUCCESSIONS
The major results of our study may be summarized as it
follows. The basins are separated by structural highs. They
favoured appreciable differences on the lithology, paleo-current
orientation and areas of clasts supply during the sedimentation of
the successions. Some of them still retain their topographical
evidence and have been effective throughout the Pleistocene. The
Val di Chiana Basin was separated from the Arezzo Basin by the
Chiani-Olmo structural high, and the Arezzo Basin was in turn
separated from the Valdarno Basin by the Rondine structural
high. By the end of the filling of the basins and with the
simultaneous action of the erosion, the sedimentation buried some
structural highs. In this case (eg. Rondine and Incisa structural
highs) the two adjoining basins show the same synthem in their
Fig. 1 – The Plio-Pleistocene basins of the Northern Apennines (redrawn and
modified from BOSI et alii, 1995).
stratigraphically higher portion (eg. Sintema del Torrente
Ciuffenna). As shown in Fig. 2, all the Pleistocene sequences lie
on an erosive surface, are interrupted by an unconformity and at
the top are closed by an old depositional surface. Geological
maps show that these unconformities have a basin extension, but
in our view they can overcome the basin boundaries and extend
to the other basins. In this case the main limits of the UBSU
could represent an useful tool to correlate the basin successions.

Fig. 2 – - Chronostratigraphic diagram summarizing the Unconformity Bounded Stratigraphic Units of the Pleistocene successions (from south to north) of Val
di Chiana, Arezzo, Casentino and Valdarno basins. The structural highs and the tentative time correlations are shown (from GHINASSI &MAGI, 2004; ARUTA et
alii, 2004).
Referring to the data known for the Valdarno Basin, the lower
synthem of the Pleistocene sedimentation (Fig. 2) could be lasted
from the base of Gelasian up to the first half of Calabrian. Later,
the sedimentation was interrupted up to the end of the
Calabrian. The geological maps show that erosion has deeply
penetrated the underlying synthem and in some cases has reached
the substrate. The youngest synthem represents a important part
of the Ionian, followed by a new erosional episode. The latter has
profoundly sculptured all the Pleistocene synthems as well as the
major valleys of the present-day hydrographic pattern
(BARTOLINI &PRANZINI, 1981).
REFERENCES
ARUTA G., BORGIA,BRUNI P., CECCHI G., CIPRIANI N. & TREDICI
Y. (2004) – Pliocene and Pleistocene Unconformity Bounded
Stratigraphic Units (UBSU) in Val di Chiana. In: Morini &
Bruni (eds), 133-136.
237
BARTOLINI C. & PRANZINI G. (1981) – Plio-Quaternary evolution
of the Arno basin drainage. Z. Geomorph., Suppl., 40, 77-91.
GHINASSI M. & MAGI M. (2004) – Variazioni climatiche,
tettonica e sedimentazione al passaggio Pliocene Medio-
Pliocene Superiore nel bacino del Valdarno Superiore
(Appennino Settentrionale). Boll. Soc. Geol. It., 123, 301-
310.
MAZZANTI R. & TREVISAN L. (1978) – Evoluzione della rete
idrografica nell’Appennino centro-settentrionale. Geog. Fis.
Dinam. Quat., 1, 55-62.
MORINI D. & BRUNI P. (2004) – The “Regione Toscana” Project
of Geological Mapping: case histories and data acquisition.
Regione Toscana, Firenze, 262p.
SESSIONE 9

SESSIONE 9
The modal analysis as a stratigraphic tool to discriminate the
perisutural Oligocene and Miocene turbidite successions of the
Northern Apennines
PIERO BRUNI (*), NICOLA CIPRIANI (*), MASSIMO NEBBIAI (*) & ENRICO PANDELI (* , **)
Key words: modal analysis, Northern Apennines, regional
geology, siliciclastic turbidites, Tertiary, Tuscan and
Umbrian Domains.
The reconstruction of the stratigraphic architecture and the
structural setting of the thick and widely outcropping Oligocene
and Miocene perisutural turbidite successions of the Northern
Apennines is discussed since they have similar lithologies, weak
biostratigraphic signals and are intensely involved in the thrustand-fold
structures of the chain, particularly from Abetone-
Mt.Cervarola area up to the Trasimeno Lake. Different
stratigraphic and tectonic interpretations have been proposed in
the geological literature for the palinspastic restorations of the
sedimentary basins of these turbidite units. Aim of this
contribution is to resume and compare new or already published
petrographic modal analyses of medium to coarse grained
arenites sampled at a regional scale by the authors in typical areas
of outcrop. That is: 1) Abetone (Macigno); 2) Dardagna and
Reno valleys, Suviana Lake-Montepiano areas, Pratomagno
(Falterona Sandstone), 3) Mt.Coroncina-Castiglion dei Pepoli
(Castiglion dei Pepoli Sandstone), 4) north-eastern Mugello
(Castel Guerrino Sandstone), 5) Santerno and Tiber valleys
(Marnoso-arenacea), 6) Porretta (Porretta Sandstone). Our results
evidence that the petrographic modal analysis is a reliable tool
to appreciate the distinction between the turbidite units (see Figs.
1 and 2):
(A) - ternary and binary diagrams of the data evidence
significative differences i) in the aphanitic rock fragments and
carbonate grains diagram (Lm, Lv, Ls+C) and ii) in the ratio
monocrystalline non-undulose quartz/monocrystalline between
Macigno and Falterona Sandstone. In our opinion the two
turbidite units were deposited in separated basins supplied by
distinct source areas of the terrigenous inputs. These data suggest
that the regional-scale tectonic alignment separating Macigno
from Falterona is a relevant tectonic feature separating the
Tuscan Nappe, toward SW, from the Falterona Unit, toward NE.
_________________________
(*) Dipartimento di Scienze della Terra, Università di Firenze,
pandeli@geo.unifi.it
(**) IGG (Istituto di Geoscienze e Georisorse) - CNR, Firenze
238
(B) - Acquerino, Carigiola and Stagno and the Castiglion dei
Pepoli Sandstone pp. (CDP1 Member in the 1:50.000 Geological
Map of Italy- Sheet n. 252 – Barberino di Mugello) turbidite
units have the same petrofacies of the Falterona Sandstone; the
data confirm that these units are tectonic elements of the
Tectonic Falterona Unit. (C) Mt. Coroncina-Castiglion dei Pepoli
Sandstone and Castel Guerrino Sandstone (CDP2 Member and
Carigiola Sandstone p.p., respectively, in the 1:50.000 Geological
Map of Italy - Sheet n. 252 – Barberino di Mugello) are
characterized by the same petrographic composition and, in turn,
have many analogies with the Marnoso-arenacea. Therefore, for
these three units we suggest a common source area of the clastic
inputs and the location of their sedimentation areas within the
Emilian-Romagna-Umbrian Domain. (D) Porretta Sandstone (or
Suviana Sandstone) has peculiar petrographic composition and
cannot be compared with the petrofacies of the other examined
turbidite units; Porretta Sandstone probably has epiligurian
affinity.
Fig. 1 - Aphanitic rock fragments and carbonate grains diagram (Lm,Lv and
Ls+c)

.
LEGEND
Fig. 2 – Qm 0-5°/Qm vs. Lm/L diagram
239
SESSIONE 9

SESSIONE 9
Key words: Calcareous turbidites, Chattian-Aquitanian,
Northern Apennines.
INTRODUCTION
Macigno and Falterona Sandstone are two thick, terrigenous,
Oligocene to Lower Miocene turbidite successions of the
Tuscan Domain, severely involved in the thrust sheets and in the
folded structures of the Northern Apennines. Since they have
similar lithologies, weak biostratigraphic signals and are
partially coeval, it is problematic to recognize their stratigraphic
architecture and to correlate the sections on regional scale.
Different stratigraphic and tectonic interpretations of these
perisutural turbidite units have been proposed, as well as
different palinspastic restorations of their sedimentary basins
(cfr. ABBATE &BRUNI, 1989). To contribute in solving these
problems, here we illustrate and compare unpublished and
published biostratigraphic nannoplankton analyses of calcaerous
turbidites sampled in two typical and well known sections: M.
Rondinaio/M. Gomito section, near Abetone (PT), for the
Macigno (belonging to the Tuscan Nappe); Trappola/Croce di
Pratomagno, outcropping in the western side of the Pratomagno
(FI-AR), for the Falterona Sandstone (belonging to the
Falterona Unit).
SAMPLE-COLLECTING AND METHODOLOGY
The very low content of calcareous microfossils (calcareous
nannoplankton and forams) in the pelite portion of the
siliciclastic beds usually requires a great amount of samples for
reliable biostratigraphic analyses. An undoubted difficulties
which can be partially overcome for the two turbidite units.
The lithologies of Macigno and of the Monte Falterona:
sandstone are characterized by prevailing sandstones, which
alternate with clayey silts, marls and shales. Occasionally there
_________________________
The biostratigraphic signal of the calcareous turbidites of Macigno
and Falterona Sandstone (Northern Apennines)
(*) Dipartimento di Scienze della Terra - Università di Firenze,
bruni@geo.unifi.it
(**) IGC (Istituto di Geoscienze e Georisorse) - CNR, Firenze
PIERO BRUNI (*), ENRICO PANDELI (*) (**) & VIVIANA REALE (*)
240
are also graded calcareous turbidites that are decimetric to
locally metric in thickness (eg. ARUTA et alii, 2004) and lateral
traceable at regional scale. This contribute aims to present the
preliminary results of calcareous nannoplankton analysis
performed on samples collected in these calcareous turbidite
beds (Fig. 1). The samples have been collected in the uppermost
part of the nannofossil-rich marly interval. By this way it has
been possible to detect a good biostratigraphic signal with low
number of samples. According to FORNACIARI &RIO (1996),
two methods of calcareous nannofossil counting were
performed: 1) counting index species versus total assemblages
(300 specimens); 2) abundance patterns of index sphenoliths
(100 sphenoliths).
RESULTS
The biostratigraphic signal of the calcareous turbidites
assignes the lower Macigno (from the base up to 1.900 m) to the
Chattian. Upward, for about one thousand meters up to the
stratigraphic top of the unit, the biostratigraphic signal is weak
and the transition Chattian/Aquitanian is not confirmed.
For the Falterona Sandstone, the analyses indicate the
Chattian for the lower half of the formation. Upward, the
nannofossils allow to identify the MNN1a-c Zone, i.e. the
Oligocene / Miocene boundary (Polvano key bed; see also:
PLESI et alii, 2002; BARSELLA et alii, 2009, for the Cortona
area).
The results did not improve the uncertainty of
biostratigraphic signal of the two sampled formations.
However, they have shown that the pelitic intervals of the
calcareous turbidite layers are useful to provide an equallyreliable
biostratigraphic signal, while requiring a significantly
lower number of samples.

Fig. 1 – Lithostratigraphy and biostratigraphy of (A) Macigno (Abetone area) and (B) Mt. Falterona Sandstone (Pratomagno, south western side). The two columns
synthesize the lithology of the two turbidite formations and indicate the stratigraphic position of the collected samples. The gray strip evidences the Oligocene-Miocene
boundary.
REFERENCES
ABBATE E. & BRUNI P. (1989) – Modino-Cervarola o Modino e
Cervarola? Torbiditi oligo-mioceniche ed evoluzione del
margine Nord-appenninico. Mem. Soc. Geol. It., 39, 19-33.
ARUTA G., BRUNI P., BUCCIANTI A., CECCHI M., CIPRIANI N.,
MONTI L., NEBBIAI M., PANDELI E., PAPINI M. & REALE V.
(2004) – Integrated stratigraphic and statistical data as a tool
for mapping perisutural turbidite. In G. Pasquarè and C.
Venturini (eds.) “Mapping Geology in Italy”. Firenze, SELCA.,
213-218.
BARSELLA M., BOSCHERINI A., BOTTI F., MARRONI M.,
MENEGHINI F., MOTTI A., CALANDRI S. & PANDOLFI L. (2009) –
Oligocene-Miocene foredeep deposits in the Lake Trasimeno
area (Central Italy): insights into the evolution of the Northern
Apennines. Ital. J. Geosc., 128, 341-352.
241
FORNACIARI E. & RIO D. (1996) – Latest Oligocene to Early-
Middle Miocene quantitative calcareous nannofossil
biostratigraphy in the Mediterranean region. Micropal., 42, 1-
36.
PLESI G., LUCHETTI L., BOSCHERINI A., BOTTI F., BROZZETTI F.,
BUCEFALO PALLIANI R., DANIELE G., MOTTI A., NOCCHI M. &
RETTORI R. (2002) – The Tuscan successions of the high Tiber
Valley (F. 289 – Città di Castello): biostratigraphic,
petrographic and structural features, regional correlations.
Boll. Soc. Geol. It., Vol. Spec. 1, 425-436.
SESSIONE 9

SESSIONE 9
The volcanic deposits of the new geological map of the Nuoro-Orosei
area (Sardinia, Italy)
___________________
PAOLO CALZIA (*), VINCENZO SALE (*), FILIPPO MUNDULA (**), ANTONIO FUNEDDA (**),
EDOARDO SARRIA (*) & RAFFAELLO CIONI (**) (°)
Key words: Basaltic lava plateau, CARG project, Nuoro-
Orosei.
The new geological map 1:50,000 of the Nuoro and Orosei
sheets, prepared in the framework of the CARG project, is
presented. The area of interest shows the evidence of an intense
volcanic activity during Pliocene, mainly characterized by a
subaerial basaltic lava plateau and by minor deposits of weak
explosive activity, which produced many scoria cones. The
detailed geological survey allowed us to recognize many
eruptive centres sometimes aligned along E-W or N030 and
N060 directions, following the main trend of Oligocene-
Miocene structures, possibly reactivated during Pliocene. This
feature suggests that some of the lava flows are the product of
fissural eruptions, lately evolved into lines of some main
centres of effusion. The thickness of each lava flow varies
between few meters and 20 meters. Many lava flows are
grouped into simple cooling units, evidenced by columnar
jointing cross cutting lava successions, suggesting that many of
the lava flows emissions were concentrated in a short time lapse
. The occurrence of some continental sedimentary deposits
interlayered within the lava flows succession testifies for some
long pauses in the activity, and constitute a marker for the
regional correlations within the lava sequence. A detailed,
stratigraphically controlled sampling in the more than 150 m
thick lava succession in the Cedrino valley and in the Orosei
zone has been carried out, in order to characterize the chemical
evolution and the timing of the volcanic activity.
All volcanic products are classified petrographically as
basalts and three litotypes have been distinguished on the base
(*) Progetto CARG–Sardegna, Cagliari
(**) Dipartimento di Scienze della Terra, Università degli Studi di
Cagliari, mundula@unica.it, rcioni@unica.it
(°) INGV, sezione di Pisa, Italy
Lavoro eseguito nell’ambito del progetto CARG con il contributo
finanziario dell’Università di Cagliari.
242
of phenocrysts assemblage: Ol basalts, Ol and Cpx basalts, and
Ol, Opx and Cpx basalts. Chemical features allow to
discriminate between alkaline and tholeitic products (LUSTRINO
et alii, 2002).
K/Ar whole rock radiometric ages performed by SAVELLI &
PASINI (1973) span from 3.90 Ma (Pedra Dorulas, northern
boundary of the study area) and 2.04 Ma (Cala Gonone, M.
Irveri/Codula Manna, along the Tyrrhenian coastline). New
radiometric data are now in preparation.
REFERENCES
LUSTRINO M., MELLUSO L. & MORRA V. (2002) - The
transition from alkaline to tholeiitic magmas: a case study
from the Orosei-Dorgali Pliocene volcanic district (NE
Sardinia, Italy). Lithos, 63, 83-113.
SAVELLI C. & PASINI G. (1973) - Preliminary results of K-Ar
dating of basalts from Eastern Sardinia and the Gulf of
Orosei (Tyrrhenian Sea). Giornale di Geologia, 39 (1), 303-
312.

The CARG project in Southern Apennines and Sicily: a contribution
for the knowledge of the geological features
_________________________
(*) Dipartimento di Scienze Geologiche, Università di Catania,
carbone@unict.it
SERAFINA CARBONE (*) & FABIO LENTINI (*)
Key words: Apenninic chain, CARG-PROJECT, Ionides,
Sicily, thrust system.
Fiftheen 1:50,000 scale geological maps have been realized
in the Lucanian Apennines and in Sicily. They have been
obtained thanks to decades of field works, enriched with
chronostratigraphical, sedimentological, structural and
geomorphological analyses. These studies have been integrated
with subsurface data. This was fundamental for the
comprehension of the complicate geodynamic evolution of this
area. In the geological maps some orogenic domains and the
foreland-foredeep systems are represented. Moreover the
structural features are well evident. In these maps tectonic
contacts, with different meanings (i.e. main thrust sheets largely
separating different tectonic units, and thrust systems
responsible of breaching of the roof thrust system) have been
distinguished.
In the whole of the southern Apennines – Sicily –
Tyrrhenian system some structural domains can be
distinguished: the foreland domains are represented by two
continental blocks, the Apulian Block to the north and the
Pelagian Block to the south, respectively belonging to the Adria
and to the Africa plates. They are separated since Permo-
Triassic times by the oceanic crust of the Ionian Sea.
The Apenninic-Maghrebian Orogen is located between two
oceanic crusts: the old Ionian crust, at present time subducting
beneath the Calabrian Arc, and the new crust of the opening
Tyrrhenian Sea. The orogenic belt is represented by a
multilayer allochthonous edifice, composed of the Calabride
Chain (CC) tectonically overlying the Apenninic-Maghrebian
Chain (AMC), which in turn overthrust onto the Upper
Miocene and Pliocene top-levels of a deep seated thrust system,
originating by the deformation of the innermost carbonates of
the Foreland Domains (External Thrust System: ETS).
The AMC tectonic units derive from the orogenic transport
during Oligo-Miocene times of sedimentary sequences
deposited in palaeogeographical domains located between the
243
Europe and the Afro-Adriatic plates. These units are composed
of Meso-Cenozoic shallow-water carbonate platforms detached
from the Panormide/Apenninic continental Block, recognizable
by means of seismic lines shot in the Tyrrhenian offshore of
Southern Apennines and Northern Sicily. The Meso-Cenozoic
basinal units, that compose the AMC, belong to two main
groups of sequences, originally located on oceanic crusts
separated by the Panormide/Apenninic Block: the external ones
(Ionides) related to an original basin, belonging to branches of
the Ionian Palaeobasin involved in the orogenesis, and the
internal ones ascribed to the Alpine Tethys (Sicilide Units).
From the geological point of view the Southern Apennines
displays strong analogies with Sicily. In particular the tectonic
units of the AMC are widely exposed in both the areas. The
Lagonegrese Units correspond to the Imerese, Mt. Judica,
Sicanian Units in Sicily. The general name proposed is Ionides.
A well constrained description of the tectono-stratigraphy of
the units, which compose the allochthonous edifice, is given,
and some geological cross-sections are illustrated, with the aim
of reconstructing times and modalities of thrust propagation,
emphasizing indeed the general decoupling of the Tertiary
flysch-type covers, which represents a fundamental character
for interpreting the surface geology.
In fact the peculiarity of the orogenic belt in Southern
Apennines as well as in Sicily mainly lies in a general duplex
geometry. The roof thrust system, several thousand meters
thick, is made up of the allochthonous units of the AMC, while
the floor thrust is represented by the ETS. This latter
corresponds to the so-called “Apulian Chain” of CARBONE &
LENTINI (1990), or to the Apulian Thrust System (FINETTI et
alii, 2005b) in Southern Apennines, and to the Pelagian-
Sicilian Thrust Belt in Sicily (FINETTI et alii, 2005a). It is
composed of more or less rooted carbonate units derived from
the internal edge of the Adria Plate, and of the Africa Plate
respectively.
The description usually should follow the order from the
outermost part of the orogen toward the hinterland and from
bottom to top. This is easy for the Foreland Domains and the
External Thrust System, but it appears more complicated in the
case of the roof thrust system, whose architecture originated
from polyphase tectonics affecting the sedimentary sequences.
The rule that the uppermost structural units should also be the
innermost is not always valid.
SESSIONE 9

SESSIONE 9
Nevertheless the knowledge about the geology of this
orogenic system has much improved and it is now well known
that the tectonic units, that constitute the backbones of the
AMC, are derived from the deformation of palaeogeographic
domains, which differ both in the characteristics of the crustal
areas on which they developed and in their geometry and
relationships with adjacent units and with respect to the
orogenic front.
The biostratigraphical, petrological and structural
constraints, accurately applied, are sufficient to define the
architecture of the orogen and, when confirmed by the
subsurface data, to restore its time-space evolution. In the
Apenninic-Maghrebian thrust belt it is possible to recognise
two oceanic complexes, of which the more external, the Ionian
Meso-Cenozoic basinal sequences, stems from the deformation
of a portion of the Ionian Palaeobasin (Lagonegro, Imerese,
Sicanian, Mt. Judica Units) (FINETTI et alii, 1996, 2005a,
2005b; LENTINI et alii, 2002) and was previously located on the
palaeo-Ionian oceanic crust, together with its own flysch-type
sequences. The innermost basinal deposits, the
Sicilide/Liguride Units, derived from the consumption of the
Alpine Tethys oceanic crust; in Southern Apennines they are
separated by a wide flysch-type cover (Cilento Group) and
largely overthrust to as far as the modern foredeep. The two
complexes are separated from each other by the units derived
from the deformation of the Panormide-Apenninic Platforms.
From the Tortonian onward the evolution of this sector was
linked to the involvement of the deformation front of the
Apulian-Pelagian continental margins, which became
established in a context of thin-skinned tectonics until the
Pliocene.
The terrigenous deposits of the basinal sequences belonging
to the Ionides are represented by Tertiary foreland/foredeep
deposits, whose relationships with the substratum are
occasionally preserved, although large detachments occurred
with further forward transport, which generated repeated slices
with an apparent increase to the original thickness.
In the geological maps of Sicily the allochthonous units of
the Oligo-Miocene Numidian Flysch have been distinguished
from the authocthonous ones. That permits an easier lecture of
the general structural features, because the uppermost nappes
occupy the structural depressions. Moreover the different
flysch-type tectonic units present different density of slides and
that is important for a regional planning.
If the new maps must be useful for the petroleum
researches, it is extremely important to distinguish the same
lithostratigraphical units, belonging to different tectonic units,
because that means that it can be different the structural level in
case of drilling.
REFERENCES
CARBONE S. & LENTINI F. (1990) - Migrazione neogenica del
sistema Catena-Avampaese nell'Appennino meridionale:
244
problematiche paleogeografiche e strutturali. Riv. It. Pal.
Str., 96, 271-296.
FINETTI I., LENTINI F., CARBONE S., CATALANO S. & DEL BEN
A. (1996) - Il sistema Appennino Meridionale-Arco
Calabro-Sicilia nel Mediterraneo Centrale: studio
geologico-geofisico. Boll. Soc. Geol. It., 115, 529-559.
FINETTI I., LENTINI F., CARBONE S., DEL BEN A., DI STEFANO
A., FORLIN E., GUARNIERI P., PIPAN M. & PRIZZON A.
(2005a) – Geological outline of Sicily and lithospheric
tectono-dinamics of its Tyrrhenian Margin from new CROP
seismic data - In: I.R. Finetti (Ed.): “CROP Deep Seismic
exploration of the Mediterranean Region”. Spec. Vol.
Elsevier, chapter 15, 319-376.
FINETTI I., LENTINI F., CARBONE S., DEL BEN A, DI STEFANO
A., GUARNIERI P., PIPAN M. & PRIZZON A. (2005b) –
Crustal tectonostratigraphy and geodynamics of the
Southern Apennines from CROP and other integrating
geophysical data - In: I.R. Finetti (Ed.): “CROP, Deep
Seismic Exploration of the Mediterranean region”. Sp. Vol.
Elsevier, chapter 12, 225-262.
LENTINI F., CARBONE S., DI STEFANO A. & GUARNIERI P.
(2002) - Stratigraphical and structural constraints in the
Lucanian Apennines (southern Italy): tools for
reconstructing the geological evolution. J. Geodyn., 34,
141-158.

Key words: Geodatabase, geological mapping, Regione
Toscana.
INTRODUCTION
The “Regione Toscana Project of Geological Mapping”
aimed to the realization of the geological maps at 1:10,000 scale
for the whole region, ended in the 2005. It has been performed
through the participation of the three Tuscan universities
(Firenze, Pisa and Siena), of the Institute of Geoscience and Earth
Resources-CNR, with the co-ordination of the Regional
Geological Survey. A complete detailed geological coverage for
the whole regional territory has been performed, then integrated
with the creation of a GIS data base and with an on-line
distribution service, managed by the Regione Toscana. To follow,
in the 2009, a Project between the Regione Toscana and the
University of Siena, in the framework of the “Accordo di
Programma Quadro Ricerca e Trasferimento Tecnologico per il
Sistema Produttivo” has been activated. It has been aimed to get
the geological continuum at scale 1:10,000 for the whole regional
territory. The main target of this project, that will be concluded at
the end of the 2010, will be the preparation of a total data base,
characterized by the complete geological congruence, where
every conflicting and/or disomogeneous elements among adjacent
sheets, have to be removed and resolved; such problematics are
unavoidably present in the original maps of the Regione Toscana,
because their realization employed different scientific
organizations.
The CARG Project led by ISPRA-National Geological
Survey, realized 33 sheets at scale 1:50,000 for the Tuscan
_________________________
The contribute of the “Regione Toscana Project of Geological
Mapping” for the realization of geological sheets 1:50.000 scale
LUIGI CARMIGNANI (*), FILIPPO BONCIANI (*), IVAN CALLEGARI (*), PAOLO CONTI (*) (°),
GIANLUCA CORNAMUSINI (*) (°), LAILA GIANNETTI (*), GUIDO LAVORINI (**), GIOVANNI MASSA (*),
FRANCESCO MANETTI (°°), DOMENICO MORINI (**) & ALTAIR PIRRO (*)
(*) Centro di Geotecnologie, Università di Siena, cornamusini@unisi.it
(**) Servizio Geologico Regionale, Regione Toscana
(°) Dipartimento di Scienze della Terra, Università di Siena
(°°) LaMMa, Firenze
245
territory on a total of 61 sheets (at the October 2009). At present,
the map realization in the CARG Project shows a differentiated
state-of-art, with geological 1:50,000 sheets: a) printed or in
printing, b) in preparation for the layout, c) field-mapping ended
or in realization.
This contribute would propose the possibility to print
geological sheets 1:50,000 scale, using the regional geological
data base at 1:10,000 scale, taking in account the state-of-art for
the CARG Project, and starting from the above assumptions of
the Geological Mapping of the Regione Toscana. Analogous
considerations and proposals can be advanced for other near
regions, which have already developed similar projects of
geological mapping at 1:10,000 scale, as Umbria and the Marche.
In particular, the proposed project would concentrate on the
areas lacking of the CARG Project coverage, so to be
complementary with it and to extend the geological coverage at
1:50.000 scale on to the whole regional territories. We propose
the layout and printing of the geological sheets at 1:50,000 scale,
starting from the data base of the regional geological continuum,
using an editorial layout different by that used by the Italian
Geological Survey for the CARG Project, and where Explanatory
Books were also provided. The editorial reference that we
consider has features similar to the 1:50,000 geological sheets
produced by the British Geological Survey, where the maps are
equipped with fundamental elements, as synthetic legend, crosssection
and structural scheme.
Here we show an exemplifying printed map at 1:50,000 scale,
which is the Sheet 332-Scansano (Fig. 1), located in southern
Tuscany, where the grade of coverage of the completed or in
progress CARG sheets is particularly low.
The setting process has provided the preparation of the data
base at scale 1:50,000, beginning from the data base of the
geological continuum at 1:10,000 scale. To follow the respective
print layout has been accompanied and joined with technical and
scientific (of geological-regional character) optimizations.
The print of the Sheet 332-Scansano at 1:50.000 scale should
emphasize the possibility to obtain cheaper and faster, but
extremely accurate and detailed geological maps, which can be
considered as complementary with the CARG maps, starting from
the 1:10,000 scale regional Geological Mapping projects.
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SESSIONE 9
Fig. 1 – Gelogical-structural sketch map of the Sheet 332-Scansano, derived by the elaboration of the 1:10.000 scale maps of the “Regione Toscana Project of
Geological Mapping”.
Furthermore, the selection of the Sheet 332-Scansano as
illustrative map, would also outline the progress of the scientific
knowledge obtained through the Regional Geological Mapping
Project. In fact, such a sheet represents an element of
comparison/update with respect to the Sheet Scansano at scale
1:50,000, produced as a prototypal type by the National
Geological Survey in the 1981.
246

Geothematic regional geodatabases for the compilation of geological
maps in areas of relevant interest: the Coltre of Marecchia Valley
(PU), the Iglesiente region (CA) and the Stazzemese area (LU)
LUIGI CARMIGNANI (*), FILIPPO BONCIANI (*), IVAN CALLEGARI (*), PAOLO CONTI (*) (°),
GIANLUCA CORNAMUSINI (*) (°), LAILA GIANNETTI (*), GIOVANNI MASSA (*), DOMENICO MORINI (**) & ALTAIR PIRRO (*)
Key words: Database, Iglesiente, Marecchia Valley, Stazzemese.
INTRODUCTION
The availability, for some Italian areas, of regional
geothematic databases derived from new field surveys at the scale
1:10,000 and from the fied mapping in the framework of the
CARG Project of the Italian Geological Survey, can now have a
unique and exceptionally efficacious tool to review, following the
interpretation of unpublished details, the geological maps
proposed in the past for specific areas, where the peculiarities
justify the production of dedicated cartography.
In this work we present, as example, the 1:50,000 scale
geological maps of three areas, in different italian regions, of
significant scientific interest: the Marecchia Valley (PU), the
Iglesiente region (CA) and the 1:10,000 map scale for the
Stazzemese area (LU).
The aim is to exploit the potential of geothematic database for
the collection and processing of unpublished geological data, in
any scale and with different intent, and show the easy
management of these data during editing.
THE REGIONAL GEOLOGICAL DATABASES
Many Italian areas shows peculiarities from a geological
perspective.
During the years detailed field investigations and often
conflict interpretations by various authors regard some regions as
“key areas” for the development of some new geological
hypothesis.
Some of this key area are:
_________________________
(*) Centro di Geotecnologie-Università di Siena, geotecnologie@unisi.it
(°) Dipartimento di Scienze della Terra-Università di Siena
(**) Servizio Geologico della Regione Toscana, Firenze
247
- the Val Marecchia area at the Emilia-Romagna – Marche
border;
- The Iglesias area in southwestern Sardinia;
- the Stazzema area in the southeastern Alpi Apuane, in the
northern Apennines.
In the northern Apennines some more very interesting areas
are the Punta Bianca area (near La Spezia), the Bobbio tectonic
windows (between Genoa and Piacenza) and some Neogene
Tertiary basins in Tuscany.
The Regione Toscana Geological Survey completed a
geological map for the whole territory at 1:10,000 scale, based on
new field mapping and on compilations from edited maps. A
geodatabase is produced from such paper maps.
We propose an automatic process to compile 1:50,000 and
1:10,000 geological maps starting from 1:10,000 base maps from
regional mapping projects. The process can led to printed
geological maps of great details (like the Stazzema area) in areas
of complicate tectonic setting and regional maps (like the Val
Marecchia and Iglesias area) in areas with large-scale geological
features.
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SESSIONE 9
Mapping (1:50,000) of a key sector of the northern Appennines and
new results achieved in the frame of the CARG project
Key words: Biostratigraphy, lithostratigraphy, Northern
Apennines, structural analysis.
The realization of the new Geological Map of Italy at
1:50,000 scale (CARG Project) has concluded by now for a large
area of the Northern Apennines extending from Pontremoli to
Pistoia and from Viareggio to Abetone (Fig. 1). According to the
mapped main geological features and the new data achieved
during the realization of six geological sheets (233 Pontremoli,
234 Fivizzano, 249 Massa-Carrara, 250 Castelnuovo di
Garfagnana, 260 Viareggio and 262 Pistoia) and synthesized in
the explanatory notes, the following main results should be
emphasized:
- dating of several formations of the Tuscan Nappe, including
the Toarcian and the Lower Cretaceous black shales, the
onset of the Lower Toarcian marly sedimentation and the
inception of the calcareous sedimentation across the
Jurassic-Cretaceous boundary;
- lithostratigraphy and ages of some incomplete and/or
condensed successions of the Tuscan Nappe Fm.;
- features of litofacies and members of the Scaglia Toscana;
- lithostratigraphy and age of the successions interposed
between the Macigno Fm. and the Arenarie di Monte
Modino Fm.;
- new lithostratigraphic and biostratigraphic frame of the
Canetolo Unit;
- recognition of the Ottone Unit also in the sheets 250 and 262
and of the Canetolo Unit in the sheet 250;
- lithostratigraphy of the Plio-Pleistocene units mapped in the
Pontremoli and Aulla areas (sheet 233), in the Serchio
Valley and in the Lucca-Montecarlo-Vinci area (sheet 250);
- reconstruction of the hydrogeological structures of the
Montecatini Terme thermal area;
- identification and mapping of many landslides which were
formerly unknown;
- mesostructural analysis of mapped tectonic units;
_________________________
LUIGI CARMIGNANI (*), PAOLO CONTI (*), GIACOMO D’AMATO AVANZI (**), GIOVANNI MASSA (*),
NICOLA PERILLI (**) & ALBERTO PUCCINELLI (**)
(*) Centro di Geotecnologie, S. Giovanni Valdarno (AR),
luigi.carmignani@unisi.it
(**) Dipartimento di Scienze della Terra, Pisa, damato@dst.unipi.it
248
- main features of several tectonic depressions, such as the
Magra Valley (sheets 233 and 234), the Serchio Valley
(sheet 250) and the Pistoia plain (sheet 262);
- low angle kilometric normal faults and their role in
exhuming the Alpi Apuane metamorphic core complex;
- the Alpi Apuane folding tectonics and correlation with the
late uplift phases;
- the cataclastic deformation in the basal formations of the
Tuscan Nappe in the area surrounding the Alpi Apuane;
- mesostructural analysis of mapped tectonic units;
- main features of several tectonic depressions, such as the
Magra Valley (sheets 233 and 234), the Serchio Valley
(sheet 250) and the Pistoia plain (sheet 262);
- low angle kilometric normal faults and their role in
exhuming the Alpi Apuane metamorphic core complex;
- the Alpi Apuane folding tectonics and correlation with the
late uplift phases;
- the cataclastic deformation in the basal formations of the
Tuscan Nappe in the area surrounding the Alpi Apuane.
Fig. 1 - Mapped sheets of the study area (Northern Apennines, Italy).

Sheet 273 - Pisa: a database for samples used in structural analyses
Key words: Geological CARtography, Sheet 273- Pisa, structural
samples database.
The Sheet 273 - Pisa, located in the northern sector of the
province of Pisa (northern Tuscany), describes most of the massif
of the Pisani Mounts, wide alluvional deposits of the Arno river
and limitated Pleistocene deposits (Fig. 1).
The Pisani Mounts represent one the deepest roots of the
Northern Apennines originated as the result of the prolonged
interaction between the Adria plane and the Sardo-Corso block.
From east to west and from the bottom to the top, three tectonicunits
can be described: the Monte Serra tectonic unit, the S.
Maria del Giudice tectonic unit and the Tuscan Nappe. The
Monte Serra and S. Maria del Giudice units are characterized by
a thick Triassic silicoclastic succession (Verrucano s.l.) deposited
in discordance on Variscan and post-Variscan successions and
covered by Jurassic-Paleocene successions with a dominant
carbonatic composition. They are affected by a Greenschist facies
metamorphism. The outcrops of Tuscan Nappe are few and
limited to the southern and western margins of the massif.
The tectonic units are divided by E-verging thrusts and
recorded a polyphase deformation history with three main
different deformation phases (D1-D3) that show a systematic
change in the structural elements orientations moving from east to
west (CAROSI et alii, 1997). After the continental collision and
the crustal thickening phase (D1 deformation phase), the tectonic
units have been affected by a compressive deformation phase
documented mainly at cartographic scale (phase D2). The D2
structures were subsequently deformed and exhumed during an
extensional coaxial regime (phase D3) active during the postcollisional
stage (CAROSI et alii, 1997).
During the field work in the Pisani Mounts massif, c. 100
oriented samples have been collected for microstructural and
petrographical analyses in key structural sites in the three tectonic
units.
_________________________
(*) Dipartimento di Scienze della Terra, Università di Pisa,
carosi@dst.unipi.it
RODOLFO CAROSI (*), CHIARA FRASSI (*), CHIARA MONTOMOLI (*),
DANIELE NANNINI (*) & PIERO CARLO PERTUSATI (*)
249
Fig. 1- Location of the Sheet 273- Pisa
Each thin section has been described following an exhaustive
scheme that includes the description of meso and microscopic
structures, metamorphic mineral association, folds geometry and
folding mechanisms and type of foliations. In this way we
characterized at the microscopic scale, the structural elements
associated to different deformation phases.
To insert inside the classical geological database used in the
CARG project, the microstructural information collected during
laboratory and field work, we proposed a first simple and friendly
database focused exclusively on samples used in structural
analysis.
In this way, we first localized each sample according to its
geographical coordinates (at the 25,000 scale) and then we
compiled a descriptive table that univocally identified each
sample joined to 4 external tables.
The descriptive table (Fig. 2) gives information about the
name and the geographic location of the sample, the type of
structures present in the thin section (e.g. S2 foliation, F2 fold)
and analogously to the database proposed for stratigraphic
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SESSIONE 9
samples (see AA.VV., 1997), descriptive fields (max 200 words)
compiled with information about macroscopic and microscopic
features (as for example, the geometry of fold and foliation and
the mineral association) collected during meso and microscopic
analyses.
Field name Date Type Descrizione campi
NUM_CAM Short integer Nnumero progressivo
SIG_CAM Text Sigla campione
ANNO Short integer Anno campionamento
UBI Text Localizzazione
ES_PIEG Text Struttura mesoscopica: piega
ES_FOL Text Struttura mesoscopica:
foliaziome
CAR_MAC Text (200words) Caratteri macroscopici
CAR_MICR Text (200words) Caratteri microscopici
GEOM_PIEG Text (200words) Geometria piega
OSS_FOL Text (200words) Caratteristiche foliazione
ASS_MIN Text (200words) Associazione mineralogica
UC_LEGE External table Formazione o membro
UN_TETT External table Unità tettonica
NOM_PETR External table Nome petrografico
PROT External table protolite
Fig. 2- Descriptive table proposed to the structural sample database.
At the end, we linked each sample to external tables
illustrating: the belonging tectonic unit, the petrographic name of
the analyzed sample, the member or formation where it has been
collected (external link to table T0180802000) and the rock
protolith.
The result is that consulting the database, it will be easy to
localize in the map folds and/or foliations developed during the
different deformation phases, or, making join and queries,
highlight a single structural element recorded in a particular
formation and/or member inside the different tectonic units.
REFERENCES
AA.VV. Quaderno 6 - Serie III 8 (1997) - Carta Geologica
d’Italia - 1:50.000 Banca Dati Geologici. Roma
CAROSI R., CERBAI N. & MONTOMOLI C. (1997) - Deformation
history of the Verrucano of Pisani Mounts (Northern
Apennines, Italy). Ann. Tecton., 9, 55-75.
250

Integrated stratigraphy of the middle – upper Miocene deposits of
San Bartolomeo Formation, cropping out whithin the geological
map n.405 Campobasso (Molise, Ssouthern Italy)
Key words: Calcareous plankton biostratigraphy, Middle and
Late Miocene, San Bartolomeo Formation, Souther
Apennines.
The San Bartolomeo Formation was established by
CROSTELLA &VEZZANI (1964), and consists of about 1000 m
thick siliciclastic and turbiditic sedimentary succession, which
lies in angular unconformity over the Sannio Unit (PATACCA &
SCANDONE, 2007).
As far as the age, this formation has been controversially
considered Serravallian –Tortonian (CROSTELLA & VEZZANI,
1964), Serravallian (TORTORICI, 1975), Langhian – Tortonian
(PESCATORE, 1971; DAZZARO et alii, 1988), latemost
Tortonian?/early Messinian (PATACCA & SCANDONE, 2007).
Moreover the tectono-sedimentary environment of these deposits
is also questionable considered: foredeep basin (COCCO et alii,
1972), piggy-back basin (Dazzaro et alii, 1988; DI NOCERA et
alii, 1988; PATACCA et alii, 1990), thrust- related basin (BOIANO,
2000), thrust-top or wedge –top basin (PESCATORE et alii,1996;
PESCATORE et alii, 2000) and thrust –sheet-top basin (PATACCA
&SCANDONE, 2007).
The deposits of San Bartolomeo Formation widely outcrop in
the center-eastern part of the geological map N. 405,
Campobasso, of the National Geological Map Series of Italy (at
scale 1:50,000). In this area the studied formation consists of a
succession, about 600 m thick, of siliciclastic and turbiditic
sediments composed by three main lithofacies: a) arenaceous and
/or arenaceous-conglomerate; b) pelitic-arenaceous; and c)
pelitic.
The age of the investigated sediments was established on the
basis of integrated calcareous plankton biostratigraphy
(calcareous nannofossils and planktonic foraminifera).
_________________________
ANTONIO CASCELLA (*), FABRIZIO LIRER (**), MASSIMO CESARANO (°) & GERARDO PAPPONE (°°)
(*) Istituto Nazionale di Geofisica e Vulcanologia, Pisa, cascella@pi.ingv.it
(**) Istituto per l’Ambiente Marino Costiero (IAMC)-CNR,
fabrizio.lirer@iamc.cnr.it
(°) Università del Molise, massimo.cesarano@libero.it
(°°) Università di Napoli “Parthenope”, gerardo.pappone@unipathenope.it
251
A total of 164 samples were collected for biostratigraphic
studies, with a sample resolution of 50 centimetres to 2 m, along
seven stratigraphical sections, logged and measured between
Casalciprano village, at North, and Baranello village at South.
The analyses of calcareous nannofossil and planktonic
foraminiferal assemblages were performed following the
procedures extensively used in Mediterranean and extra-
Mediterranean biostratigraphic studies (DI STEFANO et alii, 2008,
and references therein), and the zonal assignment followed the
biostratigraphic schemes of SPROVIERI et alii (2002) and DI
STEFANO et alii (2008).
Based on the integrated biostratigraphic study the San
Bartolomeo Formation, cropping out in Campobasso area,
encompasses the early Serravallian - middle/late? Tortonian
stratigraphic interval, between the calcareous nannofossil zones
MNN6a and MNN8/MNN9, and the planktonic foraminiferal
zones MMi5 through MMi11.
The biostratigraphic results presented and the detailed field
observations carried out for mapping the Campobasso geological
map, would suggest a reassessment of the San Bartolomeo
Formation chronostratigraphy, the Sannio Unit paleogeographic
position, and the tectono-sedimentary evolution of the Southern
Apennines during the Serravallian age.
REFERENCES
BOIANO U. (2000) – Anatomy of a siliciclastic turbidite basin:
the Gorgoglione Flysch, Upper Miocene, southern Italy:
physical stratigraphy, sedimentology and sequencestratigraphic
framework. Sediment. Geol., 107 (3-4), 231-
262.
CROSTELLA A. & VEZZANI L. (1964) - La geologia
dell'Appennino foggiano. Boll. Soc. Geol. It., 83, 121-142.
COCCO E., CRAVERO E., ORTOLANI F., PESCATORE T., RUSSO M.,
TORRE M. & COPPOLA L. (1972) - Le Unità Irpine a Nord di
Monte Marzano (Italia Meridionale). Mem. Soc. Geol. It., 13,
607-654.
DAZZARO L., DI NOCERA S., PESCATORE T. & RAPISARDI L.
(1988) - Geologia del margine della catena appenninica fra
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il F. Fortore e il T. Calaggio (Monti della Daunìa, Appennino
meridionale). Mem. Soc. Geol. It., 41, 410-422.
DI NOCERA S., PAGANO C., RUSSO B. & TORRE M. (1988) –
Successioni del bacino irpino nei dintorni di Celenza
Valfortore (Appennino Dauno). Mem. Soc. Geol. Ital., 41,
423-430.
DI STEFANO A., FORESI L. M., LIRER F., IACCARINO S. M., TURCO
E., AMORE F. O., MAZZEI R., MORABITO S., SALVATORINI G.
& ABDUL AZIZ H., (2008) - Calcareous plankton high
resolution bio-magnetostratigraphy for the Langhian of the
Mediterranean area. Riv. Ital. Paleontol. Strat., 114, v1, .51-
76.
PATACCA E., SARTORI R. & SCANDONE P. (1990) - Tyrrhenian
basin and apenninic arcs: kinematic relations since late
Tortonian times. Mem. Soc. Geol. It, 45, 425-451.
PATACCA E. & SCANDONE P. (2007) – Geology of the Southern
Apennines. Boll. Soc. Geol. It. Special Issue , 7 , 75-120.
PESCATORE T. (1971) — Considerazioni sulla sedimentazione
miocenica nell' Appennino campano-lucano. Atti. Acc.
Pontaniana, 20, 17 p.
PESCATORE T.S., PINTO F., RENDA P., SENATORE M.R.,
TRAMUTOLI M., VALENTE A. (1996) - Avanfosse mioceniche
dell’Appennino meridionale (Italia). Rend. Acc. Sc. Fis. Mat.,
63, 85-121.
PESCATORE T.S., DI NOCERA S., MATANO F. & PINTO F. (2000) –
L’Unità del Fortore nel quadro della geologia del settore
orientale dei Monti del Sannio (Appennino meridionale).
Boll. Soc. Geol. It., 119, 587-601.
SPROVIERI R., BONOMO S., CARUSO A., DI STEFANO A., DI
STEFANO E., FORESI L.M., IACCARINO S., LIRER F., MAZZEI R.
& SALVATORINI G. (2002) - An integrated calcareous
plankton biostratigraphic scheme and biochronology of the
Mediterranean Middle Miocene. Riv. Ital. Paleontol. S., 108,
337-353.
TORTORICI L. (1975) - Osservazioni geologiche sul Flysch di San
Bartolomeo nell'area compresa tra il Fiume Trigno e
Benevento (Italia meridionale). Boll. Soc. Geol. It., 94, 1791-
1809.
252

Calcareous nannofossil biohorizons of late Paleocene-middle Eocene
in the Mt. Penice Flysch (Northern Apennines, Italy)
Key words: Biostratigraphy, calcareous nannofossils, Late
Paleocene-Middle Eocene, Northern Apennines.
The nannofossil biostratigraphy of the Mt. Penice Flysch is
here presented. The section exposed along the Bobbio-Ceci road
in the Mt. Penice area has a thickness of 250 meters and is
composed by alternation of marly calcareous turbidites, thick to
very thick limestone and mudstone with middle to fine grain
arenites and calcarenites at the bottom. The lower part of the
section is characterized by turbiditic layers of siliciclastic
mudstone and arenites and rare layers of free calcite emipelagites.
The Mt. Penice Flysch was referred to the Canetolo Unit of
the Subligurian Domain by ELTER et alii (1964), PLESI (1974;
1975), MONTANARI &ROSSI (1982). Recently it has been referred
to the Esternal Ligurian Domain, on the basis of the unit age and
its involvement in the mesoalpine phase (CATANZARITI et alii,
2002).
The detailed biostratigraphic study of the Mt. Penice Flysch
performed during the realization of the CARG Project for the
1:20,000 scale Geological Map of Italy, allowed the identification
of some useful nannofossil events that could improve the
biostratigrafic resolution of the late Paleocene-middle Eocene in
the Northern Apennines.
In fact the sedimentary successions of the Northern Apennines
contain nannofossil sensitive to the etching and dissolution during
sediments deposition and diagenesis, so that some marker species
are missing or only sporadically present.
In the studied material are poorly represented some groups as
the genus Tribrachiatus and the genus Discoaster on the basis of
which are defined the Eocene biozones in the zonal schemes of
MARTINI (1971) and OKADA &BUKRY (1980). But then have
been recognized new biohorizons, some of which recently
observed also in Italy (AGNINI et alii, 2006; AGNINI et alii,
2007a; DALLANAVE et alii, 2009) and in some Atlantic and
Pacific Ocean sites (RAFFI et alii, 2005; AGNINI et alii, 2007b;
RAFFI et alii, 2009).
The bioevents turned out to be very useful to improve the
resolution of Paleocene-Eocene boundary and early Eocenemiddle
Eocene time interval, in the Northern Apennines are:
Sharp decrease of the genus Fasciculithus, related to the
________________
(*) Istituto di Geoscienze e Georisorse, CNR, Pisa, catanzariti@igg.cnr.it
(**) Dipartimento Scienze della Terra, Università di Pisa, perilli@dst.unipi.it
RITA CATANZARITI (*) & NICOLA PERILLI (**)
253
lower part of CP8b Subzone.
Concomitant Occurrence of Rhomboaster cuspis and
Discoaster araneus related to the PETM (Paleocene-Eocene
Thermal Maximum) and the CIE (Carbon Isotope Excursion)
that are used to approximate the Paleocene-Eocene boundary
(AUBRY et alii, 2007).
Highest occurrence of Fasciculithus tympaniformis.
Lowest occurrence of Sphenolithus radians related to the
upper part of CP9a Subzone and NP10 Zone.
Lowest occurrence of Noelhaerabdaceae represented by the
genera Dictyococcites, Cyclicargolithus and Reticulofenestra,
coincident with the lowest occurrence of Ericsonia formosa,
Dicoaster lodoensis, Discoaster kuepperi and the highest
occurrence of the genus Toweius. All these events seem gathering
around the NP11-NP12 zonal boundary and the particular
concomitance of these events can testify one hiatus or too large
sampling.
Lowest occurrence of Coccolithus crassus, marker of CP11
Zone.
Lowest occurrence of Reticulofenestra dictyoda, related to the
lower part of CP11 Zone.
Lowest occurrence of Discoaster sublodoensis, marker of the
NP14 Zone.
Lowest occurrence of Nannotetrina sp., useful marker to
define the NP14- NP15 zonal boundary in poorly preserved
material (PERCH-NIELSEN, 1985).
Some of these events are very useful because established on
taxa resistant to dissolution and recognizable even in etching
material.
On the basis of these events, correlable with standard
zonations, we can date accurately scattered samples and
impoverished assemblages. In addiction we can correlate, more
accurately, different geological settings, and detect how global
events, as climate and sea-level changes, affected the
sedimentation in the Northern Apennines successions.
Moreover we can evaluate the sediment accumulation rate of
such deposits.
SESSIONE 9

SESSIONE 9
REFERENCES
AGNINI C., MUTTONI G., KENT D.V. & RIO D. (2006) - Eocene
biostratigraphy and magnetic stratigraphy from Possagno,
Italy: The calcareous nannofossil response to climate
variability. Eart. Planet. Sci. Lett., 241, 815- 830.
AGNINI C., FORNACIARI E., RAFFI I., RIO D., TATEO F., BACKMAN
J. & GUSBERTI L. (2007a) - Responses of calcareous
nannofossil assemblages, mineralogy and geochemistry to the
environmental perturbations across the Paleocene/Eocene
boundary in the Venetian Pre-Alps. Mar. Micropaleontol. 63,
19-38.
AGNINI C., FORNACIARI E., RAFFI I., RIO D., RÖHL U. &
WESTERHOLD T. (2007b) - High-resolution nannofossil
biochronology of middle Paleocene to early Eocene at ODP
Site 1262: implications for calcareous nannoplankton
evolution. Mar. Micropaleontol, 64, 215-248.
AUBRY M.-P., OUDA K., DUPUIS C., BERGGREN W.A. & VAN
COUVERING J.A., Members of the Working Group on the
Paleocene/Eocene Boundary, (2007). The Global Standard
Stratotype-section and Point (GSSP) for the base of the
Eocene Series in theDababiya section (Egypt). Episodes, 30
(4), 271–286.
CATANZARITI R., OTTRIA G. & CERRINA FERONI A. (2002) -
Tavole stratigrafiche della Carta geologico-strutturale
dell’Appennino emiliano-romagnolo in scala 1:250.000.
SELCA, Firenze.
DALLANAVE E., AGNINI C., MUTTONI G. & RIO D. (2009) -
Magneto-biostratigraphy of the Cicogna section (Italy):
implications for the late Paleocene-early Eocene time scale.
Earth Planet. Sci. Lett., 285, 39-51.
ELTER P., GRATZIU C. & LABESSE B. (1964) - Sul significato
dell'esistenza di una unità alloctona costituita da formazioni
terziarie nell'Appennino settentrionale. Boll. Soc. Geol. It.,
83 (2), 373-394.
RAFFI I., BACKMAN J. & PÄLIKE H. (2005) - Changes in
calcareous nannofossil assemblage across the
Paleocene/Eocene transition from the paleo-equatorial
Pacific Ocean. Palaeogeogr. Palaeocl., 226, 93–126.
RAFFI I., BACKMAN J., ZACHOS J. C. & SLUIJSET A. (2009) - The
response of calcareous nannofossil assemblages to the
Paleocene Eocene Thermal Maximum at the Walvis Ridge in
the South Atlantic. Mar. Micropaleontol., 70, 201–212.
MARTINI E. (1971) - Standard tertiary and quaternary
nannoplankton zonation. Proceedings II planktonic
conference, Roma, 2, 739-785.
254
MONTANARI L. & ROSSI M. (1983) - Evoluzione delle unità
stratigrafico-strutturali del Nord Appennino: 2. Macigno s.s.
e Pseudomacigno. Mem Soc. Geol. It., 25 , 185-217.
OKADA H. & BUKRY D. (1980) - Supplementary modification
and introduction of code numbers to the low-latitude
coccolith biostratigraphic zonation (Bukry, 1973; 1975).
Mar. Micropaleontol, 5, (3), 321-325.
PERCH-NIELSEN K. (1985) - Cenozoic calcareous nannofossils.
In: H-M.Bolli, J.B. Saunders and Perch-Nielsen K. (Eds.),
Plankton Stratigraphy, Cambridge University Press, 427-554.
PLESI G. (1974) - L’Unità di Canetolo nella struttura di Bobbio
(Val Trebbia), Montegroppo (Val Gotra) e lungo la
trasversale Cinque Terre-Pracchiola. Atti Soc. Tosc. Sci.
Nat., Mem., Serie A, 81, 121-151.
PLESI G. (1975) - La nappe de Canetolo. Bul. Soc. Géol. de
France, 6, 979-983.

Calcareous nannofossil distribution pattern and nannobiohorizons
from Upper Cretaceous sedimentary successions
of northern Apennines (Italy)
Key words: Calcareous nannofossils, Biostratigraphy, Late
Cretaceous, Northern Apennines, Italy.
During the realization of the Geological Map of Italy
(1:100.000 scale), foraminifera allowed to date, for the first time,
many calcareous to siliciclastic successions and to improve old
dating based on invertebrates. Consequently foraminifera were a
fundamental tool to constrain the sedimentary evolution of many
lithostratigraphic units. Unfortunately, the assigned ages of
mapped units were frequently based on scattered sampling,
sometimes represented only by few samples, and the
micropaleontological data were usually based on the
discontinuous occurrence of a limited number of taxa, frequently
not including zonal markers. Furthermore, the generic inferred
age was extended to the entire unit.
In the last two decades calcareous nannofossils have allowed
to deeply improve the dating of Meso-Cenozoic sedimentary
successions first of all because the fossil record is rich, but also
because the obtained ages were based on the succession of
assemblages which were frequently characterized by the presence
of zonal markers. The continuous and abundant calcareous
nannofossil record allows to recognize the succession of
nannobiohorizons which are helpful to identify zones or zone
boundaries and hence useful for dating stratigraphic boundaries
or sedimentary events (such as the onset or the end of the
orogenesis controlled sedimentation). Consequently this fossil
group deeply contributed to improve the dating of many
lithostratigraphic units (formations, members, or even key beds),
to highlight the tectono-sedimentary evolution of large sectors of
the Italian mountain chains and to constrain the geodynamic
evolution of Apennine thrust-fold belt.
In examples, after the first effort to date the Upper Cretaceous
deposits of the Northern Apennines and to constrain the
orogenesis-controlled sedimentation based on calcareous
nannofossils (MARRONI et alii, 1992), many papers have been
published on the Upper Cretaceous siliciclastic to marly
____________________
(*) Istituto di Geoscienze e Georisorse, Pisa, catanzariti@igg.cnr.it
(**) Dipartimento di Scienze della Terra, Università degli Studi di;
perilli@dst.unipi.it
RITA CATANZARITI (*) & NICOLA PERILLI (**)
255
calcareous successions of the Northern Apennines which allowed
to refine the ages of many Helmintoid Flysch Units and of some
basal complexes (VESCOVI et alii, 1999; CATANZARITI &PERILLI,
2006; CATANZARITI et alii, 2007). In many of these papers
quantitative or semiquantitative range charts are furnished and the
recognized assemblages reported. Moreover, huge amount of
quantitative and semiquantitative biostratigraphic data have been
also achieved during the realization of the Italian Geological Map
at 1:50,000 scale (CARG Project).
Aim of this paper is to reconstruct the distribution patterns of
the Late Cretaceous calcareous nannofossil taxa, to describe the
recognized zones and to discuss the reliability of the
nannobiohorizons utilized, based on the published and
unpublished data sets. The unpublished data set is based on the
results achieved by the authors of this paper, during the
realization of the geological sheets at 1:50.00 scale of the CARG
Project: Bobbio, Neviano degli Arduini, Bargagli, Cabella
Ligure, Pontremoli, Fivizzano and Castelnuovo Garfagnana
(CARG Project).
REFERENCES
CATANZARITI R. & PERILLI N. (2006) – Age of the Ottone Unit in
the Zignago area (External Ligurian Units, Northern
Apennines): constrains from calcareous nannofossils.
Ofioliti, 31, 11-24.
CATANZARITI R., ELLERO A, LEVI N., OTTRIA G. & PANDOLFI L.
(2007) – Calcareous Nannofossil biostratigraphy of the
Antola Unit succession (Northern Apennines, Italy): new age
constraints for the Upper Cretaceous Helminthoid Flysch.
Cretaceous Research, 28, 841-860.
MARRONI M., MONECHI S., PERILLI N., PRINCIPI G. & TREVES B.
(1992) - Late Cretaceous flysch deposits of the Northern
Apennines, Italy: age of inception of orogenesis-controlled
sedimentation. Cretaceous Research, 13, 487-504.
VESCOVI P., FORNACIARI E., RIO D. & VALLONI R. (1999) - The
Basal Complex Stratigraphy of the Helminthoid M. Cassio
Flysch: a key to the Eoalpine Tectonics of the Northern
Apennines. Riv. It. Paleont. Strat., 105, 101-128.
SESSIONE 9

SESSIONE 9
The Atlas of biostratigraphic data.
A necessary integration to the 1:10000 geological map of Tuscany
ANDREA CERRINA FERONI (*), ERNESTO ABBATE (**), ANNA MARIA BAMBINI (°), ALESSANDRO BOSSIO (°°), RITA
CATANZARITI (*), SIMONE DA PRATO (*), ALESSANDRO ELLERO (*), LUCA FORESI (°), ANTONIO LAZZAROTTO (°),
MICHELE MARRONI (°°), GIULIO MASETTI (*), GIUSEPPE NIRTA (**), SILVIA PALANDRI (°°), LUCA PANDOLFI (°),
GIANFRANCO PRINCIPI (**), VIVIANA REALE (**) & BERNARDO ZANCHI (^)
Key words: Biostratigraphy, chronostratigraphy, Tuscany.
The project for the 1:10 000 scale geological map of Tuscany,
just completed, has greatly increased the knowledge of the
geology of region, recording an appreciable involvement effort
from the scientific community (University and CNR).
The substantial funds furnished by the regional geological
survey have been invested in the new mapping field work and
geological data computerization. The choice to favour the
spreading of data digitization has prevent to supply resources to
the laboratory researches, complementary to the field work, but
penalized also by the short time of the Project. We underline the
biostratigraphic researches useful to age the geological units,
composed of widespread sedimentary rocks extending over 200
million years.
This Atlas of biostratigraphic data has been performed a
posteriori by the three universities and the CNR, still involved in
the geological mapping of the Tuscan region, with the little
economic budget offered by the Regional Geological Survey, and
has the aim to present and comment the framework of the
biostratigraphic and chronostratigraphic data of the stratigraphic
units outcropping in Tuscany.
The Atlas offers, with tables (Figs. 1, 2, 3 for an example)
and topics, the presentation and the critic analysis of the available
biostratigraphic data on the six major geological sets that
constitute the upper structural levels of the structural built.
_________________________
(*) CNR - IGG Consiglio Nazionale delle Ricerche, Istituto di Geoscienze e
Georisorse di Pisa, cerrina@igg.cnr.it
(**) Dipartimento di Scienze della Terra, Università degli Studi di Firenze
(°) Dipartimento di Scienze della Terra, Università degli Studi di Siena
(°°) Dipartimento di Scienze della Terra, Università degli Studi di Pisa
(^) Laboratorio di monitoraggio e modellistica ambientale per lo sviluppo
sostenibile, LaMMa
256
Fig. 1 – Geographic distribution of foredeep succession and location of
stratigraphic sections.

Fig. 2 – Biostratigraphy and chronostratigraphy of the foredeep sections of the northern sector of Tuscany, and space-temporal distribution of foredeep
sandstones. The location of the sections is reported in Fig.1.
Fig. 3 – Biostratigraphy and chronostratigraphy of the foredeep sections of the northern sector of Tuscany, and space-temporal distribution of foredeep
sandstones. The location of the sections is reported in Fig.1.
257
SESSIONE 9

SESSIONE 9
The outlook for the geological map in Italy, from “paper” to “digital”
Key words: CARG Project, database system, geological map.
For the geological map of Italy, the switch from traditional
printed version to digital format constitutes a technological
milestone that ushers in a radical and irreversible change in the
process of acquisition, representation and popularization of
geological data, the importance of which is perhaps not yet fully
appreciated.
In over a century of activity, the national geological
community, comprising the Italian geological survey, universities
and research institutes, has cyclically collaborated to update its
geological knowledge of the national territory by taking part in a
new cartography project designed to replace the existing product,
rendered obsolete by advances made by geological sciences in
terms of expertise and methodology.
Since the end of the 1800s, there have been three Geological
Map Projects in Italy, the first two of which were to scale
1:100,000 while the third, the CARG Project currently underway,
is to scale 1:50,000. If we were to define this cyclical trend in
basic terms, we could identify distinct periods of activity
followed by periods of inactivity lasting approximately thirty
years. The most recent period of activity, still in progress,
benefits from the overlapping, on a national operational level, of
more detailed regional geological cartography projects to scale
1:10.000. Thus it appears we can establish the “shelf life” of the
geological map to be in the region of thirty years, after which, at
least until now, a replacement is called for.
On the scientific front, in keeping with the past, the last phase
produced new geological solutions underpinned by more up-todate
and objective information. Moreover, on the technological
front, this time signalling a break with the past, also it heralded a
veritable ‘revolution’ with the introduction of digital formats and
databases.
Digital formats counter the rigidity of traditional printed
formats with an extremely ductile structure, actually replacing
geological maps with a flexible database system that avoids
_________________________
(*) CNR – Istituto di Geoscienze e Georisorse, Pisa, cerrina@igg.cnr.it
(**) Regione Emilia Romagna, Servizio Geologico Sismico e dei Suoli,
gdaniele@regione.emilia-romagna.it
ANDREA CERRINA FERONI (*) & RAFFAELE PIGNONE (**)
258
solutions based on ongoing modifications, integrations and
updates. As a result, there will be an end to the two-phase cycle
that has until now governed national geological map projects.
The termination of CARG will therefore signal the end of an
entire approach, and a new operational context will be established
following processing of geological data. Within this new context
the concept of replacing the geological map is itself replaced by
the new concept of maintenance: a progressive, ongoing activity
of correcting and improving rather than intervening periodically
in a ‘drastic’ manner.
This technological revolution has many consequences and
within the specific area of interest dealt with here, they are all of
some significance.
The concept of maintenance implies gradual, ongoing action
and is effective on both the scientific and economic fronts. On a
scientific level, this is achieved through the independent review
of n themes (sectors or topics) which require updating, with the
opportunity to effect maintenance upstream, constantly
recomposing the framework by integrating the modified data into
databases. On an economic level, the financial investment is
absorbed over a prolonged period as opposed to huge investments
having to be made periodically.
In this new landscape envisaged for the future of the
geological map, which for the geological community retains the
same scientific importance as always, the end of the CARG
project constitutes a serious blow, not only because it means
scientific content will not be updated but also, and perhaps above
all, because it has been decided not to grant across-the-board
access to an essential tool, the geological database, which will be
of vital importance in the future for the application of geological
data acquisition and transmission procedures and therefore for
safeguarding the quality of what is a strategic product for
geological culture and environmental policy.
We can only hope that at every level of responsibility, the
public administration will devote due thought and consideration
to the potential offered by new technologies in relation to the
geological map.

Key words: Dent Blanche, Norian foraminifers, Roisan
dolostones, Western Alps.
Relatively well preserved remnants of Triassic fossils have
been discovered within two dolomitic bodies of the Roisan zone
during field and laboratory refinements of the Foglio Monte
Cervino (070) of the Carta Geologica d’Italia at 1:50.000 scale
(CARG Project). The Roisan zone is a metamorphic, strongly
transposed and fragmented sedimentary unit of supposed
Mesozoic age, mainly carbonatic, which is discontinuously
exposed along the ductile shear zone which separates the Dent
Blanche and Mont Mary basement nappes (upper Austroalpine
outliers, Aosta Valley-southern Valais).
The Roisan zone is generally interpreted as the former
sedimentary cover of the pre-Triassic lower- to upper crust Mont
Mary basement, but its primary substratum can not be precisely
established due to the pervasive tectonic contact between them.
This metasedimentary unit extends from the Roisan village, north
of Aosta, to the Mont Blanc du Creton (Valtournenche), through
the Col de St. Barthélemy, Grand Pays, Cima Bianca (biggest
body) and Becca di Salè-Saleron area; isolated minor slices
reappears in the P. Cors eastern spur, Hörnly ridge of the
Matterhorn, and left slope of Zmutt valley, within the NE
extension of the Mont Mary nappe. It is also recorded in the
Pillonet klippe.
The Dent Blanche and Mont Mary nappes groups two main
pre-Triassic basement units: i) the Valpelline unit, a slice of
Variscan lower crust consisting of granulite to amphibolite facies
felsic and mafic rocks; ii) the underlying Arolla unit, consisting
of Permian granitoid and gabbro protoliths. These basement units
are poorly to pervasively reworked by the polyphase Alpine
metamorphism which is documented by relics of a relative high-P
imprint, intermediate between epidote-blueschist and
glaucophane-bearing greenschist facies conditions of Late
Cretaceous age (75-73 Ma in the Pillonet klippe), and by a
greenschist facies regional overprint at decreasing pressure.
_________________________
Late Triassic microfossils in the Roisan zone, Austroalpine
Dent Blanche-Mont Mary nappe system, NW-Alps
GLORIA CIARAPICA (*), GIORGIO VITTORIO DAL PIAZ (**) & LEONSEVERO PASSERI (*)
(*) Dipartimento di Scienze della Terra, Università di Perugia,
ciarapic@unipg.it
(**) Accademia delle Scienze di Torino.
259
Remnants of a Mesozoic metasedimentary cover are also
preserved in the Dent Blanche nappe (Mt. Dolin area), over the
frontal part of the Arolla unit. These mainly consist of Triassic
dolostones and thick sedimentary breccias of supposed Jurassic
age, including pebbles of dolostones with Late Triassic forams. If
the Dolin and Roisan metasedimentary units are compared, facies
differences prevail over analogy.
Focusing on the the Roisan zone, this unit is characterized by
the occurrence of various types of dolostones, marbles and
ophiolite-free calcschists which are intimately associated with
grey-greenisch and dark mylonites coming from cover and
basement protoliths. The primary features of these metasediments
are generally effaced by the tectono-metamorphic
overprint, with the exception of a few occurrences where the
deposition environment can be reconstructed with good
confidence. Some dolostones are referable to a shallow-water
carbonate platform (Mt. Grand Pays) for the presence of thick
beds with stromatolites, green algae, erosional surfaces and
angular breccias; others (Comba de Chavacour - Tzan Lake)
show features better referable to a basinal environment as thin
bedding, with thin levels of chert-derived quartzites and thick
doloruditic beds. Dolostones are associated to tabular pure
marbles, marbles with mm-cm bands of detritic quartz and to
ophiolite-free calcschists. Any contact among these lithofacies is
transposed by polyphase ductile shear and rootless folding:
although the general concordance could often simulate a primary
succession, the internal structural setting of the Roisan zone
prevents any attempt from reconstructing the stratigraphic
sequence. Only in some relatively less deformed zones, as the
Comba di Saleron and below the Oratorio di Cuney (St.
Barthélemyt valley), this succession can be recognized from
bottom to top: a) regularly bedded dolostone and dolomitic
marble, with 1-1.5 m-thick beds (50-60 m ca); b) dolomitic
marble and massive dolostones, with disarmonic basal contact
(50 m ca); c) tabular grey marbles; d) marbles with thin bands of
detritic quartz (4-5 m).
If this succession really corresponds to the original
stratigraphic order, this scenario can be envisaged: i) Middle (?)-
Upper Triassic shallow- and deep-water dolostones; ii) Rhaetian-
Lower Jurassic tabular and quartz-bearing marbles; iii) Middle
Jurassic to Upper Cretaceous calcschists.
If this succession is reversed, marble with quartz might be
referred to the Carnian and shallow water dolostones to the
SESSIONE 9

SESSIONE 9
Norian by comparison with Southern Alps and Northern
Apennines sequences with Carnian siliciclastic deposits and
Norian platform-carbonates
No traces of silici-clastic meta-sediments, like the classic
occurrences of generally accepted Permian-Eotriassic age from
the Briançonnais and Pancherot-Cime Bianche cover units, have
been found in the entire Roisan zone (the metamorphic
conglomerates mapped in the central Roisan zone, are cataclastic
to mylonitic augengneiss of the Arolla unit). Therefore, the
Roisan series can not be older than the Middle Triassic. On the
top, the ophiolite-free calcschists mark the transition from preorogenic
(impure marble and carbonate-rich calcschist) to synorogenic
conditions (terrigenous calcschist): their age may be
bracketed between the Middle Jurassic and the early Late
Cretaceous by comparison with the Piedmont zone and
considering the constraint provided by the relatively high-P
imprint in the Pillonet basement (75-73 Ma) closely associated to
Roisan-type impure marbles. Lastly, to the Roisan zone is
generally referred also the unique occurrence of very finely
banded Fe-Mn-quartzite discovered inside the folded Arolla
gneiss NW of Cignana lake, even if a Piedmont pertinence can
not be excluded due to facies affinity. Recent dating of allanite
grains provided Permian (around 280 Ma) and more realistic
Early to Middle Jurassic ages (190-160 Ma).
The Late Triassic age of part of the Roisan zone is
documented by the Mt. Grand Pays dolostones. Their best
outcrops are on the divide between Comba Deche and Alpe
Chaleby, and on its eastern slope, over the new Alpe Leche.
GRAND PAYS DOLOSTONES AND FOSSILS
Major sedimentary features are thick bedding (1 m) often with
massive breccias. In the dolomitic beds stromatolitic levels are
evident, associated to massive intervals. Thin levels of
sedimentary breccias lying on erosional surfaces are made of
angular to sub-rounded clasts in a fine-grained matrix. All the
Fig. 1 – Stromatolites and breccias in the dolostones
260
features remind carbonate platform dolostones. At the field
observation the textures appear mainly as grainstone-packstone or
mudstone, but in thin section they are mostly a mosaic of finecrystalline
dolomite. One fortunately well preserved sample
provided a rich association of foraminifers that, although
metamorphism, can be referred to a Late Triassic age, in
particular to the Norian. The best preserved forms are Aulotortus
friedli, A. ex gr. sinuosus, Gandinella falsofriedli, Aulotortus
tenuis, A. communis and Glomospirella spp.
This association can be referred to a generic Late Triassic
age, but the presence of A. friedli and the absence of
Lamelliconus spp. and A. praegaschei let us to exclude a Carnian
age; on the other hand, the size of the forams and the absence of
Triasina hantkeni and Auloconus permodiscoides exclude the socalled
Rhaetian.
Fig. 2 – 1) Aulotortus friedli, 2) A. ex gr. sinuosus, 3-4) Gandinella falsofriedli
Dasycladalean algae were also found, observed only at the
surface. They are comparable to Heterosporella conradii in the
Norian Dolomia Principale of the eastern Southalpine (Mt.
Pramaggiore, Friuli).
In conclusion, this association is referred to the middle part
of the Late Triassic (Norian), the same age inferred from the
fossils found in Mt. Dolin.
We hope that new samples will be able to better define the
exact age of the Grand Pays bedded dolostones, but we think that
these first fossils found in the Italian part of the Dent Blanche-
Mont Marie nappe system represent a new step in the knowledge
of the Western Alps history.

The siliciclastic turbidite units of the Mt. Civitella – Mt. Elmo area
(Mt. Amiata, south-eastern Tuscany): geological setting,
petrographic composition and regional correlations
Key words: Modal analysis, Mt. Amiata area, Northern
Apennines, siliciclastic turbidites, Sub-Ligurian Domain,
Tertiary.
The morphological and structural high of the Mt. Amiata area
is well-known for its geological features consisting in: a) a
structural pile made up of Ligurid and Sub-Ligurid Units
overlying the non metamorphic Tuscan Succession (Falda
Toscana, locally affected by important tectonic elisions i.e. the
so-called “Serie Ridotta”) which in its turn lies onto the Devonian
to Triassic rocks of the Tuscan Metamorphic Units; b) the
presence of surrounding continental to marine, Late Miocene-
Pliocene structural basins (e.g. the Radicofani, Cinigiano-
Baccinello and Velona basins); c) the Quaternary Mt.Amiata
volcano; d) the geothermal fields and Hg mining areas. In this
frame, the Mt.Civitella-Mt.Elmo ridge is a part of a complex
megafold constuted by the non metamorphic Tuscan Succession
(from the Calcare e marne a Rhaetavicula Contorta Formation to
the Brolio Shales and Sugame Marl Members of the Scaglia
Toscana) which is tectonically overlie by the Ligurids (Santa
Fiora and Pietraforte Formations of the S.Fiora Unit) and the
Sub-Ligurian Unit (Canetolo Unit).
Moreover, a complex of turbidite mainly calcarenitic and
siliciclastic rocks of debated stratigraphic attribution are present
between the Tuscan terrains and the overlying Ligurian and Sub-
Ligurian Units. In fact, these rocks were generally assigned in the
geological literature or to the Scaglia Toscana pp. and Macigno
Formation of the Tuscan Nappe or to the Canetolo Unit. Our
research have affected a part of the ridge between. A 1:10,000
scale geological mapping and structural survey were performed in
the Selvena, Castell’Azzara and Mt. Elmo areas and 20
siliciclastic arenite samples were collected for modal analysis
using the Gazzi-Dickinson method and Cipriani recording
method.
The geological survey evidences that a varicoloured shaly -
calcareous unit, including greenish, paesina-like calcilutite with
____________________
(*) Dipartimento di Scienze della Terra, Università di Firenze,
pandeli@geo.unifi.it
(** ) IGG (Istituto di Geoscienze e Georisorse) - CNR - Firenze
NICOLA CIPRIANI (*), MORENO PACINI (*) & ENRICO PANDELI (**)
261
sporadic siliciclastic arenites and dolomitic calclithite, rests on
the Scaglia toscana and vertically passes into a succession of
siliciclastic turbidites (arenite sandstone unit). Finally, a mainly
calcarenitic unit tectonically overlies both the varicoloured shaly
-calcareous unit and the arenite sandstones unit.
The modal analyses (see Figs. 1 and 2) show that the arenite
sandstones have a modal arkosic composition, but they are very
different from the siliciclastic turbidites of the Macigno
Formation, but also from the Monte Senario Sandstone (Canetolo
Unit) and from the arenites of the Ligurian Domain (i.e. the
Gottero Sandstone, the Monghidoro Sandstone, the Pietraforte
sandstone and the Ghiaieto sandstone of the Elba Flysch) and of
the Montenero Member interbedded into the Marnoso-Arenacea
Formation in Val Tiberina area.
So, tacking into account the quite variable composition of the
clastic imputs in the different areas of the outcrops of the
Canetolo Unit, we correlate the succession of the varicoloured
shaly -calcareous unit, the arenite sandstones unit and the
calcarenitic unit to the Sub-Ligurian Domain. From a structural
point of view, the rocks of the calcarenitic unit and of the Tuscan
Nappe are affected by the same folding events, but the orientation
of the axes and the axial planes in the two tectonic unit appear
different. Several, sometimes overturned mesofolds deformed the
rocks of the Tuscan Nappe with a Adriatic vergence.
These structures can be interpreted as parasitic folds of a
overturned mega-anticline similar to that of the Mt. Cetona front.
The new tectonic sketch of the studied area is shown in Fig. 3 and
consists of the piling up of three tectonic units (from top to
bottom of the structural pile): Santa Fiora Unit (Ligurids),
Canetolo Unit (or Sub-Ligurian Unit) and the Tuscan Nappe.
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Fig. 1 – QFL+C DIAGRAM.
Fig. 2 – Q/Q+F VS. Qmr/Qm diagram
262
Fig. 3 – Tectonic sketch of the studied area

Key words: Eruptive units, geologic map, lithosome, UBSU,
volcanic units, volcano-stratigraphy, volcanic facies.
INTRODUCTION
The generation of a geologic map of a volcanic region is an
essential starting point from which to base the knowledge for
detailed volcanological and magmatological researches and is
fundamental to understand the volcanic activity and its impact on
the environment and human life. During the last 20 years, the
Volcano Geology has experienced a great impulse in Italy and
has become an independent kind of research, making use of
several tools, as stratigraphy, geologic mapping, structural
geology, geomorphology, petrography, geochemistry, and
physical volcanology. Indeed, several geologic maps of Italian
volcanoes have been produced within the CARG Project.
Different and innovative methods were applied to the Volcano
Geology, producing national and international scientific debates.
In this presentation, we are summarizing the results occurred
during the GEOITALIA 2009 session and the ISPRA 2009
Workshop that were focused on the comparison of different
methodologies, on the discussion of open problems, and on the
evaluation of future works and perspectives of innovative tools of
analysis.
The volcano stratigraphic tools span from the classical
geologic (stratigraphic, sedimentologic, mapping), physical
volcanologic (structural, textural, compositional, physical),
geochronologic (tephrachronologic, archaeomagnetic,
radiometric), and petro-chemical methods. Moreover, several
examples of recent studies on both effusive and explosive
volcanism demonstrate the powerful tools of integrated and
multidisciplinary approach in defining the volcanic history of
active and ancient volcanoes.
_________________________
Mapping Volcanoes: Tools, results and perspectives
DONATELLA DE RITA (*), GIANLUCA GROPPELLI (**) & LUIGINA VEZZOLI (°)
(*) Università di Roma3, Dipartimento di Scienze Geologiche,
derita@uniroma3.it
(**) CNR, Istituto per la Dinamica dei Processi Ambientali,
gianluca.groppelli@unimi.it
(°) Università dell’Insubria, Dipartimento di Scienze Chimiche e
Ambientali, luigina.vezzoli@uninsubria.it
263
GEOLOGIC MAPS AND STRATIGRAPHIC
CRITERIA
The main topics of the stratigraphic study and geologic
mapping of a volcanic region are summarized as following:
Stratigraphic methodology.
Use of lithostratigraphic units as main criterion during survey
and mapping.
Application of UBSU, temporal and spatial scale.
UBSU and their relations with the geodynamics framework.
UBSU and their relations with the eustatic changes.
Lithosomes: applications and open problems.
Facies variations.
Use of eruptive units for recent volcanics.
Stratigraphy
The geologic mapping of several Italian volcanoes is the
result of the combination of three different categories of
stratigraphic units: lithostratigraphic, synthemic and lithosomatic.
Each category of the stratigraphic framework is based on the
proper definition following the guidelines of the International
Stratigraphic Guide and of the Italian Geological Survey.
Lithostratigraphic units represent the main stratigraphic rules
used for the identification of the units during the field surveys and
can be in different ranks from the formation to member and to
single lava flow.
Synthemic units are represented by the Unconformity
Bounded Stratigraphic Units (UBSU) that are useful to synthesize
the geological history of a volcano. For example, the
unconformities are represented by angular discordances related to
the shifting of the volcano feeding system and by erosion surfaces
in the periphery of the volcano edifice. UBSUs were used to
group the lithostratigraphic units identified during fieldwork and
to reconstruct the volcanic evolution.
Lithosome is a morpho-stratigraphic term that in volcanic
terrains encloses the concept of “volcanic edifice”. Lithosomatic
units are adopted in order to better represent the spatial
organization of the different eruptive centers recognized on the
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basis of their geometric arrangement, lithology and morphology.
UBSU application
UBSUs are separated by discontinuities in the stratigraphic
successions, which emphasise the major breaks in the evolution
of the volcano and its spatial and temporal geometry. The survey
and mapping experience on several volcanoes, as Vulture and
Etna, have shown that UBSUs are applicable at all type of
volcanoes. This approach greatly improves level of detail and
highlights changes in the eruptive styles and the strong tectonic
control on the localisation of the volcanic centres through time.
Moreover, UBSUs allow to done clearness and importance to
geology, as the fundamental data set to support petrographic and
geochemical interpretations. These stratigraphic units are very
useful to compare and correlate in time and space distributions of
the volcanic activity products with deposits and environments of
other origin.
CONCLUSIONS
The innovative stratigraphic use of UBSUs methodology in
the Italian volcanic areas has improved the knowledge of volcano
geology and evolution and has permitted the integration of
information coming from different earth science fields to produce
a regional volcanic and non-volcanic geologic framework. The
lithostratigraphic units embracing volcanic facies associations are
the main tools for field survey and mapping of volcanic products.
The use of lithosome has to be cautiously. The use of eruptive
units is better appropriate to thematic maps than to geologic
maps.
264

Key words: Regional geology, Lucania, Southern Apennines.
The Sheet n°470 "Potenza" falls in the central Lucania sector
of the Southern Apennines thrust belt, characterized by very
complex tectonic and stratigraphic features (CARBONE et alii,
1991; MAZZOLI et alii, 2001; MENARDI NOGUERA &REA, 2000;
PESCATORE et alii, 1988; 1999).
In the central Lucania area, Late Triassic to Middle Miocene
basin successions and middle-late Miocene to Pliocene foreland
clastic successions crop out. Four main tectonic units have been
distinguished: the Monte Arioso, Groppa d'Anzi, Vaglio
Basilicata and San Chirico units, which are strongly deformed
and thrusted eastward upon the buried internal Apulian Platform
or Apulian thrust system (MOSTARDINI & MERLINI, 1986;
LENTINI et alii, 1990; ROURE et alii, 1991).
The tectonic units are formed by successions characterized by
basinal and shelf-margin facies (Serie calcareo-silico-marnosa
Auct.), ranging in age from Middle Triassic to Early Miocene,
and by basinal mainly calcareous-pelitic deposits of the Argille
Variegate Group, conformably followed by numidian
quartzarenites and Serra Palazzo arenites. All the basinal deposits
are referred to an external basinal domain (Lagonegro basin)
(MOSTARDINI &MERLINI, 1986; PESCATORE et alii, 1988, 1992;
ROURE et alii, 1991). After OGNIBEN (1969) and CARBONE et alii
(1988) the Argille Variegate Group cropping out in the Lucanian
Apennines belongs to tectonic units of internal derivation
(Liguridi/Sicilidi Units).
In the westernmost areas, the successions are characterized by
frequent occurrence of coarse to fine calciclastic deposits settled
by dense gravity flows and slumps coming from a carbonate
platform margin. The geometry of the sedimentary bodies, the
palaeocurrent directions, and the grain size distribution of the
redeposited limestones suggest that the carbonate input came
from a western sectors. These deposits form the internal (i.e.
_________________________
New geological data in central Lucania, Southern Apennines: the
Geological Sheet n° 470 “Potenza”
(*) Dipartimento di Scienze della Terra, Università di Napoli “Federico II”,
sildinoc@unina.it; matano@unina.it
(°) Dipartimento di Studi Geologici e Ambientali, Università del Sannio,
pescatore@unisannio.it
This work was carried out within the CARG Project.
SILVIO DI NOCERA (*), FABIO MATANO (*) & TULLIO PESCATORE (°)
265
western) margin of the Lagonegro basin and have been ascribed
to the Monte Arioso Unit (PESCATORE et alii, 1988).
The successions cropping out in the central zone are typically
composed of pelagic sediments (varicoloured clays and shales)
interlayered with fine carbonate turbidites representing more
distal facies of the coarser proximal facies described above.
Therefore, these units (Argille Variegate Group) record
sedimentation along the axial zone of the Lagonegro basin. These
deposits are ascribed to the Groppa d’Anzi Unit (PESCATORE et
alii, 1988). The facies pattern and its persistence during the basin
evolution indicate that the Lagonegro palaeogeographic domain
had to be bounded by carbonate platforms on both sides.
The successions outcropping in the easternmost areas only
consist of middle Cretaceous to middle Miocene formations
(PESCATORE et alii, 1988; GALLICCHIO et alii, 1996). They show
facies similar to those observed in the western sectors although,
in this case, the calciclastic input came from the eastern sectors.
These successions, forming the Vaglio Basilicata and San Chirico
units (Campomaggiore Unit, sensu PESCATORE et alii, 1988), are
mainly ascribed to Flysch Rosso and Numidian Flysch
formations.
The Numidian Flysch and other correlated upper Oligocene to
lower Miocene successions conformably overlie the uppermost
Lagonegro basinal units, i.e. Flysch Rosso, Argille Varicolori and
Corleto Perticara formations. In particular, siliciclastic,
volcaniclastic and calciclastic deposits with frequent
intercalations of carbonate megabreccias and calcareous
olistoliths coming from neritic environments (Paola Doce
Formation, after PESCATORE et alii, 1992, upper Oligocene–
lower Miocene in age) conformably overlie the Lagonegro
successions. The Paola Doce Formation laterally passes into the
‘Tufiti di Tusa’ (OGNIBEN, 1969), mainly formed by siliciclastic
and volcaniclastic sediments with frequent intercalations of
carbonate turbidites. Both Paola Doce and Tufiti di Tusa
formations grade into the overlying Numidian quartzarenites
(Langhian). In the northwestern sectors the Numidian sandstone
conformably overlies the marls, clays and shales of the
Lagonegro basin (‘Flysch Rosso’ and ‘Argille Varicolori’).
Siliciclastic and calciclastic deposits (Serra Palazzo Fm),
conformably lying on the Langhian Numidian quartzarenites,
outcrop along the easternmost belt (San Chirico unit).
Palaeocurrent directions and other sedimentological features
suggest a western provenance for the siliciclastic input, whereas
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calciclastic material was supplied by the eastern Apulian
platform. The depositional environment of the Serra Palazzo Fm,
was the foredeep basin located between the Langhian–Tortonian
thrust belt to the west and the not deformed Apulian platform to
the east. After the Langhian, the contractional tectonics involved
the whole western platform and the Numidian basin (PESCATORE
et alii, 1992); Early Miocene palaeogeography was then strongly
modified.
The tectonic units are unconformably overlaid by middle-late
Miocene terrigenous flysch deposits (Gorgoglione Flysch) and
Pliocene unconformity bounded marine to alluvial units (Ariano
Irpino Supersynthem).
The Gorgoglione Flysch is formed by sequences made up of
deep-sea conglomerates, sandstones and pelites unconformably
lying on the Lagonegro and Numidian units. These deposits
contain a mixture of clasts resulting from erosion of the
Apenninic carbonate platform, Lagonegro pelagic units and
crystalline nappes.
In the Early-Middle Pliocene (Ariano Supersynthem) new
wedge-top depozone basins develop along the new chain margin,
representing the palaeo-Adriatic Sea western border. The
Pliocene wedge-top deposits are formed by alluvial, lagoonal,
coastal marine and shelf marine mainly clastic successions up to
about 1.500 m thick. They lie with a regional unconformity on
several tectonic units of the orogenic wedge.
Two major synthems have been recognised in the Ariano
Supersynthem. The lower one (Tricarico Synthem) has an Early
Pliocene age and is about 100 m thick; the upper one (Tolve
Synthem) is Middle-Late Pliocene in age (biozones MPl4b -
MPl5b) and is up to 1.300 m thick; both are characterised by
mainly transgressive basal facies and thick regressive top facies.
The sedimentary, palaeoenvironmental and palaeogeographic
Pliocene evolution has been strongly influenced by the coeval
tectonic evolution of the chain. In compressional orogenic
systems, such as the Southern Apennines, tectonic activity can
largely overprint the effects of eustatic sea-level fluctuations, so
that significant changes in the relative sea level can be mostly
produced by flexural subsidence plus thrust activity.
The tectonic units of the central Lucanian Apennines show a
very complicated structural style characterised by strong lateral
variability of map-scale structures; further, this sector is widely
affected by Plio-Quaternary strike–slip and extensional faults
mainly oriented according to N120±10°, N150±10° and N50±20°
trends. Yet, excluding the brittle deformation due to Quaternary
faulting, the complexity of structural styles seems to result from
the Pliocene refolding of more ancient structures produced by
middle-late Miocene deformation.
266
REFERENCES
CARBONE S., CATALANO S., LAZZARI S., LENTINI F. & MONACO
C. (1991) - Presentazione della Carta Geologica del Bacino
del Fiume Agri (Basilicata). Mem. Soc. Geol. It., 47, 129 -
143.
GALLICCHIO S., MARCUCCI M., PIERI P., PREMOLI SILVA I.,
SABATO L. & SALVINI G. (1996) - Stratigraphical data from a
Cretaceous claystones sequence of the "Argille Varicolori" in
the southern Apennines (Basilicata, Italy). Paleopelagos, 6,
261-272.
LENTINI F., CARBONE S., CATALANO S. & MONACO C. (1990) -
Tettonica a thrust neogenica nella catena appenninicomaghrebide:
esempi dalla Lucania e dalla Sicilia. Studi Geol.
Camerti, vol. suppl. 1990, 19-26.
MAZZOLI S., BARKHAM S., CELLO G., GAMBINI R., MATTIONI L.,
SHINER P. & TONDI E. (2001) - Reconstruction of continental
margin architecture deformed by the contraction of the
Lagonegro Basin, southern Apennines, Italy. J.Geol. Soc.,
158, (2), 309-319.
MENARDI NOGUERA A. & REA G. (2000) - Deep structure of the
Campanian–Lucanian Arc (Southern Apennine, Italy).
Tectonophysics, 324, 239–265.
MOSTARDINI F. & MERLINI S. (1986) - Appennino centro
meridionale. Sezioni geologiche e proposta di modello
strutturale. Mem. Soc. Geol. It., 35, 177-202.
OGNIBEN L. (1969) - Schema introduttivo alla geologia del
confine calabro-lucano. Mem. Soc. Geol. It., 8, 453-763.
PESCATORE T., RENDA P. & TRAMUTOLI M. (1988) - Rapporti tra
le Unità lagonegresi e l’Unità sicilide nella media valle del
Basento. Mem. Soc. Geol. It., 41, 353-361.
PESCATORE T., RENDA P. & TRAMUTOLI M. (1992) - "Tufiti di
Tusa" e flysch Numidico nella Lucania centrale (Appennino
meridionale). Rend. Acc. Sci. Fis. Matem. Soc. Naz. Sci. Lett.
Art. Napoli, 59, 57-72.
PESCATORE T., RENDA P., SCHIATTARELLA M. & TRAMUTOLI M.
(1999) - Stratigraphic and structural relationships between
Meso-Cenozoic Lagonegro basin and coeval carbonate
platforms in southern Apennines, Italy. Tectonophysics, 315,
269–286.
ROURE F., CASERO P. & VIALLY R. (1991) - Growth processes
and melange formation in the southern Apennines
accretionary wedge. Earth Planet. Sc. Lett., 102, 395-412.

Three-dimensional reconstruction of the main unconformities of the
Colli Albani stratigraphy and deposit volume calculations
GIUSEPPE DIANO (*) , ANDREA BONAMICO (**), ARNALDO ANGELO DE BENEDETTI (*) & GUIDO GIORDANO (*)
Key words: Colli Albani, volcanism, Roman Magmatic Province,
hazard
INTRODUCTION
The quiescent Colli Albani volcano is composed of
overlapping edifices, with each showing changes in volcanic style
over the 600 ka history of the volcanic field. The edifices and
changes in eruption style through time are indicated in the field
by the major unconformities, which have been identified from
surface geology and borehole stratigraphies. This reconstruction
of the major unconformities allows for 3D geometric
reconstruction of relevant rock packages, the computation of the
deposit volumes, and the evaluation of syn-volcanic tectonic or
volcano-tectonic activity. Furthermore, some rock packages, such
as the Pisolitic Tuffs, the Tufo Lionato and the Albano maar
deposits, are characterised by relative low permeability and are
therefore essential for the modelling of the hydrogeological
circulation and flow of volcanic gases. The reconstructions of the
isopachs of the three main caldera forming ignimbrites erupted
between 460 and 355 ka have allowed us to calculate their
minimum preserved extra-caldera volumes at 59 km 3 (Pozzolane
Rosse), 20 km 3 (Pozzolane Nere) and 30 km 3 (Villa Senni Fm.)
respectively. The total volume of volcanic deposits erupted after
the last caldera collapse (< 355 ka) is calculated at 34.7 km 3 . The
preserved deposits of the most recent Albano polygenetic maar
have been calculated at 0.9 km 3 .
The total minimum deposit volume of the Colli Albani
volcano is 208.1 km 3 . This volume does not include the
intracaldera ignimbrite volumes which may add some 80 km 3 to
the total volume.
THE COLLI ALBANI VOLCANO HISTORY
The 3D modelling of geological surfaces allows for the
_____________________
(*) Dipartimento di Scienze Geologiche, Università degli Studi di RomaTre
giordano@uniroma3.it
(**) Parco Regionale dell’Appia Antica, Roma
267
geometric reconstruction of relevant rock packages, important for
the understanding of geological processes and for several other
applications. In volcanic environments, the main unconformities
and volcano-tectonic structures are the most important features
that can be reconstructed by means of surface and subsurface
data.
The Colli Albani (central Italy) is a quiescent volcano located
to the southeast of the capital city Roma (GIORDANO et alii,
2010). The increasing presence of human activities and
settlements into the hinterland of Roma includes the Colli Albani
resulting in an increased “human pressure” on the volcanic
environment. In the last two decades an increasing local
population has resulted in a dramatic increase of ground-water
withdrawal from drill-holes for civil and industrial purposes,
resulting in a significant depletion of the ground-water resource
(cf. MAZZA & CAPELLI 2010). Similarly, several areas with
intense gas emissions are presently urbanised, posing a major
hazard to the local inhabitants derived both by direct exposure to
volcanic gas (mainly CO2 and H2S) and by the occurrence of gas
outbursts from shallow high pressure pockets intercepted during
drillings (see CARAPEZZA et alii, 2010).
In order to identify areas of potential accumulation of gas at
shallow depth, GIORDANO et alii, (2006) performed a study
funded by the Italian Civil Defence to reconstruct the 3D
geometry of relevant stratigraphic packages. This was done by
integrating surface geology data and sub-surface stratigraphies
made available, especially during the last decades, by the drilling
of several thousands of boreholes for civil purposes.
Here we will present the computer based reconstruction of the
bases of the main ignimbrites at Colli Albani and of packages of
volcanic rocks which may be relatively impervious to gas
perculation. This reconstruction also allows the determination of
the paleo-topographic evolution of the volcano and to calculate
the precise volume of the preserved deposits for each of the
volcanic intervals analysed.
REFERENCES
CARAPEZZA M.L, BARBERI F., TARCHINI L., RANALDI M. & RICCI
T. (2010) - Volcanic hazard of Colli Albani. In: R. Funiciello
and G. Giordano (Eds) The Colli Albani Volcano. Special
Publication of IAVCEI, 3. The Geological Society, London.
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CARAPEZZA, M.L, LELLI, M. & TARCHINI, L. (2010) -
Geochemistry of the Albano crater lake. In: R. Funiciello and
G. Giordano (Eds) The Colli Albani Volcano. Special
Publication of IAVCEI, 3. The Geological Society, London.
GIORDANO G., MATTEI M. & FUNICIELLO R. (2010) - Geological
map of the Colli Albani volcano. In: R. Funiciello and G.
Giordano (Eds) The Colli Albani Volcano. Special
Publication of IAVCEI, 3. The Geological Society, London.
Insert.
MAZZA R. & CAPELLI G. (2010) - Hydrogeology of the Colli
Albani volcano. In: R. Funiciello and G. Giordano (Eds) The
Colli Albani Volcano. Special Publication of IAVCEI, 3. The
Geological Society, London.
TODESCO, M. & GIORDANO, G. (2010) - Modelling of CO2
circulation in the Colli Albani area. In: R. Funiciello and G.
Giordano (Eds) The Colli Albani Volcano. Special
Publication of IAVCEI, 3. The Geological Society, London.
268

The activities of CNR IGG in CARG project: maps, databases and
IT to improve geological data quality
GIANFRANCO FIORASO (*), ANDREA IRACE (*) , PIETRO MOSCA (*), FABRIZIO PIANA (*), SERGIO TALLONE (*),
LAURA BELLINO (*), STEFANIA TRENKWALDER (*) & DARIO VARRONE (*)
Key words: Geographic Information Systems, geological
mapping, Information and Communication Technology,
Piemonte.
The geological mapping is one of the main activity of the
CNR – IGG, Institute of Geoscience and Earth Resources in
Torino since 1995, when it was involved in the National Program
for the new Digital Geological Map of Italy at 1:50,000 scale
(CARG Project), funded by the former Italian Geological Service
(now ISPRA) and Regione Piemonte (now ARPA Piemonte).
This activity, that lasted until now without significant breaks
and has been conducted in collaboration with the Department of
Earth Science of Torino University, led to the publication of 5
sheet (132 Bardonecchia, 157 Trino, 156 Torino Est, 155 Torino
Ovest, 211 Dego) while other 3 sheets (Cesana T.se, Aosta and
Acqui Terme) are concluded and near to be published. Fifteen
years of experience on this subject allow to considerate that the
survey of the new digital geological maps can represents an
effective chance to:
- widen the basic geological data sets and improve the quality
of research methodologies;
- sustain basic researches and allow young researcher to
complete their formative path;
- acquire visibility and reliability to the regional Public
Administrations. This allowed involvement in geo-environmental
studies and planning actions, as well as in joint participation in
scientific international programs. Geo-thematic maps have been
often realized in this context on the basis of CARG geological
maps;
- developing original competences on use of Information and
Communication Technology (ICT) for representation and
dissemination of geological data and knowledge.
A list of the main result achieved by CNR IGG working group
in the last fourteen years will be briefly described, especially as
regard the positive influence of having larger available data base
and good reliability.
Particular stress will be given here in describing the
alphabetization processes followed by CNR IGG working group
_______________________
CNR - Istituto di Geoscienze e Georisorse, Torino, f.piana@csg.to.cnr.it
269
on the Geo-Informatics languages, approaches and technologies,
developed in parallel with the compilation of CARG Data Model.
Since the importance of data organization and data web-sharing is
now widely recognized, the use of ICT in the Earth Science
domain of knowledge is strongly needed when large GIS data sets
are to be managed. The on-going ICT innovation has an
important impact on geological mapping activity, since it give
origin to new conceptual and methodological perspectives about
storing, representing and sharing geological information.
In this sense, the CNR IGG working group is pursuing new
conceptual and operative ways to get the geographic descriptive
standard more suitable to the representation of geological map
data. This because digital geological maps consists of a mixing of
primary (on-field) data and interpretation subject to former
modification during the secondary working steps such as
conceptual map elaboration and editing.
It can be argued that a future development of National
Geological Mapping programs would be possible only in the
frame of a wide application of ICT, not much for the data
acquisition steps (where the basic knowledge and skills of the
field geologist are still preponderant over the technological
aspects) but for the representation and dissemination of
knowledge in order to get it more usable for society.
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Biostratigraphy results within the Italian Geological Mapping
CARG Project
ANDREA FIORENTINO (*), MARIA CRISTINA GIOVAGNOLI (*), RITA MARIA PICHEZZI (*) & MARIAGRAZIA ROSSI (*)
Key words: Biostratigraphy, CARG Project, foraminifera,
nannofossils.
The start of the Italian Geological Mapping CARG Project
represented a unique chance to perform biostratigraphic studies
over the entire territory of the country. Paleontological analyses
have been carried out on several lithostratigraphic units cropping
out in the surveyed areas. Some formations had never been
studied by a paleontological point of view in the past and the
CARG Project offered an opportunity to verify the presence of
any fossil content.
Biostratigraphy has been focused mainly on the
micropaleontological assemblages, especially on planktonic
foraminifera and nannofossil. However, analyses considered also
benthonic foraminifera, conodonts, calcareous algae, pollens and
ostracods. Most of the analyses have been carried out on thin
sections, smear slides and dry residue of washed samples.
Macropaleontological analyses have often been performed on
calcareous successions of carbonate shelf, whereas ammonites
and other fossils have received lesser attention.
Data provided by biostratigraphy played a fundamental role in
determining the age of the lithostratigraphic units and sometimes
the dating of tectonic events.
Such a widespread and conspicuous amount of
micropaleontological analyses also allowed to test the
applicability of the existing biostratigraphic schemes. It turned
out that some of the zonations elaborated in the '70s are still valid
and that peculiar zonations established for the Mediterranean are
particularly suitable for the Italian biostratigraphy.
In many cases, foram and nanno zonations, which have not
been formally established, have been correlated to standard biochronostratigraphical
references, such as that of BERGGREN et alii
(1995), in order to link them to the time scale.
Analyses based on nannofossils have been extraordinarily
common, probably because of several reasons: they are cheap,
easy to prepare and for many formations it was the first time they
_________________________
(*) ISPRA, Servizio Geologico d’Italia, Dipartimento Difesa del Suolo,
andrea.fiorentino@isprambiente.it
270
were performed. Many zonal schemes referring to different time
intervals exist in the literature. For the Jurassic BRALOWER et alii
(1989) was mostly applied together with the Thetis scheme by
MATTIOLI & ERBA (1999), whereas for the Cretaceous the
zonation by SISSINGH (1977) was generally adopted; for the
Tertiary, the zones by MARTINI (1971) were preferred, with the
further Mediterranean subdivisions elaborated for the Oligocene
by CATANZARITI et alii (1997) and for the Oligocene-Miocene
interval by FORNACIARI &RIO (1996) and FORNACIARI et alii
(1996). For the Plio-Pleistocene the Mediterranean scheme by
RIO et alii (1990) was adopted.
For planktonic foraminifera, micropaleontologists referred
mainly to the different Chapters of the Plankton Stratigraphy
(BOLLI et alii, 1985) and to PREMOLI SILVA &SLITER (1995). The
most cited paper is that of IACCARINO (1985) which presents the
planktic foram zonation for the Mio-Pliocene in the
Mediterranean. However, the paper by SPROVIERI et alii (2002)
was commonly cited in addition to the former. Sometimes
references to previous papers, dating to the '60s and the '70s,
were made.
The Plankton Stratigraphy (BOLLI et alii, 1985) was also cited
in many cases for correlations, comparisons and additional details
concerning both forams and nannos as well as for the Chapter on
tintinnids.
For the carbonate platform successions, two publications were
basically used as references: DE CASTRO (1991), which was
generally adopted for the southern Apennines, and CHIOCCHINI et
alii (1994), which was eventually integrated with more recent
updates. They take into account mainly microfossil assemblages
with benthonic foraminifera and calcareous algae, but also
include macrofossils such as rudists. Regarding Tertiary
macroforaminifera, reference was made to the paper by SERRA-
KIEL et alii (1998).
REFERENCES
BERGGREN W.A., KENT D. V., SWISHER C.III & AUBRY M.P.
(1995) - A revised Cenozoic geochronology and
chronostratigraphy. In W.A. Berggren, D.V. Kent, M.P.
Aubry and J. Hardenbol (eds) - Geochronology, Time Scales
and Global Stratigraphy Correlations. SEPM Spec. Publ. 54,
129-212.

BOLLI H., SAUNDERS J. B. & PERCH-NIELSEN K. (1985) -
Plankton Stratigraphy. Cambridge University Press.
BRALOWER T.J., MONECHI S. & THIERSTEIN H.R. (1989) –
Calcareous Nannofossil zonation of the Jurassic-Cretaceous
Boundary interval and correlation with Geomagnetic Time
Scale. Mar. Micropaleont., 14, 153-235.
CATANZARITI R., RIO D. & MARTELLI L. (1997) – Late Eocene to
Oligocene Calcareous Nannofossil Biostratigraphy in
Northern Apennines: the Ranzano Sandstones. Mem. Sci.
Geol., 49, 207-253.
CHIOCCHINI M., FARINACCI A., MANCINELLI A., MOLINARI V&
POTETTI M. (1994) – Biostratigrafia a foraminiferi,
dasicladali e calpionelle delle successioni carbonatiche
mesozoiche dell’Appennino Centrale (Italia). Studi Geologici
Camerti Vol. Spec. 1994, 9-129.
DE CASTRO P. (1991) - Mesozoic. In F. Barattolo, P. De Castro
and M. Parente - Field Trip Guide-book of the 5th
International Symposium on Fossil algae: Capri, 7-12 april
1991, 21-44.
FORNACIARI E., DI STEFANO A., RIO D. & NEGRI A. (1996) –
Middle Miocene quantitative calcareous nannofossil
biostratigraphy in the Mediterranean region.
Micropaleontology, 42, 37-63.
FORNACIARI E. & RIO D. (1996) – Latest Oligocene to Early
Miocene Quantitative Calcareous Nannofossil
Biostratigraphy in the Mediterranean Region.
Micropaleontology, 42, 1-36.
IACCARINO S. (1985) – Mediterranean Miocene and Pliocene
planktic foraminifera. In H. Bolli, J. B. Saunders and K.
Perch-Nielsen (eds) Plankton Stratigraphy, Cambridge
University Press, 283-314,
MARTINI E. (1971) – Standard Tertiary and Quaternary
calcareous nannoplankton zonation. In Farinacci A. Proc.
2nd Planktonic Conf., 2, 739-785, Tecnoscienza, Roma.
MATTIOLI E. & ERBA E. (1999) – Synthesis of calcareous
nannofossil events in Thetyan lower and middle Jurassic
succession. Riv. It. Paleontol. S., 105, 347-376.
PREMOLI SILVA I. & SLITER W.V. (1995) - Cretaceous planktonic
foraminiferal biostratigraphy and evolutionary trend from
the Bottaccione section, Gubbio, Italy. Paleontografia Italica,
82, 1-189.
RIO D., RAFFI I. & VILLA G. (1990) – Pliocene-Pleistocene
calcareous nannofossil distribution patterns in the western
Mediterranean. Proceedings of the Ocean Drilling Program,
Scientific Results, 107.
SERRA-KIEL J., HOTTINGER L., CAUS E., DROBNE K., FERRANDEZ
C., JAHURI A.K., LESS G., PAVLOVEC R., PIGNATTI J., SAMSO
271
J.M., SCHAUB H., SIREL E., STROUGO A., TAMBAREAU Y.,
TOSQUELLA J. & ZAKREVSKAYA E. (1998) – Larger
foraminiferal biostratigraphy of the Tethyan Paleocene and
Eocene. Bull. Soc. gèol. France 169/2, 281-299.
SISSINGH W. (1977) – Biostratigraphy of Cretaceous calcareous.
Geol. Mijnbouw., 56, 37-65.
SPROVIERI R., BONOMO S., CARUSO A., DI STEFANO A., DI
STEFANO E., FORESI M.L., IACCARINO S.M., LIRER F., MAZZEI
R. & SALVATORINI F. (2002) – An integrated calcareous
plankton biostratigraphic scheme and biochronology for the
Mediterranean middle Miocene. Riv. It. Paleontol. S, 108,
337-353.
SESSIONE 9

SESSIONE 9
Key words: Continental deposits, Early Miocene, Northeastern
Sardinia, Transtensive tectonics.
New geological surveys carried out by authors in relation with
territory planning projects at regional and local scale showed the
presence of conglomeratic deposits of Miocene time occuring in
Gallura and eastern Logudoro regions (Northeastern Sardinia,
fig.1) not reported until now or referred to a Pleistocene age in
official geological maps since lacking in overlaying sediments.
In Gallura region, between Isola Rossa and Vignola Mare
suburbs, extensive outcrops of continental deposits occur,
reported as f1 unit in the old geological maps at 1:100,000 scale
(SERVIZIO GEOLOGICO D’ITALIA, 1974) and as unit 3b in
CARMIGNANI et alii (2008). Lithological, stratigraphic and
geometric characteristics of clastic deposits suggest a Miocene
age. They consist of coarse massive grey-greenish sandstones,
locally cemented, and both clast and matrix-supported
conglomerates with large boulders sourced from Palaeozoic
basement mainly consisting of granitoid rocks; sometimes
conglomerates are interbedded with red silty clay sheets. The
thickness of deposits is about 50 m and their general dipping is
towards NW. The features of sandstones and conglomerates
suggest the existence of an ancient alluvial fan system debrisflow-dominated
in proximal parts of which source area was the
drainage basin of Gallura granitoid mountains.
The deposits lay over Late Palaeozoic granitoids sometimes
with the interposition of rhyolitic ignimbrites (BARBIERI et alii,
1975) of which age in Northern Sardinia ranges between 21 and
18 Ma (GATTACECA et alii., 2007 and references). Pyroclastic
rocks are related to a structural lineament which is part of a NEtrending
left-lateral to transtensive fault set (Viddalba fault,
Tempio fault, Olbia Fault, etc.) active during early Miocene in
North-eastern Sardinia (OGGIANO et alii, 1995; LECCA et alii,
1997, CAMIGNANI et alii, 2001).
It suggests that Tertiary continental Gallura basin developed
as the result of transtensive tectonic activity accompanied by
pyroclastic flows emission; uplift along the fault fronts created a
_________________________
Backdating of some Pleistocene continental deposits in Northern
Sardinia. Preliminary results
(*) ARPA Sardegna contractor to CARG Project, forci.al@tiscali.it
(**) ARPA Sardegna contractor to CARG Project, mrlangiu@tiscali.it
(°) tilokka@yahoo.it
ALESSANDRO FORCI (*), MARIA RITA LANGIU (**) & GIOVANNI TILOCCA (°)
272
topographic high rapidly eroded with subsequent dispersion of
sediments to form coeval alluvial fan at the basin margin
probably under semiarid climates.
Fig. 1 – Main strike-slip fault systems of Northeastern Sardinia (after
Carmignani et alii, 2001), location of places and deposit outcrops (in
orange) cited in the text.
In the absence of palaeontological data and overlaying
sediments, on the basis of similar lithostratigraphic feature the
continental deposits of Gallura area can be related to other
analogous deposits in Northern Sardinia setting under Upper
Burdigalian marine units (PECORINI, 1963; TILOCCA, 1989; 2003;
OGGIANO et alii, 1995; FUNEDDA et alii, 2003; SAU et alii, 2005);
in addition, new field data carried out by authors (CARG Project)
in Nurra and Anglona regions seem to support an Early-Middle
Burdigalian (Orleanian) age for Gallura continental deposits.
Analogous lithostratigraphy and geometry are recognizable in
the deposits cropping out in Logudoro region: near Ozieri
cemetery continental deposits there are a few tens meter thick and
consisting of poorly sorted conglomerate with subrounded
pebble-to-boulder clasts of Palaezoic rocks. The deposits rest
upon Palaezoic rocks and Early Miocene volcanics and were
considered Pleistocene in age (Unit q2 in SERVIZIO GEOLOGICO
D’ITALIA, 1965). Outcrops geometry and the presence of
interbedded pyroclastic-epiclastic sheets seem to indicate an
Early-Middle Burdigalian age. Moreover, the clastic deposits are
related to stratified greywackes and epiclastites referred to
Formazione Lacustre Auct. of Early Miocene time outcropping
nearby. In Sas Concheddas area, 2.5 km northwestward,

analogous coarse matrix-supported breccias containing over
10 m 3 sized boulder (Fig. 2) outcrop unconformably overlaying
Tertiary volcanic rock or Palaezoic granites; sometimes breccias
fills extensional cracks into volcanics about 10 meters large.
By analogy with Gallura deposits, features of Logudoro ones
revealed ancient alluvial fans which terminated in a lacustrine
basin under a persistent volcanic activity during Early Miocene.
Breccias represent proximal sediments along a fault front and
they are probably correlated to the termed Brecce di Codinattu of
Chilivani-Berchidda basin (OGGIANO et alii, 1995) and other
deposits outcropping in Middle-Northern Sardinia (PASCI et alii,
1998).
New field surveys are being performed between Ozieri and
Pattada where recent road excavations revealed volcanic outcrops
adjacent to tectonic lineament striking NE-SW.
This preliminary note aims to give an impulse to a revision of
uncertainty dated sedimentary covers unconformably overlaying
pre-Miocene formations according to work carried out in CARG
Project in the whole Sardinia.
Fig. 2 – Matrix-supported breccia with a large boulder of granite. Is
Concheddas region (Ozieri – SS).
REFERENCES
BARBIERI M., BROTZU P., MORBIDELLI L., PENTA A. & TRAVERSA
G. (1975) - Rioliti ignimbritiche mioceniche della Gallura
(Sardegna settentrionale). Period. Min., 23, 269-286.
CARMIGNANI L., OGGIANO G., BARCA S., CONTI P., ELTRUDIS A.,
FUNEDDA A., PASCI S. & SALVADORI I. (2001) - Geologia della
Sardegna, Note illustrative della Carta Geologica della
Sardegna in scala 1:200.000. Mem. Descr. Carta Geologica
d'Italia, Serv. Geol. It., 60, 283 pp., Ist. Polig. Zecca dello Stato.
CARMIGNANI L., OGGIANO G., FUNEDDA A., CONTI P., PASCI S. &
273
BARCA S. (2008) - Carta Geologica della Sardegna in scala
1:250.000. Litografica Artistica Cartografica, Firenze.
FUNEDDA A., OGGIANO G. & PASCUCCI V. (2003) - I depositi
miocenici della Sardegna Settentrionale: il Bacino del Logudoro.
Escursione post-congresso. Atti Convegno GeoSed 2003,
Alghero 28 Settembre – 2 Ottobre 2003, 381-414.
GATTACCECA J., DEINO A, RIZZO R., JONES D.S. , HENRY B.,
BEAUDOIN B. & VADEBOIN F. (2007) - Miocene rotation of
Sardinia: New paleomagnetic and geochronological constraints
and geodynamic implications. Earth Planet. Sci. Lett., 258, 359-
377.
LECCA L., LONIS R., LUXORO S., MELIS E., SECHI F. & BROTZU P.
(1997) - Oligo-Miocene volcanic sequences and rifting stages in
Sardinia: a review. Period. Mineral., 66, 7-61.
OGGIANO G., PASCI S. & FUNEDDA A. (1995) - Il bacino di
Chilivani-Berchidda: un esempio di sruttura trastensiva.
Possibili relazioni con la geodinamica cenozoica del
Mediterraneo occidentale. Boll. Soc. Geol. It., 114, 465-475.
PASCI S., OGGIANO G. & FUNEDDA A. (1998) - Rapporti tra
tettonica e sedimentazione lungo le fasce trascorrenti cenozoiche
della Sardegna centro-settentrionale. Boll. Soc. Geol. It., 117,
443-453.
PECORINI G. (1963) - Contributo alla stratigrafia post-miocenica
della Nurra di Alghero. Rend. Sem. Fac. Sc. Univ. Cagliari, 33,
1-11.
SAU A., LECCA L., LONIS R., SECCHI F. & FERCIA M.L. (2005) -
La seconda fase del Rift Sardo: evoluzione e vulcanismo dei subbacini
transtensionali di Ardara-Chilivalni e Bonorva (Sardegna
sett.). Boll. Soc. Geol. It., 124, 3-20.
SERVIZIO GEOLOGICO D’ITALIA (1965) - Carta Geologica
d’Italia, Foglio 194 “Ozieri”.
SERVIZIO GEOLOGICO D’ITALIA (1974) – Carta Geologica
d’Italia, Fogli 167-168 “Isola Rossa-La Maddalena”.
TILOCCA G. (1989) - I bacini continentali miocenici della
Sardegna settentrionale, con particolare riguardo alle loro
facies fito-vulcano-clastiche e carbonatico-silicee (Logudoro,
Nurra, Anglona, Gallura). Unpublished PhD Thesis, pp.273.
TILOCCA G. (2003) - Sintesi delle conoscenze sui terreni
continentali terziari in Sardegna settentrionale (Italia). Atti del
Convegno.GeoSed 2003, Alghero 28 Settembre – 2 Ottobre
2003, 533-538.
SESSIONE 9

SESSIONE 9
The 196 Cabella Ligure Sheet of the 1:50.000 scale
geological map of Italy: main results
FERRUCCIO FORLATI (*), PAOLO FALLETTI (*), LIDIA GIACOMELLI (*), MICHELE MARRONI (°) (**),
LUCA PANDOLFI (°) (**), GIUSEPPE OTTRIA (**), ANDREA BERNARDESCHI (°), RITA CATANZARITI (**) & ANNE TAINI (**)
Key words: Central Liguria, Ligurian Units, Mesozoic,
Stratigraphy, Structural Geology, Tertiary Piedmonte Basin,
Tertiary.
INTRODUCTION
The central Liguria (Northern Apennines, Italy) represents a
complex geological area where the connection between Ligurian
Alps and Northern Apennines occurs. In this key-area the
1:50.000 scale sheet 196 “Cabella Ligure” represent a key-sheet
that can provide valuable constraints for the tectonic evolution of
the linkage between the Alps and Apennines.
TECTONIC SETTING
In this area a complex stack of tectonic units, belonging to
different palaeogeographic domains can be recognized: the
Internal Ligurian Units, the External Ligurian Units and the
subligurian Units. The deformation history of this area has been
achieved from Late Cretaceous to Neogene timespan during the
convergence and the following continental collision between the
Europe and Adria plates. The central Liguria is thus characterized
by a tectonic setting where the oceanic- and continent-derived
units, already deformed during the pre-Oligocene, are
unconformably covered by a thick sedimentary succession
deposited from Late Eocene to Late Miocene in an episutural
basin, known as the Tertiary Piedmont Basin.
MAIN RESULTS
The geological mapping associated to a structural analysis on
the Antola Unit has revealed a complex tectonic history with
folding phases developed before and during the sedimentation of
_________________________
(*) ARPA Piemonte
(°) Dipartimento di Scienze della Terra, Università degli Studi di Pisa,
marroni@dst.unipi.it
(**) Istituto di Geoscienze e Georisorse – IGG, CNR
Foglio realizzato nell’ambito di una Convenzione CNR-IGG e Regione
Piemonte
274
the Tertiary Piedmont Basin. The oldest phases, probably both of
Eocene age, were acquired by the Antola Unit during its
westward displacement of the Tertiary Piedmont Basin and
during an eastward, gravity-driven tectonics. The stratigraphical
and paleontological studies (mainly developed on nannofossil
assemblages) have provided a more complete picture of the age
of the different members of the Late Cretaceous Antola
succession. The collected data provides strong evidences for a
correlation between Antola and Cassio Units.
However, the most prominent results have been reached about
the stratigraphy of the Tertiary Piedmont Basin deposits, that
preserve the sedimentary records, mainly represented by major
stratigraphic discontinuities, of the regional tectonic events
connected to the Northern Apennine belt construction.
The area covered by the Sheet 196 “Cabella Ligure” is
located in the easternmost sector of the Tertiary Piedmont Basin,
where the lowermost part of the succession, represented by the
above described succession, ranging from Priabonian to Early
Burdigalian is preserved. In this area the sedimentary succession,
unconformably overlying the External Ligurian Antola Unit, is
represented by marine-marginal deposits characterized by strong
lithofacies variation and by marked compositional changes.
The Tertiary Piedmont Basin succession has been subdivided
in several depositional units bounded by unconformity surfaces.
The unconformity surfaces are characterized by the presence of
angular unconformities and continuos erosional surfaces, abrupt
facies changes in contrast with Walther principle, development of
coarse turbidite systems, deposition of chaotic bodies and
significant compositional changes.
By using unconformity surfaces it has been possible to
recognize 11 depositional units (see the “prototipo” sheet), with
local chronostratigraphic value. These units can be defined as
“hybrid units”, comprising either the charateristics of UBSU and
those of the allostratigraphic units, since the unit’s limits can be
traced also where unconformity surfaces pass in paraconformity
surfaces. Each unit represents a stratigraphic succession
constituted by a set of genetically linked depositional systems.
Each system is bounded by tectonic-related unconformity
surfaces of local and/or regional significance.
The use of hybrid depositional units allows a better
understanding of the basin architecture and of its time-space
evolution, giving emphasis on the synsedimentary tectonics
affecting the basin through time.

2
275
SESSIONE 9

SESSIONE 9
Updating the Paleogene calcareous nannofossil biostratigraphy in
the Mediterranean region
ELIANA FORNACIARI (*), ISABELLA RAFFI (**), DOMENICO RIO (*), CLAUDIA AGNINI (*) & RITA CATANZARITI (°)
Key words: Biostratigraphy, calcareous nannofossils,
Mediterranean.
In the last fifteen years, an intense work has been carried out
on a large number of Paleogene sedimentary sections outcropping
in the Mediterranean area with the aim of improving the
biostratigraphic and biochronologic resolution provided by
calcareous nannofossils. A major effort was focused on the
Paleocene and Eocene time intervals. Results from Mediterranean
on-land sections and ODP sites are presented, including 5
sections in the Southern Alps of Northeastern Italy, 16 sections in
the Northern Apennines and 3 sections from the Umbria-Marche
basin. The resulting Mediterranean biostratigraphic and
biochronologic framework is correlated and discussed with data
from oceanic reference sections from the Atlantic Ocean, the
ODP Sites 1052, 1262, 1263. Our studies permit to extend the
existing calcareous nannofossils Mediterranean zonal schemes,
already proposed in the Neogene and late Paleogene intervals to
overcome the inadequacy of the nannofossil standard zonations
(MARTINI, 1971; OKADA &BUKRY, 1980) due to the absence or
rarity of several marker species in Mediterranean sediments.
Calcareous nannofossils biostratigraphy is confirmed to be a
powerful tool for regional and worldwide biostratigraphic
correlations, and to be significantly useful to the establishment of
a sound time framework which is essential for deciphering
geological and climatic processes. The proposed biostratigraphy
substantially improves the time resolution, sometimes doubling
the current partitioning based on standard Zonations.
REFERENCES
MARTINI (1971) - Standard Tertiary and Quaternary calcareous
nannoplankton zonation. In: A. Farinacci (Ed.) - Proceedings
of the 2nd Planktonic Conference. Edizioni Tecnoscienza,
Roma, 2, 739–785
OKADA H. & BUKRY D. (1980) - Supplementary modification
_________________________
(*) Dipartimento di Geoscienze, Università di Padova,
eliana.fornaciari@unipd.it
(**) DiGAT – CeRSGeo, Università degli Studi “G.d’Annunzio” di Chieti-
Pescara
(°) Istituto di Geoscienze e Georisorse, CNR-Pisa
276
and introduction of code numbers to the low-latitude
coccolith biostratigraphic zonation (Bukry, 1973;1975). Mar.
Micropaleontol., 5, 321-325.

The contact metamorphic aureole of the Mt. Capanne pluton:
new data from the CARG project
Key words: contact metamorphism, Elba Island, Mt.Capanne
aureole, tectonics.
The Elba Island is made of a complex stack of both
continental- and oceanic-derived units (from the Tuscan and the
Ligurian Domains, respectively), piled up during the Apennine
syn-collisional shortening events in the Late Oligocene-Middle
Miocene time interval. Post-orogenic extension, associated to the
emplacement of two main anatectic plutonic bodies (the Mt.
Capanne pluton, at about 6.8 Ma, in western Elba and the La
Serra-Porto Azzurro, at about 5.9, in eastern Elba), deeply
modified the geology of Elba Island, leading to the nucleation of
Fig. 1 - Geological sketch map of western Elba Island.
_____________________________
(*) Dipartimento di Scienze della Terra, Università di Firenze
pandeli@geo.unifi.it
(**) IGG (Istituto di Geoscienze e Georisorse) - CNR - Firenze
FRANCESCA GARFAGNOLI (*), FRANCESCO MENNA (*), GIUSEPPE NIRTA (*),
ENRICO PANDELI (*)(**)&GIANFRANCO PRINCIPI (*) (**)
277
low angle detachment faults, that crosscut and displaced the
thrust sheets stack. Finally, a mainly NS-trending set of highangle
normal faults dissected the tectonic stack at the Miocene-
Pliocene boundary.
The contact metamorphic aureole of the Mt. Capanne pluton
(Fig. 1) is made of an ophiolitic succession (Punta Polveraia-
Fetovaia Unit) including serpentinites, gabbros and a likely Late
Jurassic to Lower Cretaceous volcanic and sedimentary cover.
According to several authors, the peak conditions of contact
metamorphism reach T=575-700 °C and P=1.5-2 kbar. In the
Fetovaia area, a slightly recrystallized Eocene calcareous-marly
succession (Punta Le Tombe Unit or Fetovaia Flysch Auctt.),
including an ophiolite bearing debris flow deposits and slide
blocks, tectonically overlies the contact between the pluton and
the oceanic metamorphosed rocks. The aim of this study is to
SESSIONE 9

SESSIONE 9
Fig. 2 - Outcrop of polydeformed calcschist and marble west of the Spartaia Bay.
define the metamorphic and structural evolution of the middle- to
high-temperature shear zones recognized in some key outcrops
(Spartaia, Punta Polveraia, Punta Nera-Punta del Timone,
Pomonte-Fetovaia, Cavoli-Colle di Palombaia) located at
different distances from the Mt. Capanne pluton.
In all of them, the host rock is characterized by the
development of syn-metamorphic close to isoclinal F2 folds (Fig.
2), with an axial plane, millimetric to centimetric-spaced, zonal to
discrete crenulation cleavage (S2= biotite + muscovite ± quartz ±
calcite ± opaque minerals), transposing a previous foliation,
which is parallel to the lithologic partititions (possibly S0//S1).
Along the limbs of the F2 folds, the main composite schistosity is
parallel to the contact between the host rock and the pluton and
consists of the superposition of the S1 and S2 foliations.
Intrafoliar centimetric rootless hinges and sheath folds, rarely
connected to the D1 event, are also present.
Moreover, a mylonitic fabric is associated to the shear zones
related to the D2 phase. The HT-LP minerals (e.g. pyroxene,
wollastonite, hornblende, garnet, vesuvianite) generally appear
mimetic or static with respect to the foliations or fill post-S2
veins, but they may locally begin to grow during the D2 folding.
The involvement of 8 Ma old porphyric dykes in the D2
structures of the host rock (Fig. 2), testifies that the D2 tectonic
event took place after the emplacement of the dikes, likely during
the intrusion of the Mt.Capanne pluton.
The D2 kinematic indicators (S/C structures, d-or s -
structures) generally suggest a centrifugal sense of shear, with
respect to the centre of the pluton. Subsequent non-metamorphic,
open to close folds, characterized by sub-horizontal axial planes,
are frequently recognized at the mesoscale mesoscale and is
278
likely coeval to the medium-angle detachment fault which
emplaced the Punta Le Tombe Unit onto the Punta Polveraia-
Fetovaia Unit. Finally, high angle normal faults (such as the
Eastern Border Fault from Colle di Palombaia to Procchio) and
fractures cut all the previous ductile structures.

Key words: Colli Albani, hazard, Roman Magmatic Province,
volcanism.
INTRODUCTION
The Colli Albani geological map summarises ten years of
mapping that includes the entire Colli Albani volcano as part of
the new 1:50,000 Geological Map of Italy (Servizio Geologico
d’Italia – CAR.G. project - sheets n. 374 Roma, n. 387 Albano, n.
388 Velletri, n. 375 Tivoli). The map is centred on the Colli
Albani volcano and also includes part of the surrounding pre- and
syn-orogenic Mesozoic-Cenozoic, marine, carbonatic-terrigenous
successions that form the Apennine mountain chain to the East,
and the post-orogenic Pliocene-Pleistocene, marine-transitionalcontinental
terrigenous successions that constitute the basement
for and are partly interfingered with the Colli Albani volcanic
succession. We acknowledge the continuous support and reviews
from the colleagues of the Italian Geological Survey, who have
revised the progresses of the geological surveys and the redaction
of the geological maps, which form the basis for the Geological
Map of the Colli Albani volcano
THE COLLI ALBANI VOLCANO HISTORY
The Colli Albani volcano has been active since ~ 600 ka and
is presently quiescent. The rock stratigraphy indicates that the
activity of the volcano has undergone major changes in terms of
eruption style, average eruption rate and location of active vents.
Chemistry of the Colli Albani products is remarkably mafic, K-
___________________
Stratigraphy, volcano tectonics and evolution of
the Colli Albani volcanic field
(*) Dipartimento di Scienze Geologiche, Università degli Studi di
RomaTre, Roma, giordano@uniroma3.it)
(**) A.A. De Benedetti, A. Diana, G. Diano, A. Esposito, M. Fabbri, F.
Gaudioso, F. Marasco, I. Mazzini, M. Miceli, V. Mincione, M. Porreca, S.
Rodani, C. Rosa, A.P. Vinkler, E. Caprilli, S. Taviani, A. Trigari, D.
Bilardello, S. Malinconico, T. Sabato Ceraldi, R. Funiciello, D. De Rita, M.
Mattei, M. Parotto
GUIDO GIORDANO (*) & THE CARG TEAM (**)
279
rich and silica undersaturated. Nevertheless, the volcano has
experienced all types of eruption styles, from plinian explosive
paroxysms, to milder strombolian to hawaiian eruptions, to
effusive, including also large and small scale phreatomagmatism.
The first period of activity of the volcano is named Vulcano
Laziale period and lasted from ~ 600 ka, to ~ 355 ka. During this
period, volcanism was dominantly explosive, with an average
eruption rate of 1 km 3 /ka. At least seven intermediate to large
volume ignimbrites (VEI 5-7) were erupted and emplaced over an
area larger than 1600 km, forming an extensive ignimbrite shield
around the central, continuosly forming, ~ 8 x 8 km caldera. The
caldera complex and the ignimbrite shield are named Vulcano
Laziale edifice.
The Vulcano Laziale edifice can in turn be subdivided into a
lower Pisolitic Tuffs succession (~600-500 ka), where
ignimbrites are dominated by large scale phreatomagmatism
associated with the likely presence of an early caldera lake, and
an overlying Pozzolane Tuffs succession, where ignimbrites show
a dominantly magmatic fragmentation style, likely in response to
the progressive exhaustion of the caldera lake. The typical
succession of these mafic ignimbrites is made by a sub-plinain to
plinian basal scoria fall deposit covered by the main dark scoria
and ash tabular ignimbrite sheet found as far as >30 km from
caldera rim and across ridges of several hundreds metres in
elevation, and characterised by co-ignimbrite breccias at
proximal locations.
Major ignimbrites were erupted with an average interval time
of ~ 40 ka. After each paroxysmal ignimbrite eruption, the
volcanic activity was dominantly effusive to mild explosive,
concentrated along peri-caldera fissure systems, forming
continuous scoria cone and lava ridges, along with more
explosive eruptions from intracaldera vents. The last major
caldera forming eruption of the Vulcano Laziale period occurred
at ~355 ka emplacing the ignimbrites of the Villa Senni
Formation.
Following this eruption, the complex Tuscolano-Artemisio
peri- and extra-caldera fissure system, dominantly made of scoria
cones and lavas, formed in response to the deflation of the
caldera and peri-caldera area, along with the formation of the
intracaldera Faete stratovolcano. These edifices were emplaced
between ~355 and ~180 ka, an interval time named Tuscolano-
Artemisio-Faete period. While similar peri-caldera and intracaldera
activity occurred earlier, i.e. after each major calderaforming
eruption during the Vulcano Laziale period, the
SESSIONE 9

SESSIONE 9
Tuscolano-Artemisio-Faete period testifies of a significant
reduction of average eruption rate, by one order of magnitude, at
0.1 km 3 /ka, which can be related to a consistent reduction of deep
recharge of the plumbing system, justifying why no further
ignimbrite eruptions occurred after 355 ka.
Peri-caldera activity started initially along the northern and
eastern peri-caldera ring fractures (Tuscolano and Artemisio
sections respectively) and after ~300 ka progressively migrated
outward in extra-caldera position (Pantano Borghese section) and
to the western peri-caldera fractures (S. Maria delle Mole
section).
These latter fracture systems ended their activity almost
simultaneosly, along with the end of the activity at the Faete
intracaldera stratovolcano, between ~280 and ~250 ka. After 250
ka, activity migrated to the south (Monte Due Torri section). The
most recent activity along this latter peri-caldera area interfingers,
between ~200 ka and ~180 ka, with phreatomagmatic products
which instead become dominant in the most recent activity of the
Colli Albani volcano. Starting from ~200 ka (Via dei Laghi
period) the western section of the peri-caldera area has been the
site of repeated very small to small volume, maar-forming
phreatomagmatic eruptions, which formed both monogenetic and
polygenetic maars, collectively named Via dei Laghi maar field.
The most recent of these maars is the polygenetic Albano maar,
which was formed after ~70 ka by at least 7 eruptions migrating
along a NW-SE trending, 3.5 km long fracture.
The last eruption of the maar occurred at < 23 ka. Subsequent
phreatic activity occurred throughout the Holocene, with lahars
originated by dramatic withdrawals of the deep maar lake, at least
till the Eneolithic time (6000-5000 years ago) and likely till
Roman times (IV cent. B.C.E.), when Romans dug a tunnel drain
in order to keep the lake at constant low level. Presently the
Albano area is the site of volcanic gas emissions, ground uplift
and periodic seismic swarms, which may indicate the persistent
activity of a magmatic body at depth.
280

Key words: Brown Tuffs, correlations, geological mapping,
volcanic hazard, widespread pyroclastic deposits.
The Brown Tuffs (BT) on the Aeolian Islands are pyroclastic
ash-rich deposits with very homogeneous lithological features.
Their areal distribution, recurrence through time and
volcanological interpretation have been long debated basically on
a single island scale. Geological fieldwork and stratigraphic
analysis carried out during the nineties, together with new
stratigraphic investigation performed in the course of ongoing
geological mapping of sheets Nos. 577 bis – “Isole di Stromboli e
Panarea”, 580 bis – “Isole di Alicudi e Filicudi”, and 581/586 –
“Isole di Salina, Lipari e Vulcano” as part of the Geological
Mapping of Italy - 1:50,000 project (CARG Project), have
resulted in a systematic reconstruction of BT stratigraphy and
distribution on a regional scale across the Aeolian archipelago.
The combination of stratigraphic and tephro-chronological
data together with available radiometric ages, show that BT
eruptions and depositions are recurrent through time. Distinct and
successive BT units were emplaced from ~80 up to ~7 ka and are
identified by means of the occurrence of localized erosive
surfaces and interbedding of widespread tephra-layers, local
volcanic products, paleosols and epiclastic deposits. The most
complete BT succession is documented on Lipari where 14
distinct stratigraphic units are recognized. In particular, the interisland
correlation of Ischia-Tephra (56 ka) and Monte Guardia
pyroclastites from Lipari (22-21 ka) allows identification at
regional level of Upper (UBT), Intermediate (IBT) and Lower
BT (LBT) units, occurred between 80-56 ka, 56-22 ka and 20-7
ka, respectively. We suggest that the UBT on Lipari (and Salina)
are correlated with the Piano Grotte dei Rossi pyroclastites on
Vulcano island based on stratigraphy, similar lithological,
textural and compositional characters and morpho-types of glass
fragments. Lithological, compositional and stratigraphic data also
provide a feasible correlation of IBT units on Lipari with the
_________________________
Areal distribution and stratigraphy of widespread pyroclastic
Brown Tuffs in the Aeolian archipelago
FEDERICO LUCCHI (*), CLAUDIO ANTONIO TRANNE (*) & GIANFILIPPO DE ASTIS (**)
(*) Dipartimento di Scienze della Terra e Geologico-Ambientali, Università
di Bologna, federico.lucchi@unibo.it, claudio.tranne@unibo.it
(**) Istituto Nazionale di Geofisica e Vulcanologia.
gianfilippo.deastis@ingv.it
281
Monte Molineddo 3 pyroclastites on Vulcano Island.
Both these correlations, combined with consistent N-wards
thickness and grain-size variations, suggest that the UBT and IBT
source area(s) are localized at Vulcano. This is in agreement with
compositional features showing that BT shards are mainly
shoshonitic and latitic, with minor trachy-rhyolitic component,
thus matching the composition of magmas erupted at Vulcano
during the last 50 ka. Merging of field observations, grain-size
and SEM analyses apparently indicate that UBT on Vulcano and
south Lipari have been emplaced during high-intensity
hydromagmatic explosive events giving rise to pyroclastic density
currents spreading laterally from an eruptive vent(s) localized
inside the La Fossa Caldera structure. More distal outcrops of
UBT on north Lipari and Salina (possibly on Panarea) are
interpreted as the result of fallout processes from co-ignimbrite
ash clouds or associated sustained eruptive columns. Basically
based on the large homogeneity of field characters and
compositional features, also the LBT and IBT units are
considered to derive from recurrent, large scale hydromagmatic
eruptions of a source(s) located on Vulcano Island.
Note that, according to their wide distribution and substantial
thickness, BT represent the most voluminous (and recurrent)
pyroclastic deposits across the whole Aeolian archipelago, thus
assuming a fundamental role for the purpose of volcanic hazard
assessment and regional-scale correlation of volcanic and tectonic
events. Therefore, they are a good example of mapping and
stratigraphic studies leading to a new perspective of long-term
volcanic risks in this volcanic district.
SESSIONE 9

SESSIONE 9
CARG Project Foglio 378 Scanno: new contribution for the
geological setting of Central Apennines
ENRICO MICCADEI (*), MAURIZIO PAROTTO (**), ANTONIO PRATURLON (**),
TOMMASO PIACENTINI (*) & CLAUDIO BERTI (°)
Key words: Abruzzo Apennines, CARG project, structural
setting.
In the last years, geological studies in Central Italy are leading
to a new and more complex definition of the geological-structural
setting of the Apennine orogen.
Geological mapping and structural analysis have permitted to
identify, and cinematically characterize, tectonic elements
supposed to have a regional significance. These elements are to
be added to an already complex geological setting resulting from
the interference between a well articulated Meso-Cenozoic
paleogeographic evolution and a polyphasic tectonics. The
surface data is to be linked to the data of deep geophysical
investigations of this area of the Apennines chain, such as the
Crop11 Project (Civitavecchia – Vasto) still under study.
The geological mapping of the Foglio 378 Scanno, between
the Marsica area and the Peligna valley (central Abruzzo), has
outlined a paleogeographic and structural setting more complex
than the one previously known in literature. The identified
compressional tectonics, the strike slip tectonics with several
evidences, and the extensional one, provide new contributions to
the definition of the Neogene-Quaternary evolution of this sector
of the chain. Geometry and kinematics of tectonic elements
permit to fix new constraints concerning the regional
interpretations. Overthrusting of different Mesozoic
paleogeographic domains and large displacements occurred on
the major tectonic elements, make this area a key area for the
comprehension of the relationship among the different tectonicstratigraphic
units, even if a complete analysis will come only by
the mapping of the surrounding areas, within the CARG Project.
Trying to read in time the main geological events involving
the area of the Foglio 378 Scanno, it is possible to highlight the
complexity of all the structuring phases of the orogen.
_________________________
(*) DIGAT Università degli Studi "G. D'Annunzio" Chieti-Pescara,
miccadei@dst.unich.it
(**) Dipartimento di Scienze Geologiche, Università degli Studi Roma Tre
(°) Lehigh University, USA
Lavoro eseguito nell’ambito e con il contributo finanziario del Progetto
CARG Foglio 378 Scanno, in collaborazione con la Regione Abruzzo e con
il Servizio Geologico d’Italia (ISPRA).
282
The sin-orogenic tectonics induces the overthrusting of
tectonic-stratigraphic units along main thrusts of calcareous units
over terrigenous ones.
As result of sin-orogenic compressional tectonics, the main
units seems to be arranged in two different structural levels, being
possible to define “upper units”, comprising carbonate platform
and margin facies , and “lower units” including slope and basin
facies and more external margin and carbonate platform facies.
Moreover, some small units could belong to a more deep
structural level, whose interpretation is to be connected to the
complex tectonic and stratigraphic setting of the southern areas
(Monti della Meta).
According to the results of the investigations of sin-orogenic
terrigenous units outcropping in the area and piggy back late
orogenic conglomerates, the thrusting of tectonic-stratigraphic
units should be ascribed to Late Miocene (i.e. Late Messinian)
and Early Pliocene.
Concerning sin-orogenic tectonics and, in this case, mostly
late-orogenic tectonics the tectonic-stratigraphic units appear to
be displaced along three main transpressional deformation belt,
comprising several fault planes mostly NNW-striking. These
features, already known in some cases in literature (F. Sangro and
F. Giovenco valleys), show a clear persistence all over the area of
the Foglio 378 Scanno. The activity time of these elements is still
unclear, but should anyway be constrained between the last
compressional events (Early Pliocene) and the first evidence of
post-orogenic extensional tectonics (Late Pliocene). To date there
are no evidence or models suggesting that these tectonic elements
could be coeval to the compressional ones. On the fault planes,
several superimposed kinematic indicators provide evidence of
different transport directions both toward eastern sides and
northern sides.
At regional scale scientific debate concerning the
superimposition of the western carbonate platform and the eastern
one is still open. A more certain paleogeographic reconstruction
of the interposed slope-to-basin domain, and of its original width,
could be achieved only in a larger regional view, with the
mapping of the surrounding areas (i.e. Foglio 377 “Trasacco”,
Foglio 391 “S. Donato Val di Comino”, etc). New surface
geological data should be also compared with deep seismic lines
data aiming at evaluate the possible location of the interposed
basin in a regional view.

Post-orogenic tectonics, developed since Late Pliocene –
Early Pleistocene, together with large scale uplift, define a further
complex structural setting, with the formation of the main
tectonic basins, more widely represented in the northern
surrounding areas of the Foglio 368 “Avezzano” and Foglio 369
“Sulmona” (Fucino Plain, Subequan Basin, Sulmona Basin).
Since Early Pleistocene, and possibly Late Pliocene,
extensional tectonics define a ridge and valleys landscape as
suggested by the morpho-lithostratigraphic setting of the older
synthems of the post-orogenic continental succession. Otherwise,
neotectonic evidence along Late Pleistocene and Holocene faults
are generally small, and characterize mainly the boundary areas,
whereas they are markedly evident in the surrounding areas (i.e.
Cinque Miglia Plain and Fucino Plain). Quaternary and recent
tectonics of the Fucino areas is indeed one of the best-known and
studied within Italy.
In summary, the structural setting shows a tectonics activated
since Miocene and still active up to the whole Holocene.
Enlarging the regional view, extent, direction, and geodynamic
significance of the horizontal movements along the
transpressional tectonic elements, as well as the different
hypothesis concerning Meso-Cenozoic paleogeographic
configuration and shortening along compressional tectonic
elements, could be clarified and defined only after the mapping of
the surrounding areas (Fogli 377 “Trasacco”, 379 “Capracotta”,
390 “Frosinone”, 391 “S. Donato Val di Comino”, 392 “Castel di
Sangro”)
Finally, the Foglio 378 “Scanno” mapping, within the CARG
Project has provided new contributions concerning the geological
setting of Central Apennines, and the main contributions and cues
come from the definition of the geological setting, within a larger
regional context.
The project has provided a good satisfaction to the wide
working group that contributed to the realization concerning both
scientific and management aspects. The strong spirit of
cooperation that prompted all the partner of the project,
Geological Survey of Italy (ISPRA), Regione Abruzzo, and
University “G. d’Annunzio” of Chieti-Pescara, permitted us to
overcome problems and obstacles that always occur in these
projects and to complete the work in the right times and modes,
as indicated by the CARG project guidelines.
283
SESSIONE 9

SESSIONE 9
The Athesian volcanics: a spectacular example of caldera complex
CORRADO MORELLI (*), GIUSEPPE MARIA BARGOSSI (**), MARTA MAROCCHI (**), GIANLUCA PICCIN (°),
ALESSANDRO MORETTI (°) & VOLKMAR MAIR (*)
Key words: Athesian Volcanic Group, Caldera, CARG project,
Permian magmatism, Southern Alps.
Within the scientific community, it is generally believed that
the National Geological Mapping Project (CARG) is mainly
devoted to the applied aspects related to geological hazards. In
this study we want to draw further attention on the main scientific
results deriving from the CARG project.
The recent (i.e. 1999-2010) geological survey of the CARG
Sheets Merano, Appiano, Mezzolombardo, Trento and Bolzano
has allowed mapping a large sector of Permian volcanic rocks,
the so called Athesian Volcanic Group (AG). These volcanic
rocks have been the objects of very few (mainly petrographic)
studies in the last decades, even if they represent one of the
widest and most spectacular outcrops of Permian volcanics in
Italy and Europe.
The volcanic sequence in the Athesian area (Trentino Alto
Adige) is bounded by two regional discordances, the lower one
on the South-Alpine Variscan metamorphic basement and the
upper one represented by the Upper Permian continental red beds
(Val Gardena Sandstones).
The AG volcanic activity lasted about 10-15 Ma with a
deposition rate that changed throughout the eruptive cycle
(SCHALTEGGER & BRACK, 2007, VISONÀ et alii, 2007;
MAROCCHI et alii, 2008) during the Lower Permian in a postorogenic
extensionsional to transtensional geodynamic context
(ROTTURA et alii, 1998; WILSON et alii, 2004).
The first important result of the geological mapping within the
CARG project is to have defined a new volcanic stratigraphic
framework, based on the determination of the rock bodies
geometries and the volcanic facies, all supported by petrographic
and geochemical analyses. The new results present a quite
homogeneous magmatic-stratigraphic evolution for the whole
area with important correlations. In spite of the stratigraphic
_________________________
(*) Servizio Geologico, Provincia Autonoma di Bolzano,
corrado.morelli@provincia.bz.it
(**) Dipartimento di Scienze della Terra e Geologico Ambientali,
Università di Bologna.
(°) Libero professionista
284
differences between distinct sectors, it is possible to recognize a
quite unitary evolution showed by the large-scale correlation of
two important ignimbrite units: the Ora formation and the
Gargazzone formation.
The continental volcanic activity of the Athesian Volcanic
Group (AG) is characterised by a serial sub-alkaline character
with calcalkaline geochemical affinity. The volcanic succession
ranges from rhyodacitic-andesitic to rhyolitic, with prevailing
pyroclastic flows and subordinated lavas and epiclastites. Facies
distribution and thickness of the different stratigraphic units have
been strongly influenced by an extensive synvolcanic tectonics.
In particular, the results show that the nature and distribution of
the single volcanic units is strictly related to the formation of
calderas of different ages, which come spatially and structurally
alongside and/or are superimposed. We generally find that
volcanic units are younger in the central sector than those at the
caldera borders. This is due to the particular spatial distribution
of the calderas. The widespread uplift and incision of Permian
rocks in the Athesian area, together with the modest tectonic
deformation, allow to observe exceptional outcrop exposure of
volcanic bodies geometry and in particular of caldera fillings and
their relationship with the extra-caldera areas.
Thus, the results so far indicate that the AG is a complex
volcano-tectonic system in an extensive context with multiple
calderas formation. Recent publications, inspired by the CARG
project fieldwork, present detailed stratigraphic reconstructions
supported by absolute age dating (MORELLI et alii, 2007;
MAROCCHI et alii, 2008).
A further important aspect lies in the potential of these rocks
to give insights into the formation processes of crystals-rich
ignimbrites. These kind of ignimbrites have been related to highly
explosive continental caldera settings and are reported from both
recent (e.g. the Altiplano Puna Volcanic Complex, DE SILVA et
alii, 2006; the Cerro Galan volcanic complex, Andes, FOLKES et
alii, 2009) and ancient contexts (e.g. the Oligocene San Juan
volcanic field Fish Canyon Tuff, USA, BACHMANN et alii, 2000;
the Late Devonian Central Victorian Magmatic Province,
Australia, CAS et alii, 2003, CLEMENS & WALL, 1984).
Nevertheless, the processes controlling fragmentation
mechanisms, eruption and deposition are still obscure and
deserve more investigation. Furthermore, future volcanologic
studies on the Athesian volcanics could have the potential to

clarify the exact timing between caldera collapse, onset/evolution
of eruptions and mode of intra/extra caldera filling.
It’s very important here to stress that only a geological
mapping project like the CARG, in which field geologists and
researchers have the possibility to cooperate and progress for a
long period (more the 10 years), can achieve such high-quality
scientific results.
REFERENCES
BACHMANN O., DUNGAM M. A. & LIPMAN P. W. (2000) -
Voluminous lava-like precursor to a major ash-flow tuff: lowcolumn
pyrolcastic eruption of the Pagosa Peak Dacite, San
Juan volcanic field Colorado. J. Volcanol. Geotherm. Res.
98, 153-171.
CAS R. A. F., O’HALLORAN G. J., LONG J. A. & VANDENBERG A.
H. M. (2003) - Middle Devonian to Carboniferous. Geology
of Victoria. Geol. Soc. Aust. Spec. Publ., 23, Melbourne.
CLEMENS J. D. & WALL V. J. (1984) - Origin and evolution of a
peraluminous silicic ignimbrite suite: The Violet Town
Volcanics. Contrib. Mineral. Petrol., 88, 354-371.
DE SILVA S., ZANDT G., TRUMBULL R., VIRAMONTE J. G., SALAS
G. & JIMENEZ N. (2006) - Large ignimbrite eruptions and
volcano-tectonic depressions in the Central Andes: a
thermomechanical perspective. In C. Troise, G. De Natale
and C.R.J. Kilburn, (Eds) - Mechanisms of Activity and
Unrest at Large Calderas. Geol. Soc. Spec. Publ., London,
269, 47-63.
FOLKES C. B., DE SILVA S., WRIGHT H. M., CAS R. A. F., LESTI C.
& VIRAMONTE J. G. (2009) - A Re-appraisal of the
stratigraphy and volcanology of the Cerro Galan volcanic
system, NW Argentina. GSA Annual Meeting, Portland,
abstract n. 164893, 41 (7).
MAROCCHI M., MORELLI C., MAIR V., KLÖTZLI U. & BARGOSSI
G. M. (2008) - Evolution of large silicic magma systems: New
U-Pb zircon data on the NW Permian Athesian Volcanic
Group (Southern Alps, Italy). J. Geol., 116, 480-498.
MORELLI C., BARGOSSI G. M., MAIR V., MAROCCHI M. &
MORETTI A. (2007) - The Lower Permian volcanics along the
Etsch Valley from Meran to Auer. Mitt. Österr, Miner. Ges.,
153, 195-218.
ROTTURA A., BARGOSSI G. M., CAGGIANELLI A., DEL MORO A.,
VISONÀ D. & TRANNE C. A. (1998) - Origin and significance
of the Permian high-K cala-alkaline magmatism in the
central-eastern Southerm Alps, Italy. Lithos, 45, 329-348.
SCHALTEGGER, U.&BRACK, P. (2007) - Crustal-scale magmatic
systems during intracontinental strike-slip tectonics: U, Pb
285
and Hf isotopic constraints from Permian magmatic rocks of
the Southern Alps. Int. J. Earth Sci., 96, 1131-1151.
VISONÀ D., FIORETTI A. M., POLI M. E., ZANFERRARI A. &
FANNING M. (2007) - U-Pb SHRIMP zircon dating of
andesite from the Dolomite area (NE Italy):
geochronological evidence for the early onset of Permian
volcanism in the eastern part of the Southern Alps. Swiss J.
Geosci., 100, 313-324.
WILSON M., NEUMANN E. R., DAVIES G. R., TIMMERMANN M. J.,
HEEREMANS M. & LARSEN B. T. (2004) - Permo-
Carboniferous magmatism and rifting in Europe:
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SESSIONE 9

SESSIONE 9
Key words: Applied geology, digital geological map, geological
survey of Regione Toscana, groundwaters, metadata, scale
1:10.000, soil science, web services.
INTRODUCTION
During the late 1990s the Geological Survey of Tuscany
focused its interest on the production of digital geological maps,
georeferenced database and on the development of web services
to download these products free of charge.
The idea was to provide local agencies, decision makers,
consultants and professionals an easy and quickly way to gain
information.
In fact it has been demonstrated (MORINI, 2004) that the
printing phase takes too much time for an operational use of the
products. Nowadays, thanks also to many open source and free
software, the use of Geographical Information System greatly
increased both at public and private level.
Moreover one of the main advantage is that a digital map or a
database can be updated continuously at any time, without
planning a new expensive and longlasting survey programmes,
whenever an updated edition of the map comes out as strictly
necessary.
It was decided to realase every intermediate step, as a preview
of the final product, and make it available on the Internet,
according to the idea that “something is better than nothing”.
The decision was demonstrated as a successful one by
monitoring the number of daily downloads from our servers.
PAST
The first digital map was realized in 1998-99 by carring on
the vectorization of the national geological map at the scale
1:100,000, started from the Arno River Basin Autority. At that
time, the printed map was the only one covering the whole
Region.
_________________________
The Geological Survey of Regione Toscana:
from the Geological Map to the digital geothematic Databases
(*) Regione Toscana – Servizio Geologico Regionale,
domenico.morini@regione.toscana.it
DOMENICO MORINI (*)
286
In the next year, with a budget of about 8 millions euro, the
Geological Survey started the “Regione Toscana” project of
geological mapping. The supervision of the project was carried
on by the Tuscany Geological Survey and its executive arm, the
Consorzio LaMMa (Laboratory of Monitoring and
Environmental Modelling for sustainable development). The 735
maps at 1:10,000 scale, covering all the Regione Toscana, were
surveied from the Departments of Earth Sciences of the three
Tuscany Universities and the National Research Council. They
also provided georeferenced database for each map. The last map
was provided in the second half of 2006. As said, no maps were
printed, but only available in digital format.
Many “Thematic Derived Maps” were developed in parallel
with the production of the Geological vector maps (lithological
(oriented to soil science), lithotechnical, hydrogeological
(permeability) and geomorphological. Again all of these products
are downlodable from Internet.
In the last years the Survey started a new branch of activity
related to the groundwaters saving programmes adopted by
Regione Toscana. The main project was the implementation of a
database (BDSRI) storing technical georeferenced information on
about 200,000 wells, abstractions of surface water, springs,
stratigraphies, piezometers, chemical analysis and the like. This
database homogenized data derived from many different Local
Authorities.
Other projects completed during this period were the IFFI
project (Italian Landslides Inventory) for the digitalization of all
landslides of Tuscany, and the scanning of the whole paper-based
archive known as “Archivio ex Rimin” containing papers and
maps about mines since XIX century.
PRESENT AND FUTURE
Many of present and future activities are deeply discussed in
the proceedings of this congress and both in oral or poster
presentations, so in several cases just references to the pertaining
papers are given.
Presently the Geological Survey follows three lines of
activity: groundwater, applied geology and soil science.
Another line of work covering all of these topics concerns the
publishing of data and metadata on Internet.
Concerning groundwater the most important projects are:
• Acquifers. In progress.

• Mineral and thermal waters database (BDCAMT) that
concerns all the administrative concessions and technical
data for the exploitation of mineral and thermal waters.
Completed.
• Geothermal database (BDGT) which stores, among
many other information, data on high, medium and low
enthalpy. In progress.
Concerning applied geology the main projects are:
• Stability of slopes. In progress.
• Geothematic database of municipal plans. In progress
• Asbestos and treatment methodologies. Starting
• Continuum of the geological map of Regione Toscana.
Closure.
• Marble and quarray activities. Closure.
• Subsoil uses. In progress.
• Atlas of biostratigraphic data. Closure.
Concerning soil science the objective is to implement a
georeferenced database storing maps and data derived from the
elaboration of geological map 1:10,000 and many other regional
databases. In progress.
The last covered branch was the internet portal to the
geological information for Regione Toscana. There are many web
map services (too many to list) and metadata for almost all digital
information. The “Geological Map Manteinance” service has
started this year. Professionals, students or the like can submit a
specific form when they find incongruity between geological map
and a direct observation in the field or if they wish to add a
stratigraphy from a new drill.
Follow this link to access all the geological information of
Regione Toscana: http://www.regione.toscana.it/geologia
REFERENCES
MORINI D. (2004) – The “Regione Toscana” project of
geological mapping: a summary and a proposal. In: D.
Morini and P. Bruni (Eds.) - The “Regione Toscana” project
of geological mapping. Case histories and data acquisition.
Regione Toscana, 11-23.
287
SESSIONE 9

SESSIONE 9
Key words: Elba Island, geological evolution, Northern
Apennines, stratigraphy, tectonics.
The geology of the Elba Island is very interesting for the
structural complexity, for the relationships between the Mio-
Pliocenic magmatism and tectonics and for being placed between
Corsica and Northern Apennine. Its long-living geologic history
takes roots in the Palaeozoic, but the Alpine tectonic evolution
begins in the Late Cretaceous - Early Tertiary during the
consumption of the Mesozoic Western Tethys (Liguria-Piedmont
Basin). This event produced the collision and polyphase
deformation of the European (Corsica) and Adriatic (Tuscan
Domain) paleocontinental margins. The final emplacement of
the tectonic units occurred during the post-orogenic extension
and, finally, during the intrusion and uplift of the Late Miocene
monzogranitic plutonic bodies (the about 6.8 Ma M.Capanne and
the about 5.9 Ma La Serra-Porto Azzurro pluton) when skarns
bodies and part of the famous Fe-ores were originated. New
stratigraphical and structural data (BORTOLOTTI et alii, 2001;
CARG Project Sheet Isola d’ Elba) modify and complicate the
previous geological frame proposed first by TREVISAN (1950)
and BARBERI et alii (1969) based into the piling of five
Complexes. Our new scheme comprises nine main tectonic units,
built up of Tuscan, Ligurian and Ligurian-Piedmont successions
complexly piled up. In particular they are (from bottom to top of
the tectonic pile, see Fig. 1):
Porto Azzurro Unit “PU” – It mainly consists of the Mt.
Calamita Fm. (micaschist and quartzose phyllitic successions
with local ortho-amphibolites intercalations of likely Cambro-
Ordovician and Carboniferous-Permian age) which represents
part of the Tuscan basement. These rocks are unconformable
covered by Triassic to Hettanian formations (the siliciclastic
Verrucano, the Tocchi Fm. and the Calanchiole Marble and
crystalline dolostone). PU shows a complex tectono-metamorphic
history, which ends with the cornubianitisation processes and
deformations linked to the La Serra-Porto Azzurro monzogranitic
intrusion. A low-angle fault associated with an about ten m thick
cataclastic horizon (Zuccale fault) constitutes the contact with all
the overlying tectonic units.
_________________________
The Elba island: an intriguing geological puzzle in the Northern
Tyrrhenian sea
ENRICO PANDELI (*), VALERIO BORTOLOTTI (*) & GIANFRANCO PRINCIPI (*)
(*) Dipartimento di Scienze della Terra - Università di Firenze and IGG
(Istituto di Geoscienze e Georisorse)-CNR – Firenze, pandeli@geo.unifi.it
288
Ortano Unit “UO” - It comprises more or less cornubianitised
phyllites and quartzites (Capo d’Arco Schists) at the base, locally
crosscut by rare and thin aplitic and microgranitic dikes (similar
to those intruded in the Porto Azzurro Unit). At their top
porphyroids and porphyritic schists grade upward to phyllites and
quartzitic metasandstones and metaconglomerates. This
succession can be correlated with the Ordovician Variscan
formations of the Apuan Alps and of the central Sardinia and
probably represents an Alpine kilometric-scale isoclinal fold with
Ordovician metavolcanites at the core.
Acquadolce Unit “AU” - It begins with a basal massive, partly
dolomitic marbles that grade upwards to sometimes cherty
calcschists with, at their top, a metapelitic siliciclastic succession
with local calcschist intercalations. In the latter rocks DURANTI et
alii (1992) found a Lower Cretaceous microfauna and DEINO et
alii (1992) obtained a 19-20 Ma for the main schistosity. We
think that these terrains probably correspond to a Ligurian-
Piedmont oceanic sequence as the Schistes Lustrés of Corsica and
of the Gorgona I. Also the presence of a serpentinite sheet at its
top agrees with this interpretation.
Monticiano-Roccastrada Unit “MU” - The base of this Unit is
made of fossiliferous graphitic metasediments of Late
Carboniferous-Early Permian (Rio Marina Fm Auctt.), on which
the detrital Triassic Verrucano successions deposited. The
epimetamorphic successions of Capo Castello-Isola dei Topi and
of Capo Pero (north and south of Cavo, respectively), which
includes formations from Late Jurassic (siliceous metalimestones)
to the Oligocene (Pseudomacigno), represent part of the
Verrucano cover.
Tuscan Nappe “FT” - In the Porto Azzurro-Rio Marina, and
Norsi-La Valdana areas, it is represented only by calcareousdolomitic
breccias (Calcare Cavernoso Auctt.); northwards, also
the overlying carbonatic (Rhaetavicula Limestone and “Calcare
Massiccio” - Late Triassic-Hettangian), carbonatic-cherty
(Limano Fm and “Ammonitico Rosso” - Middle-Late Liassic)
and marly-carbonate formations (Posidonia Marlstones - Dogger)
crop out.
Grassera Unit “GU” - It comprises at the base calcschists,
sometimes with cherts, but most of the unit is made up of
varicoloured slates and siltstones with rare manganiferous,
recrystallized siliceous and calcareous beds Its lithofacies are
different from those of all the formations of both Tuscan and
Ligurian Domains. So, we propose a provenance of GU from the
Ligurian-Piedmont paleogeographic domain, as the AU.

Ophiolitic Unit “OU” – This unit is built up of some minor
thrust sheets (e.g. the Acquaviva, Mt. Serra, Sassi Turchin and
Volterraio Subunits), characterised by ophiolites of the oceanic
basement of the Western Tethys (serpentinites and gabbros) on
which is generally present a more or less complete volcanic
(basalts) and sedimentary (Mt. Alpe Cherts, Nisportino Fm,
Calpionella Limestones and Palombini Shales) cover of Late
Jurassic-Early Cretaceous age. This unit can be interpreted as a
relic of a trapped oceanic crust originally near the Corsica
European margin.
Eocene Flysch Unit “EU” - It is represented by a shaly-marly
succession with turbiditic calcilutites, sandstones and ophiolitic
breccias of Eocenic age.
Cretaceous Flysch Unit “CU” - In this second turbiditic unit
we can distinguish, on top of the Palombini Shales and
varicoloured shales, a lower section, represented by siliciclastic
sandstones and conglomerates (Ghiaieto Sandstones) and an
upper one with marly limestones and marls (Marina di Campo
Fm). The age of the last two formations is Campanian-
Maastrictian.
Fig. 1 - The central and eastern Elba tectonic pile. PU- Porto Azzurro Unit; UO-
Ortano Unit; AU- Acquadolce Unit (a. Porticciolo Subunit, b- Santa Filomena
S.); MU- Monticiano-Roccastrada Unit; TN- Tuscan Nappe; GU- Gràssera Unit;
OU- Ophiolitic Unit (a- Acquaviva Subunit; b- Mt. Serra S.; b1- Capo Vita S.; c-
Sassi Turchini S.; d- Volterraio S.; e- Magazzini S.; f- Bagnaia S.); EU-
Paleogene Flysch Unit; CU- Cretaceous Flysch Unit (after BORTOLOTTI et alii,
2001).
REFERENCES
BARBERI F. et alii (1969) - Note illustrative della Carta
Geologica d’Italia alla scala 1:100.000. Foglio 126 Isola
d’Elba. Serv. Geol. d’It., 32 pp.
BORTOLOTTI V. et alii (2001) - Geology of Central and Eastern
Elba Island, Italy. Ofioliti, 26 (2a), 97-151.
DEINO A. et alii (1992) - Datazioni 40Ar/39Ar del metamorfismo
dell’Unità di Ortano-Rio Marina (Isola d’Elba): risultati
preliminari. Studi Geol. Camerti, Vol. Spec. 1992/2, 187-192.
289
DURANTI S. et alii (1992) - Geological evolution and
metamorphic petrology of the basal sequences of Eastern
Elba (Complex II). Acta Vulcan., 2, 213-229.
TREVISAN L. (1950) - L’Elba orientale e la sua tettonica di
scivolamento per gravità. Mem. Ist. Geol. Univ. Padova., 16,
5-39.
SESSIONE 9

SESSIONE 9
Key words: acidic-intermediate magmatic dikes, Elba Island,
Neogene magmatism, Northern Tyrrhenian Sea.
The Elba Island (Northern Tyrrhenian Sea) is a complex and
well-known assemblage of geological bodies which developed
during a long time span (about 90 Ma), essentially since Late
Cretaceous to Pliocene. Its structural framework includes
nappes derived from different paleogeographic domains (e.g.
Tuscan and Ligurian Domains), piled up during the Oligocene-
Middle Miocene syn-collisional events of the Northern
Apennines tectogenesis. In the Late Miocene-Early Pliocene,
this structural pile was intruded by different, mainly acidic (e.g.
the monzogranitic M.Capanne and La Serra-Porto Azzurro
plutons, the laccolitic complex of the central Elba) and minor
intermediate-acidic femic (e.g the Orano Porphyry, the Monte
Castello dike and Casa Carpini dike: DINI et alii, 2002;
CONTICELLI et alii, 2001; PANDELI et alii, 2006) magmatic
bodies. In this frame, we studied acidic-intermediate magmatic
dikes, of likely Late Miocene age, cropping out in the southern
part of the Island, along the eastern coast of the Capo Stella
Promontory (NNE of Casa Mazzarri locality, location in Fig.
1). These decimetric up to 130 cm-thick, grey to brownish,
magmatic bodies fill a high to medium angle fracture network,
generally characterized by a NW-SE strike and a NE dip,
cutting the Jurassic pillow lavas, pillow breccias and
ialoclastites of the Ligurian Ophiolitic Unit.
The dikes and the basaltic host rocks are affected by low-angle
reverse faulting characterized by a SE-ward tectonic transport
and by quartz veins. The phaneritic sub-volcanic rocks are
characterized by a porphyritic textures with subhedral to
euhedral zoned plagioclase ( with albite polysynthetic
______________
The Neogene magmatism in the Northern Tyrrhenian Sea: setting
and compositional data of the Monte Capo Stella dikes (Southern
Elba Island, Tuscan Archipelago)
(*) Dipartimento di Scienze della Terra, Università di Firenze,
pandeli@geo.unifi.it
(**) IGG (Istituto di Geoscienze e Georisorse) - CNR - Firenze
ENRICO PANDELI (*) (**), ALBA SANTO (*) (**) & MONICA CANDIDO (*)
Fig. 1 – Tectonic scheme of central and eastern Elba according to BORTOLOTTI et
alii (2001). 1- Porto Azzurro Unit; 2- Ortano Unit; 3- Acquadolce Unit (a-
Porticciolo Subunit; b- Santa Filomena Subunit); 4- Monticiano Roccastrada Unit;
5- Tuscan Nappe; 6- Gràssera Unit; 7- Ophiolitic Unit (a- Acquaviva Subunit; b-
Mt. Serra Subunit; c- Capo Vita Subunit; d- Sassi Turchini Subunit; e- Volterraio
Subunit; f- Magazzini Subunit; g- Bagnaia Subunit); 8- Eocene Flysch Unit; 9-
Cretaceous Flysch Unit; 10- La Serra-Porto Azzurro monzogranite; 11- Mt. Castello
shoshonitic dike. F- Faults; l- Low angle tectonic contact: thrusts and detachments.
Arrow: location of the Monte Capo Stella dike.
290
and albite-carlsbad twinnings, local decussate textures and
epidote alterations, Fig. 2), subhedral to anhedral quartz (often
with embayed rims, Fig. 3), and subordinate K-feldspar
(sanidine, orthoclase) phenocrysts, up to 7 mm in size.
Noteworthy, plagioclase composition displays high variability,
from albite to labradorite.

Often chloritized biotite and amphibole (kaersutite, hornblende)
microphenocrysts also occur in low quantity. The
holocrystalline-microcrystalline groundmass is made up of
xenomorphic quartz and K-feldspar, plagioclase microliths,
biotite and amphibole. Fe- and Ti-oxides, apatite, zircon and
epidote are present as accessory minerals. The studied dikes
locally show chilled margins and an evident decrease of crystal
size from inner to outer zone.
400 µm
Fig. 2 – Decussate texture of a plagioclase phenocryst in the Monte
Capo Stella Dyke. Crossed polars.
400 µm
Fig. 3 – Embayed quartz xenocryst in the Monte Capo Stella Dyke.
Crossed polars.
Here the texture is variable from microcrystalline, with
plagioclase and biotite (generally chloritized), to aphanitic and
is locally characterised by the presence of sub-millimetric
irregular, at times spherical to ellipsoidal spots, not completely
resolvable at the microscope observations. The Monte Capo
Stella dike display quartz-dioritic composition. Major and
trace element analyses evidence some differences (e.g. K, Rb,
La) among rock samples collected from different dykes. The
REE patterns are characterised by fractionated LREE and
MREE and positive anomaly of Eu.
291
The mantle-normalized trace element patterns show relatively
high content of the most incompatible elements with a positive
spike of Th and high LILE/HFSE ratios. Negative spikes of Nb,
P and Ti are also observable. No negative anomalies of Sr are
present.
87 Sr/ 86 Sr and
143 Nd/ 144 Nd isotopic ratios are
respectively 0.708129 and 0.512209. The petrographic and
compositional data suggest that the Monte Capo Stella dikes
belong to the intermediate-acidic rocks of the Tuscan Magmatic
Province characterized by mixing of upper mantle magma with
crustal anatectic components. When compared with other
intermediate-acidic dikes of the Elba Island (e.g. the Orano
Porphyry, the Mt.Castello dike, the Casa Carpini dike),
petrographic features and some major and trace element
abundances point to differences which confirm the high
compositional variability of magmatic products from Elba
Island.
REFERENCES
BORTOLOTTI V., FAZZUOLI M., PANDELI E., PRINCIPI G.,
BABBINI A. & CORTI S. (2001) - Geology of Central and
Eastern Elba Island, Italy. Ofioliti, 26 (2a): 97-151.
CONTICELLI S., BORTOLOTTI V., PRINCIPI G., LAURENZI M.A.,
D’ANTONIO M. & VAGGELLI G. (2001)- Petrology,
Mineralogy and geochemistry of mafic dyke from Monte
Castello, Elba Island, Italy. Ofioliti, 26 (2a):249-262.
DINI A, INNOCENTI F, ROCCHI S, TONARINI S&WESTERMAN
DS. (2002) - The magmatic evolution of the late Miocene
laccolith-pluton-dyke granitic complex of Elba Island,
Italy. Geol. Mag., 139:257-279.
PANDELI E., SANTO A.P., MORELLI M. & ORTI L. (2006) -
Petrological and geological data of porphyritic dikes from
the Capo Arco area (eastern Elba island, northern
Tyrrhenian sea). Per. Mineral., 75, 2: 291-302.
SESSIONE 9

SESSIONE 9
The Geological Sheet n° 419 “San Giorgio La Molara”: new data for
the analysis of the Sannio segment of Southern Apennnines (Italy)
TULLIO PESCATORE (*), SILVIO DI NOCERA (°), FABIO MATANO (*) (°) & FELICE PINTO (*)
Key words: Regional geology, Sannio, Southern Apennines.
INTRODUCTION
The n°419 "San Giorgio la Molara" map sheet falls in the
Sannio sector of the Southern Apennines. The very complex
tectonic and stratigraphic features of the Sannio Apennines have
been described in several papers (SELLI, 1957; DAZZARO et alii,
1988; PESCATORE et alii, 2000, 2008; DI NOCERA et alii, 2006).
In the study area, Late Cretaceous to Middle Miocene basin
successions and middle-late Miocene to Pliocene foreland clastic
successions crop out. The landscape is characterised by relatively
high calcareous moutains in the western margin and calcareouspelitic
and arenaceous-pelitic hills in the central-eastern sectors,
which are separated by wide and smooth Fortore, Tammaro and
Calore river valleys.
STRATIGRAPHY
Facies analyses, stratigraphy, tectonics and geological
mapping of the Late Cretaceous to Miocene units allowed us to
identify four different tectonic units: the Sannio, Frigento, Fortore
and Valle del Tammaro units, which are strongly deformed and
thrusted eastward upon the buried Apulian thrust system. All the
basinal deposits are referred to an external basinal domain
(Lagonegro-Molise basin) (MOSTARDINI & MERLINI, 1986;
CASERO et alii, 1988; PESCATORE et alii, 1988, 1992).
The tectonic units are mainly formed by Upper Cretaceous to
Early Miocene successions characterized by basinal and shelfmargin
facies (‘Flysch Rosso’ Fm.) and by basinal mainly
calcareous-pelitic deposits of the Argille Variegate Group and
Corleto Perticara fm., conformably followed by numidian flysch
quartzarenites and arkosic arenites (Fragneto Monforte fm. and
_________________________
(*) Department of Geological and Environmental Sciences, University of
Sannio, pescatore@unisannio.it; fpinto@unisannio.it
(°) Department of Earth Science, University of Naples “Federico II”,
sildinoc@unina.it; matano@unina.it
This work was carried out within the CARG Project.
292
San Giorgio fm.). The ‘Argille Variegate’ is believed to be of
internal provenance (‘Sicilide Complex’) after OGNIBEN (1969).
In the westernmost areas, the successions are characterized by
frequent occurrence of coarse to fine calciclastic deposits settled
by dense gravity flows (Flysch Rosso fm.) coming from a
carbonate platform margin, as well as by slumps and greater
thicknesses of the single beds; they are followed by Upper
Burdigalian – Upper Langhian p.p. numidian flysch
quartzarenites.
These deposits form the internal (i.e. western) margin of the
Lagonegro basin and have been ascribed to the Sannio unit. The
Frigento Unit (DI NOCERA et alii, 2002) is formed by Upper
Cretaceous - Middle Miocene mainly calcareous-siliceous-pelitic
basinal deposits. The sequence is formed by a calcareous-pelitic
turbiditic unit (Flysch Rosso fm.), by upper Burdigalian – upper
Langhian p.p. numidian flysch quartzarenites conformably
overlaid by Upper Langhian p.p. – Serravallian p.p. Fragneto
Monforte terrigenous deposits.
The successions cropping out in the central-eastern zone are
typically composed of pelagic sediments (varicoloured clays and
shales) intercalated with fine carbonate turbidites representing a
more distal facies of the coarser proximal facies. Therefore, these
units show lateral relationships with the margin and base of slope
sequences previously described and record sedimentation along
the axial zone of the Lagonegro-Molise basin. These deposits are
ascribed to the Fortore and Valle del Tammaro units. In the
“Argille Variegate” sequences fault-related folding complex
structures are widespread with significant along-strike variations
in thrust displacement. These structures display both vertical and
lateral changes in style; deformation is expressed by the
development in the pelites of asymmetrical folds with strongly
refolded fold axes and pervasive fracture cleavage, producing
sometimes a chaotic assemblage of the strata.
The Fortore Unit (DAZZARO et alii, 1988; PESCATORE et alii,
2000) is formed by an Upper Cretaceous - Burdigalian basinal
calcareous-pelitic succession, formed by Argille Variegate Group
and Corleto Perticara fm., by numidian flysch quartzarenites,
unconformably overlaid by San Bartolomeo flysch. In particular,
siliciclastic, volcaniclastic and calciclastic deposits with frequent
intercalations of carbonate clastics (Paola Doce fm., after
PESCATORE et alii, 1992, upper Oligocene–lower Miocene in
age) conformably overlie Argille Variegate group and Corleto

Perticara formation. The Paola Doce formation grades into the
overlying Numidian quartzarenites.
In the Valle del Tammaro unit, the Numidian sandstone
directly and conformably overlies Argille Variegate group and
Corleto Perticara formation; the middle-late Miocene siliciclastic
and calciclastic deposits (San Giorgio fm.), conformably lying on
the numidian flysch, Argille Variegate group and Corleto
Perticara formation, outcrop along the easternmost belt.
The tectonic units are unconformably overlain by middle-late
Miocene terrigenous flysch deposits (Reino-Morgia dei Rauli
fm., Caiazzo sandstones and San Bartolomeo Flysch) and
Pliocene unconformity bounded marine to alluvial units. In the
Pliocene (Ariano Irpino supersynthem) wedge-top depozone
basins developed. They lie by means of a regional unconformity
on several tectonic units of the orogenic wedge. In the study area
only one depositional sequence has been recognised: the Andretta
Synthem (Baronia Fm.) has an Early Pliocene age (biozone
MPl4a) and is about 200 m thick.
TECTONICS
The Lagonegro-Molise units of the Sannio Apennines show a
very complicated structural style: mainly east-verging
imbrications are recognized and northeast verging folds related to
reverse faults are located into regional thrust sheets. The tectonic
superpositions are complicated by a polyphased structuration,
which occurred after the juxtaposition of the Sannio unit onto the
Frigento unit onto the Fortore/Valle del Tammaro units, during
the deposition of Upper Miocene and Pliocene siliciclastic
deposits.
The structural complexity seems to characterize the whole
orogenic evolution of the ENE-verging fold-and-thrust belt
system, but the major imbrications result from the post-Messinian
refolding and breaching of more ancient structures. The presence
of fault cut-off structures and the presence of the Inner Apulian
Platform (Apulian thrust system) at a depth of ca. 2000 m testify
their assemblage as resulting from the breaching developed after
duplexing of the Inner Apulian unit. The complexity of structural
styles seems to result from the Pliocene refolding of more ancient
structures produced by middle-late Miocene deformation.
REFERENCES
CASERO P., ROURE F., ENDIGNOUX L., MORETTI I., MULLER C.,
SAGE L. & VIALLY R. (1988) - Neogene geodynamic evolution
of the Southern Apennines. Mem. Soc. Geol. It., 41, 109-120.
DAZZARO L., DI NOCERA S., PESCATORE T., RAPISARDI L.,
ROMEO M., RUSSO B., SENATORE M. & TORRE M. (1988) -
Geologia del margine della catena appenninica tra il F.
293
Fortore ed il T. Calaggio (Monti della Daunia - App. Merid.).
Mem. Soc. Geol. It., 41, 411-422.
DI NOCERA S., MATANO F. & TORRE M. (2002) - Le unità
“sannitiche” Auct. (Appennino centro-meridionale):
rassegna delle correnti interpretazioni stratigrafiche e
paleogeografiche e nuove ipotesi con l’introduzione
dell’Unità di Frigento. St. Geol. Camerti, n. s., 1 (1), 87-102,
Camerino.
DI NOCERA S., MATANO F., PESCATORE T., PINTO F.,
QUARANTIELLO R., SENATORE M.R. & TORRE M. (2006) -
Schema geologico del transetto Monti Picentini orientali -
Monti della Daunia meridonali: unità stratigrafiche ed
evoluzione tettonica del settore esterno dell'Appennino
meridionale. Boll. Soc. Geol. It., 125, 1-20.
MOSTARDINI F. & MERLINI S. (1986) - Appennino centro
meridionale. Sezioni geologiche e proposta di modello
strutturale. Mem. Soc. Geol. It., 35, 177-202.
OGNIBEN L. (1969) - Schema introduttivo alla geologia del
confine calabro-lucano. Mem. Soc. Geol. It., 8, 453-763.
PESCATORE T., RENDA P. & TRAMUTOLI M. (1988) - Rapporti tra
le Unità lagonegresi e l’Unità sicilide nella media valle del
Basento. Mem. Soc. Geol. It., 41, 353-361.
PESCATORE T., RENDA P. & TRAMUTOLI M. (1992) - "Tufiti di
Tusa" e flysch Numidico nella Lucania centrale (Appennino
meridionale). Rend. Acc. Sci. Fis. Matem. Soc. Naz. Sci. Lett.
Art. Napoli, 59, 57-72.
PESCATORE T., DI NOCERA S., MATANO F. & PINTO F. (2000) -
L'Unità del Fortore nel quadro della geologia del settore
orientale dei Monti del Sannio (Appennino meridionale).
Boll. Soc. Geol. It., 119, 587-601.
PESCATORE T., DI NOCERA S., MATANO F., PINTO F., BOIANO U.,
CIVILE D. & MARTINO C. & QUARANTIELLO R. (2008) - Prime
considerazioni sulla geologia del settore centrale dei monti
del Sannio. Mem. Descr. Carta Geol. d’It., 77, 77-94.
SELLI R. (1957) - Sulla trasgressione del Miocene nell'Italia
meridionale. Giorn. Geol., ser. 2, 24, 1-54
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The geological map of Emilia-Romagna Region from scale 1:10,000
to scale 1:250,000: scientific base, utility and future
Key words: Cartography, Geological and thematic maps.
For over 30 years, Emilia-Romagna regional authority has
been working to develop knowledge of the physical environment
of its territory, sharing this knowledge with interested parties. In
1978, thanks to a partnership with Bologna University’s Institute
of Geology (now the Department of Earth Sciences and
Environmental Geology) and the regional Geological Office (now
the Geological, Seismic and Soil Survey), the Region began the
task of producing the Geological Map to scale 1:10,000 of its hill
and mountain territory, starting from two areas in the provinces of
Bologna and Forlì having different geological characteristics. The
positive results achieved subsequently enabled the Region, in
1982, to launch a 10-year project of systematic surveying to scale
1:10,000 of the entire hill and mountain territory, in partnership
with the Departments of Earth Sciences of the Universities of
Bologna, Modena, Padova, Parma, Pavia, Pisa and the CNR
(National Research Council) of Pisa.
Since 1992 Emilia-Romagna Region has been committed to
the national geological cartography project (CARG project)
which has led to the Geological Map to scales 1:25,000 and
1:50,000 of the regional territory and neighbouring areas plus the
digitization of the maps and related geological data.
During the 1990s the Region’s corpus of geological maps
provided the foundations for the elaboration of various maps to
scale 1:250,000: firstly, the Structural-geological Map of the
Emilia-Romagna Apennines (Coord. A. Cerrina Feroni), which
represents the culmination of many years of geological and
cartographic research activities carried out by the Region’s
geological survey in close collaboration with the scientiphic
Community (Universities and the National Research Council),
plus the Seismotectonic Map of the Emilia-Romagna Region
(Coord. M. Boccaletti, L. Martelli), the fruit of a research project
aimed at the comparison, synthesis and representation of
_________________________
(*) Regione Emilia Romagna, Servizio Geologico Sismico e dei Suoli
rpignone@regione.emilia-romagna.it, aangelelli@regione.emiliaromagna.it
RAFFAELE PIGNONE (*) & ANGELA ANGELELLI (*)
294
seismological data and active structures, produced in partnership
with the National Research Council, Universities and the National
Institute of Geophysics and Volcanology (INGV).
Drawing on various maps of a strictly technical-scientific
nature, numerous other thematic maps to various scales have also
been produced: to scale 1:250,000 the Masterplan on Geoenvironmental
Hazards, the Landslide Susceptibility Map of the
Emilia-Romagna Region – Landslide Relative Hazard Map for
Civil Protection Purposes, the Geological Map of the Emilia-
Romagna Plain and the map of the Geological Landscape of
Emilia-Romagna; the Landslide Inventory Map to scale 1:25,000
and the maps of Geo-environmental Itineraries (scale from
1:15,000 to 1:60,000).
The considerable body of knowledge accrued in relation to
the regional territory has also made it possible to conduct a
census of the assets of the Geological Heritage and Geosites, the
primary objective of which is to safeguard and enhance the most
important areas from a scientific and popularization point of
view.
Along with cartographic activities, geological data has been
stored in a georeferenced digital archive, supporting the creation
of separate thematic databases which are currently housed in a
single repository, the geodatabase of the Geological, Seismic and
Soil Survey.
The main activities which Emilia-Romagna Region will focus
on in the future, in addition to the completion of geological
mapping of the lower plain, are:
- the most far-reaching liberalization possible, using web-gis
tools, of all basic, scientific, applicative and educational
information acquired to date;
- the compilation of educational maps for an increasingly
broad audience;
- the compilation of applicative maps with a view to
enhancing and safeguarding natural resources (water and soil)
and hazard maps (slope stability, seismic microzonation).
- the maintenance and updating of basic geological maps,
although this activity requires resources and funding which are
currently difficult to come by.

Key words: Geological mapping, Vesuvius, Volcanic Risk
Cartography represents a fundamental instrument inside the
volcanic risk definition. This fact is particularly true in the case of
densely populate areas and in areas that were populate from the
antiquity. This is the case of Vesuvius. In this very densely
populated land cartography become the synthesis of a number of
disciplines, such as Geology, Volcanology, Archaeology and
History. In the event under investigation, the new cartography of
detail produced through the synergy of these various kinds of
information has allowed to modify in substantial way the zoning
of the risk from opening of eruptive fractures in the territory of
the municipalities of Torre del Greco and Ercolano (Fig.1), with
serious implications for the future management of these
territories.
This job has drawn origin from some question marks left
opened from the archaeomagnetic dating of the lavas from the
eruptive period comprised between the 79 and 1631. The
produced archaeomagnetic dating had put in evidence the
presence of a certain number of lavas of medieval age,
outcropping all along the Vesuvius coast, of which many
generated from eccentric vents positioned at the foot of the
volcanic cone. Between issues left opened from this job, there
was the possibility of a double dating for a lava flow known in
the local literature with the name of Calastro. This lava flow has
been possible to date by means of the archaeomagnetic method to
X century BC or to IX-X century BC. This fact is due to the
incertitude of the Curve of Secular Geomagnetic Variation in this
lapse of time. The archaeological study of BREGLIA (1938)
describing the Roman remnants in the Calastro area has allowed
to clear this matter and clearly attribute Calastro lava to the
medieval period. In addition the entire Calastro lava flowing way
has been reconstructed, with two remarkable points at least: (i)
the emission vent of this lava flow is placed inside Torre del
Greco, in a garden of a nursing home; (ii) the Calastro lava flow,
before reaching the sea, pass troughs a morphological step. This
morphologic climbs has interpreted to the continuation towards
_____________________________
Geological mapping inside densely populated volcanic areas.
The example of Torre del Greco and Ercolano (Vesuvius)
CLAUDIA PRINCIPE (*), ANNARITA PAOLILLO (**), GIUSEPPE LUONGO (**) & MARINA BISSON (•)
(*) Istituto di Geoscienze e Georisorse CNR Pisa, c.principe.igg.cnr.it
(**) Dipartimento di Geofisica e Vulcanologia, Università Federico II, Napoli
(•) Istituto Nazionale di Geofisica e Vulcanologia, sezione di Pisa
295
North-West of the morphologic high from the Castello of Torre
del Greco. These morphologic anomalies represent how much
remains of a coast top-line. This coast line has been, tentatively,
attributed in this work to the main phase of the Versilian
transgression (approximately 5600 Y BP). All the two medieval
lavas outcropping in the studied area (or Calastro that the
neighbor lava flow of “Scogli della Scala”) have had to exceed
this climb before reaching the sea. Successively the morphology
of the coast has been partially flattened from the arrival of the
pyroclastic flows of the eruption of 1631, than have interposed
between a tap and the other and whose covered towards sea it has
been in the present job controlled and confronted with the
historical record opportunely analyzed.
Another incoherence between the historical cartography and
the job of PRINCIPE et alii (2004) was the medieval age (eruption
of 1006-07) of lava flow found near the “Vesuvius Café”, a tap
that in the map of Hon 1861 turned out attributed to the eruption
of 1697. Taken care of a re-examination of the historical
descriptions of the eruption of 1697 (e.g. in SORRENTINO, 1739)
and the course of the lavas, and the on field evidences, has
allowed to carry out a new cartography of 1797 lavas, that in
reality finished its race hardly to the escape of Fosso dei Cervi,
than of medieval lava flow of the Vesuvius Café, that arrested its
flow against the morphologic relief of the Calastro vent.
Holding in consideration also the positioning of tectonic
trends present in this area and particularly the so-called “Faglia di
Torre del Greco” described for the first time into the geological
literature by FINETTI &MORELLI (19765), from our job results the
picture of a zone of strong structural weakness, where a sure
number of eruptions at least in the last 2000 years has opened
eccentric mouths from witch lava flows outpoured, interesting a
territory today strongly inhabited. The last one of these eruptions
in time order is the eruption of the 1861 of which Luigi Palmieri
described and mapped not only the eruptive phenomena and the
cartography of the lavas, but also the location of an impressive
trend of fractures that affected the slopes of the Gran Cono
Vesuviano up to the sea.
Finally, if we confront the obtained geologic paper through
this multidisciplinary job, with the paper at the scale 1:15,000
produced by SBRANA &SANTACROCE in 2003, it turns out
obvious that the risk implications that can be drawn from these
two maps, that bring back a different cartography, are
absolutely different. On one side the risk for the opening of
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eruptive fractures remains confined to the Northern portion of the
territory of Torre del Greco, from the other the area to risk
assumes the form of the very widest one wraps that from the base
of the Great Cone arrives till the sea. It is obvious, therefore, that
when it is in game much screw human like in the event of the
Vesuvius and more than 700,000 people who live to its feet, the
maximum effort must be made in order to exceed the cultural
barriers between different disciplines and face the hard and dusty
work on the field that the job of the cartographer demands.
Fig. 1 – Morphology of the territories comprises in the Torre del Greco and
Ercolano Municipalities
REFERENCES
FINETTI I. & MORELLI C. (1976) - L'Esplorazione sismica a
riflessione dei golfi di Napoli e Pozzuoli. Boll. Geof. Teor.
App., 16, 175-221.
PRINCIPE C., TANGUY J.C., ARRIGHI S., PAIOTTI A., LE GOFF M.
&ZOPPI U. (1976) – Chronology of the Vesuvius activity from
A.D. 79 to 1631 based on archaeomagnetism of lavas and
historical sources. B. Volcanol., 66, 703-724.
SBRANA A. & SANTACROCE R. (EDS) (2003) – Carta geologica
del Vesuvio. Scala 1:15.000. S.E.L.C.A., Firenze.
SORRENTINO I. (1739) – Istoria del Monte Vesuvio. Napoli,
Severinbi, 228.
296

Employment of portable gamma-ray spectrometer in survey and mapping of
intrusive complexes: a case study from the Buddusò pluton (Sardinia)
Key words: Buddusò pluton, portable gamma-ray spectrometer,
radioactivity, Sardinia-Corsica Batholith.
This work illustrates the preliminary data concerning the
employment of a portable gamma-ray spectrometer in survey and
mapping of intrusive complexes.
To discriminate among different intrusions, which are
generated from different magmatic pulse in composite batholiths
made up of coalescent plutons, is not an easy task, particularly if
different intrusions with similar petrofacies come into contact.
Fig. 1 – Portable gamma-ray spectrometer.
ANTONIO PUCCINI (*), STEFANO CUCCURU (*), DANIELE SECHI (*), GIACOMO OGGIANO (*),
FABIO MANTOVANI (°), GERTI XHIXHA (°) & SARA MARIANI (**)
However, if textural and modal features are indistinguishable, the
only effective way able to discriminate such intrusions is the
chemical analysis of trace element, the cost of which is rarely
sustainable when the aim of the survey is the production of a
geological or thematic (dimension stone) map.
For this purpose a portable gamma-ray spectrometer at the
National Lab of Legnaro (INFN) was developed. The equipment
_________________________
(*) Dipartimento di Scienze Botaniche, Ecologiche e Geologiche –
Università di Sassari, scuccuru@uniss.it
(°) Dipartimento di Fisica – Università di Ferrara
(**) Centro di Geotecnologie – Università di Siena
297
consists of one liter thallium-activated sodium iodide scintillator
[NaI(Tl)], digiBASE by ORTEC and a netbook which manages
also humidity and temperature sensors. By using the Jradview
software is possible to process the data in real time and to
determine uranium and thorium (in ppm), expressed as equivalent
units, and potassium concentration (in %) as well as total activity
expressed in Bq kg -1 . Following the IAEA guidelines (IAEA-
TECDOC-1363 (2003)), the gamma-ray spectroscopic analysis is
performed by monitoring three spectral windows: 1.37-1.57 MeV
for 40 K , 1.66-1.86 MeV for 214 Bi and 2.41-2.81 MeV for 208 Tl.
The concentrations of U/Th are estimated by 214 Bi/ 208 Tl
decays, under the assumption that the U and Th decay series are
in secular equilibrium. This occurs when the parent half life is
much longer than the daughter half life and then the number of
atoms of a daughter isotope essentially becomes constant after
some time. Two conditions are necessary for secular equilibrium.
First, the parent radionuclide ( 238 U/ 232 Th) must have a half-life
much longer than that of any other radionuclide in the series.
Second, a sufficiently long period of time must have elapsed, to
allow for ingrowth of the decay products. The state of secular
equilibrium in natural uranium and thorium ores is significantly
altered when they are processed to extract specific radionuclides,
in particular Ra and Rn.
Assuming secular equilibrium we aimed to test the usefulness
of this tool in geological mapping and in the identification of
coalescent plutons which form the batholiths. The handiness of
the instrument, the possibility of in situ measurement and, above
all, the immediacy of the results in the outcrop, may be of
considerable advantage in the expeditious survey of intrusive
complexes.
Sardinia is an ideal testing area because a large portion of the
Sardinia-Corsica Batholith is well exposed, consisting of several
coalescent intrusions which often are very similar from textural
and compositional point of view.
A campaign of measures on different intrusions and on their
internal facies was therefore carried out. The acquired data
highlighted that similar petrological facies of different plutons
showed substantially different values of the considered nuclides.
At the same time measurements made on slightly different facies
belonging the same pluton showed comparable values.
We decided to focuse the tests on the Buddusò pluton and its
host intrusions. The Buddusò pluton (BRUNETON &ORSINI, 1977;
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Fig. 2 – K-eTh and K-eU graphs. P: Pattada Pluton; C: Concas Pluton; BE: Benetutti pluton; L: M.te Lerno Pluton; SC: Sos Canales Pluton; T: Alà dei Sardi-Tepilora
Pluton; BU: Buddusò Pluton (vertical lines: tonalites-granodiorites; horizontal lines: monzogranites – leucomonzogranites).
ORSINI &FERNANDEZ, 1987; BARBEY et alii, 2008) is a relatively
small intrusion (about 70 km 2 ), with an internal structure of
concentric shells which shows a normal magmatic differentiation
from tonalitic-granodioritic facies in the external shell to
monzogranitic and leucomonzogranitic facies in the core. This
pluton is surrounded by the Concas, Sos Canales, Benetutti,
Monte Lerno, Pattada and Alà dei Sardi-Tepilora plutons which
range from the tonalities-granodiorites to leucomonzogranites.
All the acquired measurements were plotted on K-eTh and KeU
graphs which showed that the data arrange themselves
forming populations corresponding to the different plutons (Fig.
2).
Taking into account only the Buddusò values, we noted that:
- an internal subdivision is present which corresponds to the
different petrological terms that constitute the intrusion (tonalitesgranodiorites
and monzogranites-leucomonzogranites);
- there is a direct correlation from tonalites to
leucomonzogranites and K and eU abundance. Instead the
abundance of eTh appears less correlated;
- measurements made close to the contacts between different
facies of the intrusion show transitional values between those of
tonalitic-granodioritic and monzogranitic facies, whereas an
appreciable differences rise between monzogranitic and
leucomonzogranitic terms.
Conversely the granodiorites and tonalites of the Pattada
intrusive unit, which are similar and seems continuous with the
Buddusò intrusion, show meaningful difference in K/U and,
particularly in K/Th ratios. As for the monzogranites and
leucomonzogranites striking differences rise between the similar
terms of Buddusò and P.ta Tepilora, M.te Lerno, Concas and
Benetutti granites which as supposed belong to different intrusive
pulses.
This first experimental test seems to encourage the
employment of portable gamma-ray spectrometer as an aid in the
expeditious survey of intrusive complexes. In fact our data show
that K, eU and eTh concentrations of cogenetic facies (belonging
298
the same pluton) are similar. Conversely, granitoids showing
similar petrofacies but belonging to different intrusive units, show
different concentration of the three considered nuclides.
REFERENCES
BARBEY P., GASQUET D., PIN C. & BOURGEIX A.L. (2008) -
Igneous banding, schlieren and mafic enclaves in calcalkaline
granites: the Budduso pluton (Sardinia). Lithos, 104,
145-163.
BRUNETON P. & ORSINI J.B. (1977) - Le massif granitique de
Budduso: une seule intrusion de type zoné concentrique.
Compt. Rend. Acad. Sci. Paris, 284, 151-154.
ORSINI J.B. & FERNANDEZ A. (1987) - Signification de la
discordance structurale entre fluidalité magmatique et
zonalité pétrographique dans les intrusions de granitoides:
l’exemple de l’intrusion de Budduso. Compt. Rend. Acad.
Sci. Paris, 304, 993-996.
IAEA-TECDOC-1363 (2003) - Guidelines for radioelement
mapping using gamma ray spectrometry data.

The new geological map of the San Pietro Island (Sardinia, Italy)
ROBERTO RIZZO (*), FILIPPO MUNDULA (**) & RAFFAELLO CIONI (**) (°)
Key words: CARG project, San Pietro Island, welded
ignimbrites.
The new 1:50,000 geological map of San Pietro Island
(Sardinia, Italy), prepared in the framework of the CARG project,
is presented here. San Pietro Island (SPI) is located 7 km at the
south-western tips of Sardinia, and it is part of the Sulcis
archipelago, along with S. Antioco and minor islets. It is
completely formed by volcanic terrains (TARICCO, 1934) from the
Sulcis Volcanic District (SVD). Volcanic activity in the SVD is
represented by a succession more than 500 m thick (ASSORGIA et
alii, 1990; MORRA et alii, 1994), and related deposits have been
grouped into a Lower Sequence and an Upper Sequence (MORRA
et alii,1994):
1) The Lower Sequence dates back to 28.4-17.0 Ma
(BECCALUVA et alii, 1985; MORRA et alii, 1994). It is dominated
by calc-alkaline basaltic to intermediate lavas and subordinate
pyroclastics erupted from vents located in the southern part of the
SVD (Carbonia, Narcao, Giba and southern S. Antioco Island).
2) The Upper Sequence is dated between 17.6 and 13.8
(MORRA et alii, 1994) or between 18.6 and 15.1 Ma (PASCI et
alii, 2001). Volcanic activity was characterized by the emission
of large-volume dacitic to rhyolitic ash flows with calc-alkaline to
peralkaline affinity, and subordinate peralkaline lavas (ASSORGIA
et alii, 1990, MORRA et alii, 1994).
The volcanic products cropping out on the SPI were
subaerially emplaced during Langhian (Middle Miocene),
probably in a time span of about 1 Ma starting from 15.8 Ma
(PIOLI & ROSI, 2005). They mainly consist of large volume
ignimbrites and by minor volumes of comenditic lava flows, and
epiclastic deposits. The general stratigraphy of the SPI was first
described by TARICCO (1934) and revisited by GARBARINO et alii
(1985, 1990). The SPI succession includes 11, mainly high-grade
_________________________
(*) Progetto CARG–Sardegna, Cagliari
(**) Dipartimento di Scienze della Terra, Università degli Studi di Cagliari,
mundula@unica.it, rcioni@unica.it
(°) INGV, sezione di Pisa
Lavoro eseguito nell’ambito del progetto CARG con il contributo
finanziario dell’Università di Cagliari.
299
ignimbrites, separated by paleosoils and minor, not very extended
pyroclastic and epiclastic products. This volcanic succession can
be well related to the Upper Sequence of SVD successions and
has been subdivided into three Groups (MUNDULA et alii, 2009):
M. Sirai, Cala Lunga and Punta delle Colonne.
The geological peculiarity of the island is the presence of a
peralkaline rhyolitic lavic and ignimbritic succession, interlayered
within the products of the regionally extended calc-alkaline
activity. The most interesting volcanic products at SPI are
represented by variously welded ignimbrites and comenditic lava
flows. No vents or caldera related to the Upper Sequence are
exposed in the SVD, except for some effusive vents on the SPI.
Volcanic products of the SPI offer very good expositions and
uncommon well preserved textures both at the meso- and microscale.
There is no evidence of significant tectonics affecting
volcanic deposits. Only a limited vertical faulting with a
maximum downthrow of 40 m and a tilting not larger than 10°
were recognized to affect the geology of SPI. These conditions
facilitate an in-depth study of the vertical and lateral variations in
welding and syn-deposition deformational textures of the large
ignimbrite deposits.
The high variability of welding intensity of ignimbrites from
SPI allowed to test a simplified method for microscopic facies
classification. This method (MUNDULA et alii, 2009) can be used
for the lithological characterization of ignimbritic units in other
mapping projects.
REFERENCES
ASSORGIA A., FADDA A., GIMENO TORRENTE D., MORRA V.,
OTTELLI L. & SECCHI F.A. (1990) - Le successioni
ignimbritiche terziarie del Sulcis (Sardegna sud-occidentale).
Mem. Soc. Geol. It., 45, 951-963.
BECCALUVA L., CIVETTA L., MACCIOTTA G. & RICCI C. A. (1985)
- Geocronology in Sardinia: results and problems. Rend. Soc.
Min. Petrol. It., 40, 57-72.
GARBARINO C., MACCIONI L. & SALVADORI I. (1985) - Carta
geopetrografica dell’Isola di San Pietro. S.EL.CA, Firenze.
GARBARINO C., LIRER L., MACCIONI L. & SALVADORI I. (1990) -
Isola di San Pietro Carloforte. Cenni di geologia e
vulcanologia. Della Torre Eds., Cagliari 67 pp..
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MORRA V., SECCHI F.A. & ASSORGIA A. (1994) - Petrogenetic
significance of peralkaline rocks from cenozoic calc-alkaline
volcanism from SW Sardinia. Chemi. Geol., 118, 109-142.
MUNDULA F., CIONI R. & RIZZO R. (2009) - A simplified scheme
for the description of textural features in welded ignimbrites:
the example of San Pietro Island (Sardinia; Italy). Boll. Soc.
Geol. It., 128 (3), 615-627.
PASCI S., PIOLI L., PISANU G., ROSI M., SALE V., BENVENUTI E. &
LAURENZI M. (2001) - Tettonica e vulcanismo miocenici nel
Sulcis (Sardegna SW). Geoitalia, III FIST Meeting, 5-8
September 2001 Chieti (Italy).
PIOLI L. & ROSI M. (2005) - Rheomorphic structures in highgrade
ignimbrite: The Nuraxi Tuff, Sulcis volcanic district
(SW Sardinia, Italy). J. Volcanol. Geotherm. Res., 142 (1-2),
11-28.
TARICCO M. (1934) - Geologia del foglio Isola di San Pietro-
Capo Sperone (Sardegna). Boll. R. Uff. Geol. d’It., 59 (2),1-
78, Roma.
300

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The Subsoil Use Atlas of Regione Toscana:
2d mapping of criticalities due to normative overlaps
(*) Laboratorio di Monitoraggio e Modellistica ambientale per lo sviluppo
sostenibile - LaMMA, romanelli@lamma.rete.toscana.it
(**) Regione Toscana – Servizio Geologico Regionale,
guido.lavorini@regione.toscana.it, domenico.morini@regione.toscana.it
STEFANO ROMANELLI (*), GUIDO LAVORINI (**) & DOMENICO MORINI (**)
Key words: Mines, normative concessions and criticalities,
quarries, springs, subsoil, subsoil use, thermal and mineral
waters, web map services, well.
INTRODUCTION
During the last decade, the Servizio Geologico - Regione
Toscana (Tuscany Geological Survey) supplied many raw
geological data in digital format. The most important is the
Geological Map at 1:10.000, a base for any further geological
related work.
The “Subsoil Use Atlas of Regione Toscana” represents one
of the main interesting derived product that integrates most of the
regional geological geodatabases.
This Atlas permits to the decision makers to have an easy but
powerful digital tool concerning the subsoil resources and their
possible exploitation.
MATERIALS AND METHODS
The main porpouse of the Atlas is to discover areas in which
different administrative concessions (geothermal, water, mines
and so on) overlay each other in a way that to determine
normative criticalities.
The first step has been to edit a legend to define the different
criticalities.
Three classes of criticality have been described:
- intersections between concessions of the same type or
concessions involving the exploitation of the same resource;
- exploitation of the resources of the second concession
forbidden by the first one;
- intersections between concessions of different types that
involve the exploitation of different resources tied to restrictions
according to the following laws: DLGS 152/06 Art. 94, LR
301
86/94, LR 38/04.
Another class has been added concerning intersections
between concessions from wich criticalities are not expected.
Layers used for the project have been extracted from many
georeferenced databases developed during the last years from the
Geological Survey of Regione Toscana.
In detail they are:
- subsoil and water resources database (BDSRI). This
database stores technical information about wells, abstractions of
surface water, springs, stratigraphies, piezometers, chemical
analysis and the like for the whole Regione Toscana. This
database homogenizes data derived from many different Local
Authorities. It contains information about more than 200.000
georeferenced points. Only the 2277 wells and the 2822 springs
flowing acqueducts are of interest for this work. Both have two
strict buffer zones of 10 and 200 meters around themselves.
- mineral and thermal waters database (BDCAMT): this
database concerns all the administrative concessions for the
exploitation of mineral and thermal waters for the whole Regione
Toscana. Each concession is delimited by three concentric zones,
with a different degree of constrains for area. The database
contains also hydrogeological, physical and chemical parameters
retrieved from technical reports attached to the concession acts.
The database stores information about 71 concessions, generating
205 constrain areas.
- Layer regarding quarries concessions: the delimitation of
quarries boundaries is an upgrading project, so that this layer is
updated whenever a Province provides new information.
Presently this layer contains 384 polygons.
- Layer regarding mines concessions: in Tuscany there are no
mines still expoloited. Concessions are active only to secure the
area. This layer contains 37 polygons.
- Layer of 8 geothermal concessions.
All the layers and data described above have been collected
into a new Postgresql/Postgis database.
As known Postgis is the spatial extension to “the world's most
advanced database”, Postgresql. An SQL script has been edited
concerning all the possible spatial intersections between the
different constrain zones. Then, the script creates 4 new layers
one for each criticality.
In this way, whenever a layer changes (e.g. the quarries layer),
running the SQL script again allows to obtain an uptdated layer.
Next table shows the number of intersections for each class
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Fig. 1 – example of multiple intersections between concessions of the same type and concessions of different type (see text)
according to the legend described before:
Intersection but no criticality 38
Criticality 1 23
Criticality 2 2
Criticality 3 356
The relevant number in the last class is mostly due to wells
and springs.
In Fig.1 an example of multiple intersections between
concessions is depicted: intersections of the same type (mines),
and different ones (mines and thermal and mineral waters).
Intersection 1 - Sant'Albino mine concession, painted as the
dark grey irregular area, intersects Acquapuzzola Villa Contucci
mine concession, brown (and red) area. The first concession is
completely inside the second one. The criticality is between two
concessions of the same type. These two concessions should not
live together.
Intersection 2 - Acquapuzzola Villa Contucci mine concession
intersects Sant'Albino Thermal and Mineral Water concession
(dark green). The area of intersection is the red one. Neither these
two concessions should live togheter.
Intersection 3 - Sant'Albino mine concession and Sant'Albino
Thermal and Mineral Water concession. These two concessions
302
should not overlap, too.
Next step was the development of an Internet Map Service
retrievable at the following address:
http://159.213.57.103/sotto2d/
FUTURE DEVELOPMENT
The acquifers of Regione Toscana are under definition as
reported in another paper submitted to the proceedings of this
congress. At the moment no criticalities are provided for these
areas, a sharp description of restrictions and related forbidden
activities is expected in a close future. So this layer will be part of
the project as soon as the acquifers will have normative
relevance.
Another development will be the addition of the third
dimension to permit a three-dimensional perspective. The third
dimension will be take in the Internet Map Service too, according
to the OGC standard “Web Perspective View Service”.

SESSIONE 10
I vincoli geologico-strutturali nelle ricostruzioni
dell'evoluzione cinematica della catena alpinoappenninica-maghrebide
CONVENERS
Sabina Bigi (Università Roma "La Sapienza")
Giovanni Musumeci (Università di Pisa)
Enrico Tavarnelli (Università di Siena)
Andrea Zanchi (Università degli Studi di Milano-Bicocca)
303
SESSIONE 10

SESSIONE 10
Time-space evolution of a near-classic thrust and fold belt in the
outer part of the Northern Apennines
MASSIMILIANO R. BARCHI (*), WALTER ALVAREZ (**) & DAVID H. SHIMABUKURO (**)
Key words: Thin skinned tectonics, thrust and fold belts, Umbria-
Marche Apennines.
The Umbria-Marche Apennines (UMA) are an arc-shaped
fold-thrust belt, with eastward convexity and vergence,
representing the outer part of the Northern Apennines. In the late
1980’s, the UMA was interpreted by several authors (e.g. BALLY
et alii, 1986) as a typical thin-skinned thrust belt, whose thrusts
were emplaced in an in-sequence, piggy-back mode, over an
undeformed basement, gently dipping towards the hinterland (i.e.
SW-dipping). The basal décollement (sole thrust), separating the
thrust sheets from the underlying basement, would be located
within a 1500 thick succession of alternated anhydrites and
dolomites (the Late Triassic Burano Fm.).
In this paper we re-examine the tectono-sedimentary evolution
of the UMA, mainly on the basis of: seismic reflection profiles,
imaging the subsurface setting of the thrust belt; stratigraphic
data, constraining the time-space evolution of the syntectonic
foreland basins; and geomorphic observations, such as presentday
topography and evolution of the fluvial network.
We compare the time-space evolution of the UMA tectonic
wedge with the classic model of thin-skinned tectonics, which
describes the steady-state growth of a critical-taper fold-thrust
belt, advancing over an undeformed basement. Considering both
geological and geomorphological features, the UMA can be
divided into two major regions, here named the Eastern UMA
and Western UMA, with a boundary at the western margin of the
main Apennine ridge, passing through Cantiano and Foligno.
Our analysis shows that the Eastern UMA, comprising the
main Apennine ridge and the outer (eastern) ridges and foothills,
generally fits the critical taper model: in fact, moving from the
foreland (NE) towards the hinterland (SW), both the structural
and topographic elevations increase, while the top of the
basement deepens from about 5 to about 12 km. In contrast, the
Western UMA is a topographically and structurally low region,
where Tertiary turbidites extensively crop out and the basement is
much shallower (about 6 km) than below the adjacent and
easternmost mountain ridge.
_________________________
(*) Dipartimento di Scienze della Terra, Università di Perugia,
mbarchi@unipg.it
(**) University of California, Berkeley
304
We also collected and analysed the available stratigraphic and
sedimentological data about the syntectonic clastic wedges of
UMA. Considering these data in detail, we found a major
discontinuity in the evolution and eastward migration of the
foreland basins: in fact there is a jump in the migration of the
foredeep, from Inner Umbria (Late Miocene Marnoso-Arenacea
fm.) to the Marche Foothills (Pliocene-present sediments). This
discontinuity is related to the rise of the Apennines ridge,
occurred during the Tortonian-Messinian time interval.
Summarizing, the departures of the UMA fold-thrust belt
from the classic model are due to the presence of discontinuities
in the depth to basement, the migration history of the foredeep,
and the elevation of the topographic surface. All these
discontinuities occur at the same geographic location (at the
boundary between the Western and the Eastern UMA) and they
possibly reflect the same event, i.e. the rise of an anticlinorial
ridge that was higher than might have been expected, based on
the previously occurred deformation of the Western UMA.
In order to explain the described discontinuities, a wide range
of causative processes can be invoked, that may also have acted
simultaneously. These causes span from “local” (or internal)
causes, related to the thrust belt stratigraphy and evolution, to
“regional” (or external) causes, related to the geodynamic
framework where the thrust belt is formed.
Local causes may include: the effects of surface transport
processes (i.e. syntectonic sedimentation and erosion); the
propagation of the thrust system to deeper structural levels,
involving the upper part of the basement; the effects of tectonic
inheritance on the localization and/or amplification of
contractional structures during mountain building (e.g. BUTLER et
alii, 2006). Regional causes may include the activity of thrusts at
lithospheric scale (LAVECCHIA et alii, 2003); or, in a completely
different geodynamic scenario, different stages of evolution of the
West dipping subduction of the Adriatic slab (e.g. FACCENNA et
alii, 2001).
Finally, some Authors (e.g. DOGLIONI et alii, 1998; BARCHI et
alii, 1998) hypothesized that the Northern Apennines actually
consist of two superposed thrust belts, generated by different
driving mechanisms: the former thrust belt (Etruscan belt), would
be generated as a back-verging response to the collision between
the Alps and the Adriatic lithosphere. The second thrust belt
(Umbrian belt) would be related to the subsequent roll-back and
retreat of the Adriatic litosphere. In this scenario, the low region

of the Western UMA would represent the border between the two
different mountain buildings, which the Northern Apennines
consists of.
REFERENCES
BALLY A.W., BURBI L., COOPER C. & GHELARDONI R (1986) –
Balanced sections and seismic reflection profiles across the
Central Apennines. Mem. Soc. Geol. It., 35, 257-310.
BARCHI M.R., MINELLI G&PIALLI G. (1998) – The Crop 03
profile: a synthess of results on deep structures of the
Northern Apennines. Mem. Soc. Geol. It., 52, 383-400.
BUTLER R.W.H., TAVERNELLI E. & GRASSO M. (2006) –
Structural inheritance in mountain belts: An Alpine-Apennine
perspective. J. Str. Geol., 28, 1893-1908.
DOGLIONI C. et alii (2001) – The Crop 03 profile: a synthess of
results on deep structures of the Northern Apennines. Mem.
Soc. Geol. It., 52, 383-400
FACCENNA C., BECKER T.W., LUCENTE F.P., JOLIVET L. &
ROSSETTI F. (2001) – History of subduction and back-arc
extension in the Central Mediterranean. Geoph. J. Int., 145,
809-820.
LAVECCHIA G., BONCIO P., CREATI N. & BROZZETTI F. (2003) –
Some aspects of th Italian geology not fitting with a
subduction scenario. J. Virtual Explorer, 10, 1-14.
305
SESSIONE 10

SESSIONE 10
Kinematic and timing constraints of the Villalvernia-Varzi line at the
Apennine-Alpine boundary
Key words: Epiligurian Basin, Oligo-Miocene, tectonics,
Tertiary Piedmonte Basin, Villalvernia-Varzi line.
The Villalvernia-Varzi line represents the boundary
between the Tertiary Piedmont Basin, to the south and the
Epiligurian Succession to the north.
According to the seismic and geophysical data, this line has
been interpreted as a high-angle reverse fault along which the
Ligurian units with the unconformable Tertiary Piedmont Basin
at the top thrust the units of the Northern Apennine belt during
the Middle-Late Miocene.
Over 90s the Villalvernia-Varzi line has been interpreted as
a left-lateral strike-slip fault, which, together with the Insubric
line, allowed the indentation of the Adria Plate toward the west
during the Oligo-Miocene.
Despite the relevance of this line for the understanding of
the Alps-Apennine relationships, the field-data able to provide
valuable constraints for the kinematics and timing are almost
lacking.
In this work the results of the study of the Villalvernia-
Varzi line are described starting from a geological-structural
survey performed at detailed scale, from 1:5.000 to 1:2000.
The Villalvernia-Varzi line occurs, in the field, as several
kilometers thick, est-west trending deformation zone, where a
complex arrays of sub-vertical shear zones separate less
deformed areas. The sub-vertical shear zones are represented
by foliated cataclasites showing variable thickness from a few
centimeters to over a meter. The foliated cataclasites are
characterized by a shaly matrix with well developed S-C
surfaces, showing inside boudins of more competent
lithologies. In the map, the orientation of these shear zones
describe a complex Riedel system with R, R’ and P surfaces,
that occur in the field as shiny surfaces where striae and
slickenlines indicate a sinistral shear sense of movement. The
main foliation, which can interpreted as P foliation, is mainly
oriented N120E-N140E and form an angle of about 30° with
_________________________
ANDREA BERNARDESCHI (*), MICHELE MARRONI (*) (°) & LUCA PANDOLFI (*) (°)
(*) Dipartimento di Scienze della Terra, Università di Pisa,
pandolfi@dst.unipi.it
(°) Istituto di Geoscienze e Georisorse, CNR
306
the main direction of the Villalvernia-Varzi line, which is eastwest
trending.
In most of the outcrops, the developement of anastomosing
shear zones isolate lenses of less deformed material. The rockstypes
enclosed between the shear zones can be classified into
two main groups:
1) coherent elements, made up of rock derived from the
Tertiary Piedmont Basin and/or Epiligure Succession, where
original lithology can be still recognized.
2) mélange elements, consisting of a block-in-matrix
texture. The matrix is generally deformed and characterized by
a well developed scaly-fabric.
In order to characterize in detail the rocks involved in the
deformation zone and to identify the possible origin from
adjacent areas, rocks and clasts from the deformed zone have
been analyzed using the contents in calcareous nannofossili.
The blocks (ranging from the ruditic up to the boulder size) are
polygenic and derive from rocks belonging to the Tertiary
Piedmont Basin and/or Epiligure Succession and from
calcilutites referable to Maastrichtian Helminthoid Flysch (cfr.
Antola Fm. and Cassio Fm.) and Hauterivian-Barremian
Palombini Shale.
The younger age recognized in the elements of the
deformed zone is the middle Rupelian (biozone MNP23) while
the deformed zone is sealed by the unconformable deposits of
the Burdigalian-Serravalian Epiligurian Succession (Lumello
Marl and M.Vallassa Sandstone,).
This data support the idea that the fault zone that developed
the mélange elements was active at the Oligocene-Miocene
boundary with a sinistral shear sense. Evidences of younger
post-Miocene reactivation phases are recognized, but they are
represented by minor strike-slip subvertical faults with
displacement of few meters.
Finally, the collected data point out to an important role of
the Villalvernia-Varzi line only in a short time span, i.e. at the
Oligocene-Miocene boundary, during a major reorganization of
the domains at the boundary between the Alpine and Apennine
belts.

__________________
Transpressive evolution of the Ligurian Alps - Northern Apennines
system – 2: a perspective from the Northern Apennines
CARLO BERTOK (°°), ANNA D’ATRI (°°), LUCA MARTIRE (°°), PIETRO MOSCA (°), FABRIZIO PIANA (°),
ANDREA CERRINA FERONI (*), ALESSANDRO ELLERO (*), RITA CATANZARITI (*),
ALESSIA MUSSO (°°), ELENA PEROTTI (°°) & DARIO VARRONE (°)
Key words: Northern Apennines, transpression, Western Alps.
INTRODUCTION
The convergent evolution of the European and Adriatic
continental margins of the Liguria-Piemonte ocean, has been
thought by some Authors (SCHOLLE, 1970; SCANDONE, 1979;
PRINCIPI & TREVES, 1984) as partitioned into two distinct
branches with peculiar geometric and kinematic characters . The
northern branch was characterized by an east dipping (“Alpine”)
subduction, while the southern one by a west dipping
(“Apenninic”) subduction.
From the kinematic point of view, this interpretation, that
explains a large amount of geological observations, implies the
presence of a regional transfer zone (active for several tens
millions years) between these opposite-dipping branches of the
Liguria-Piemonte realm. This transfer zone, was assumed to run
at the northern-eastern boundary of the Western Ligurian Alps,
and in the region between these units and the Northern
Apennines.
In this region, the occurrence of strike-slip or transpressional
tectonics since the Cretaceous up to Late Miocene times is largely
documented by recent data and re-interpretation of large data sets
on the Western and Eastern Ligurian Alps sectors and in the
Tertiary Piemonte basin, as well as on the external boundary of
the Ligurian units of Northern Apennines and their adjacent
Miocene foredeep basins of the Emilia Apennines (CERRINA
FERONI, 1988; CERRINA FERONI et alii, 2004).
Oblique convergent evolution of both european and adriatic
margins of the southern branch of the Liguria-Piemonte ocean is
suggested, to justify a consequent development of several enechelon
kinematic transfer zones, developed distinctly through
(°°) Dipartimento di Scienze della Terra, Università di Torino
(°) CNR - Istituto di Geoscienze e Georisorse, Torino, f.piana@csg.to.cnr.it
(*) CNR - Istituto di Geoscienze e Georisorse, Pisa
307
Cretaceous-Early Miocene times, that could be envisaged, as a
whole, as the regional kinematic transfer required by the model.
As a major consequence, the presence of a single, precisely
located, transfer zone between Ligurian Alps and Northern
Apennines is not necessary if a transpressive-transtensive
evolutionary model for the whole Alps-Apennines junction zone
is suggested.
This topic will be discussed in two separate contributions,
examining the problem respectively from the "Alpine" and
"Apennines" point of view.
The first contribution regards the Ligurian Alps perspective
on the problem, while the second contribution focuses on the
Apennines perspective.
THE LIGURIAN ALPS PERSPECTIVE
This contribution illustrates data and interpretation of the
Cretaceous-Early Miocene tectono-sedimentary evolution of
Western Ligurian Alps at the transition zone between the
Dauphinois and Ligurian Brianconnais domain, where evidences
of pre-Alpine transcurrent tectonics are reported and where
poorly to non-metamorphic Ligurian sedimentary units
(Helminthoides Flysch) are involved within transpressive Alpine
shear zones (PIANA et alii, 2009). Furthermore, the subsurface
and surface structures at the northern boundary of Ligurian Alps
are described, where Ligurian meta-ophiolites are in contact with
Helminthoides Flysch and with the Oligo-Miocene succession of
the syn-orogenic Tertiary Piemonte Basin (MOSCA et alii, 2009).
REFERENCES
CERRINA FERONI A. (1988) – La duplicazione della catena a
falde, per trascorrenza longitudinale, nell'Appennino
settentrionale: una soluzione alternativa. Rend. Soc. Geol.
It., 11, 325-328.
CERRINA FERONI A., OTTRIA G. & ELLERO A. (2004) – The
Northern Apennine, Italy: geological structure and
transpressive evolution. In: U. Crescenti, S. D’Offizi, S.
SESSIONE 10

SESSIONE 10
Merlini and L. Sacchi (Eds.) - Geology of Italy - Special
Volume of the Italian Geological Society for the IGC 32
Florence – 2004, 15-32.
MOSCA P, .POLINO R., ROGLEDI S& ROSSI M. (2009) - New data
for the kinematic interpretation of the Alps–Apennines
junction (Northwestern Italy) Int. J. Earth Sci (Geol.
Rundsch.) DOI 10.1007/S00531-009-0428-2
PIANA F., MUSSO A., BERTOK C., D’ATRI A., MARTIRE L.,
PEROTTI E., VARRONE D., MARTINOTTI G. (2009) – New data
on post-Eocene tectonic evolution of the External
Brianconnais (Western Ligurian Alps). J. Geosc., (Boll. Soc.
Geol. It.), 128, 2, 353-366, DOI 10.3301 /
IJG.2009.128.2.353.
PRINCIPI G. & TREVES B. (1984) – Il sistema Corso-Appenninico
come prisma di accrezione. Riflessioni sul problema generale
del limite Alpi Appennini. Mem. Soc. Geol. It., 28, 548-576.
SCANDONE P. (1979) – Origin of the Tyrrhenian Sea and
Calabrian Arc. Boll. Soc. Geol. It., 98, 27-34.
SCHOLLE P.A. (1970) – The Sestri-Voltaggio line: a transform
fault induced tectonic boundary between the Alps and the
Apennines. Am. J. Sci., 269, 343-359.
308

The complex lithosphere structure of Central Apennines as revealed
by combined Tomographic and Receiver Functions images
Key words: Central Apennines, Tomography, Receiver
Functions.
INTRODUCTION
The Apennines of Italy is a manifest example of a complex
tectonic environment. As part of the Mediterranean Alpine belt,
it results from the emergence of the accretionary wedge formed
during the westward subduction of the Adriatic slab after the
consumption of the Tethys ocean.
In this study, we use the techniques of Receiver Functions
and Tomography to describe the features in central Apennines,
from the very peculiar anomalies found in the crust, to the
lithosphere-asthenosphere boundary (LAB). Results are shown
along transects across the belt, from the Tyrrhenian to the
Adriatic Sea.
The application of these two different and independent
techniques yields new and original information on P- and Svelocities,
relevant to improve our understanding of the
tectonic environment.
We document strong lateral and vertical heterogeneities in
the crust, that define shallow sheets of the Mesozoic cover that
overlay high Vp and high Vs bodies interpreted as either
dolomitic or partially hydrated mafic rocks.
These bodies are likely involved in the evolution of the
thrust-and-fold belt. Except for a low Vs layer located above
the Moho interface, the crust is characterized by unusually high
Vs values. These high Vs anomalous bodies, partially
associated with high Vp, may be related to sheets of lower crust
and mantle material involved in the crustal roots of the chain.
The low Vs layer located above the Moho may be a
consequence of the presence of fluids released by the hydrated
_________________________
IRENE BIANCHI (*), GENNY GIACOMUZZI (°) (*), CLAUDIO CHIARABBA (*), RAFFAELE DI STEFANO (*),
NICOLA PIANA AGOSTINETTI (*) & ALESSANDRO AMATO (*)
(*) Istituto Nazionale di Geofisica e Vulcanologia, Sezione CNT
irene.bianchi@ingv.it
(°) Università di Bologna
309
upper mantle. The Tyrrhenian mantle shows low velocities
from the Moho to about 80-100 km depth, making the LAB
almost transparent; towards the belt axis the LAB interface
becomes more pronounced and it is clearly delineated in the
external Adria domain.
Here the Moho is located at about 22-24 km and the mantle
displays high S-wave velocities.
The features just described testify for an extremely complex
lithosphere structure, not easily reconcilable with classical and
simple models of westward subduction of Adria, and the
inherited structure of the Tethys passive margin may have
played a role in the evolution of the Apennines wedge.
SESSIONE 10

SESSIONE 10
Evolution of the Oligocene-Miocene foredeep successions in the
Toscana-Umbria area: constraints from stratigraphical,
biostratigraphical and petrographical data
Key words: Foredeep successions, Macigno Fm., Marnoso-
Arenacea umbra Fm., Montagnaccia Fm., Northern
Apennine.
INTRODUCTION
The analyses of the Oligo-Miocene siliciclastic deposits of the
Northern Apennine thrust-and-fold belt are a useful tool to
recontruct collisional and post-collisional stages connected with
the building of the chain.
The Northern Apennines evolution is characterized since the
Late Oligocene by a continous migration of the thrust beltforeland
system associated to the development of thick foredeep
turbidite successions (the Late Oligocene - Early Miocene
Macigno Fm. and the Middle to Late Miocene Marnoso-Arenacea
Fm). Whereas the features of these deposits are well known, less
information are available about their transition, whose remnants
are well exposed in the Tuscany-Umbria area.
In this paper, an integrated approach on the Oligocene-
Miocene foredeep successions outcropping in the Trasimeno
Lake area is proposed, in order to provide useful constraints for
the regional correlations across the Northern Apennines.
OLIGO-MIOCENE FOREDEEP DEPOSITS
In the Tuscany-Umbria area three different foredeep
siliciclastic successions can be identified. Their differences in age
and in the arenite composition can be interpreted as the result of
the shifting in space and time of the depocentre of the Oligocene-
Miocene foredeep, connected with the eastward progressive
migration of the thrust belt-foreland system.
The oldest foredeep deposit is the Macigno Fm, cropping out
_________________________
(*) Dipartimento di Scienze della Terra - Università di Pisa,
fbotti@dst.unipi.it
(°) Istituto di Geoscienze e Georisorse – C.N.R., Pisa
FLAVIA BOTTI (*), MICHELE MARRONI (*) (°), SILVIA PALANDRI (*),
LUCA PANDOLFI (*) (°) & NICOLETTA RICCHETTI (*)
310
in western part of the study area (Fig. 1). It belongs to two
tectonic units: the western Tuscan Nappe (TN) and eastern
Sansepolcro-Monte Filoncio Unit (SFU – BARSELLA et alii,
2009). In the Macigno Fm, three members have been
distinguished, referred, from bottom to top, as arenaceous Molin
Nuovo, arenaceous-pelitic Poggio Belvedere and peliticarenaceous
Lippiano members. The Macigno Fm. overlies the
Scaglia Toscana Fm, characterized by Calcareniti di Dudda
member, in the TN, and Filoncio member in the SFU. Its
stratigraphic base becomes progressively younger eastward as
suggested by the inception of the siliciclastic turbidites foredeep
in Chattian age (MNP25a Biozone), in the TN, and in
Chattian/Aquitanian boundary (MNN1a Biozone) in the SFU. In
this area top of the Macigno Fm, is always Aquitanian in age.
A fine-grained rock fragments compositional trend has been
recognized in the sandstone of the Macigno Fm., In the lower part
(Molin Nuovo and Poggio Belvedere p.p. members) the
metamorphites and volcanic fine-grained rock fragments are
dominant (Lm42-59 Lv30-38Ls+CE6-20), whereas a progressive
upward decrease of the volcanic fragments characterizes the
sandstones composition of the upper portion (Lippiano member),
that becomes metamorphite-dominated (Lm84-99-Lv1-11-
Ls+CE1-8).
The Montagnaccia Fm, is the transitional foredeep succession
located between the Tuscan and Umbria-Marche domains. This
formation outcrops at the stratigraphic top of the Rentella Unit
(BROZZETTI et alii, 2000), located between the Tuscan Nappe (at
the hangingwall), and the Umbria-Romagna Unit (at the
footwall).
The Montagnaccia Fm, is represented by arenaceous-pelitic
beds alternating with decametre intervals of thin-fine marly beds;
in the lower portion a level of black cherty centimetre bands and
silica-rich horizons are present, as commonly detected in all
Aquitanian-Burdigalian successions of the Northern Apennine.
These foredeep siliciclastic deposits Aquitanian-Burdigalian in
age (MNN1d/MNN2a Biozones) have a fine-grained rock
fragments compositional mode Lm52-78Lv2-10Ls+CE12-45,
comparable with that of Marnoso-Arenacea Fm, of Alpine
provenance.

Fig. 1 – Structural sketch-map of Tuscan-Umbria area and related
geological cross-section A-B. (1) Calcareniti di Dudda member: Poggioni
lithofacies; (2) Calcareniti di Dudda member: Montanare lithofacies; (3)
Montagnaccia Fm.: cherthy lithofacies.
The Montagnaccia Fm, lies stratigraphically above a foreland
succession consisting of Rupelian-Aquitanian (MNP24-MNN1d
Biozones) varicoloured pelagic and grey hemipelagic, marls and
marly-shales (Monte Rentella Fm,). In the Monte Peglia area, at
the botton of the Monte Rentella Fm, a carbonatic succession
311
showing transitional lithostratigraphic features between the
Scaglia toscana Fm, and the Umbria Scaglia Fms occurs. From
the top, this carbonatic succession is characterized by a
Thanethian–Rupelian varicoulored calcareous marls (NP6-
MNP23 Biozones) showing downward a gradual transition to a
white and pink limestone with red chert nodules, Turonian p.p.-
Selandian in age (Helvetoglobotruncana helvetica Zone – NP5
calcareous nannofossil Biozone). These two lithotypes have been
informally names as marly and calcareous members of the Scaglia
di Monte Peglia Fm,, respectively.
The lower part of stratigraphic succession of the Rentella Unit
is very similar with the Umbria-Marche one, as suggested by the
occurrence downward of 20 m of Scaglia Bianca Fm, (here is not
present Livello Bonarelli), 70 m of Marne a Fucoidi Fm, and at
least 150 m of limestones belonging to the Maiolica Fm,. In the
Tuscan-Emilian Apennine a very similar succession is described
in the “Suviana well” (ANELLI et alii, 1994) at the base of the
Aquitanian - Burdigalian siliciclastic turbidites analogous to
Montagnaccia Fm.,
Marnoso-Arenacea Fm. is the more external foredeep deposits
belonging to the Umbria Romagna Unit. In the study area this
siliciclastic deposits are Burdigalian-Langhian in age and they are
represented only by the Casa Spertaglia member. This member,
consists of thin-fine arenaceous-pelitic turbidites. made up of a
CE-dominated fine-grained rock fragment association (Lm30-51-
Lv1-12-Ls+CE37-69).
All these data allow an Oligo-Miocene paleogeographic
reconstruction of the Northern Apennine foredeep. Particulary the
the Rentella Unit can be considered a transitional succession
located between the Tuscan and Umbria-Marche domains. Based
on the age, the compositional mode of the turbidite sandstones,
and structural position, the Rentella Unit can be compared to the
Carigiola Unit outcropping in the Tuscan-Emilian Apennine.
REFERENCES
ANELLI L., GORZA M., PIERI M. & RIVA M. (1994) - Subsurface
well data in the Northern Apennines (Italy). Mem. Soc. Geol.
It., 48, 461-471.
BARSELLA M., BOSCHERINI A., BOTTI F., MARRONI M.,
MENEGHINI F., MOTTI A., PALANDRI S. & PANDOLFI L. (2009)
- Oligocene-Miocene foredeep deposits in the Lake
Trasimeno area (Central Italy): insights into the evolution of
the Northern Apennines. It. J. Geosci.,128(2), 341-352.
BROZZETTI F., LUCHETTI L. & PIALLI G. (2000) – La successione
del Monte Rentella (Umbria Occidentale): biostratigrafia a
nannofossili calcari ed ipotesi per un inquadramento
tettonico regionale. Boll. Soc. Geol. It., 119, 407-422.
SESSIONE 10

SESSIONE 10
The structural and kinematic history of a complex fold-and-thrust
belt: an example from western Basilicata, southern Italy
FRANCESCO BUCCI (*), PAOLA GUGLIELMI (**), IVANA ADURNO (°), ROCCO NOVELLINO (*), ENRICO TAVARNELLI(*),
ERWAN GUEGUEN (°) & GIACOMO PROSSER (**)
Key words: Agri Valley, Lucania, Melandro Valley, Southern
Apennine fold-and-thrust belt, structural analysis.
INTRODUCTION
The repeated opening and closure of oceans along the same
trends, and the consequent fragmentation and reassemblage of
continents, has long led to the concept of a cyclical recurrence
in orogenic events, and a certain cyclical pattern is commonly
recognised in the evolution of fold-and-thrust belts. Orogenic
cycles generally involve two extensional stages, namely preorogenic
and post-orogenic extension, separated by an
intervening stage of contraction. However, when seen in greater
detail, the evolution of fold-and-thrust belts is generally more
complex. In fact, numerous studies from both active and fossil
orogenic belts outline that the inferred histories are punctuated
by the superposition of kinematically different structures, thus
making each example a specific, distinct case. Moreover, the
complete history of a fold-and-thrust belt is usually inferred
from numerous observations carried out at different localities
sparse over wide areas, whereas the entire sequence of
structural stages is very rarely preserved within orogenic
segments of limited extent.
In this contribution we anticipate the results of a structural
investigation carried out along the central sector of the
Apennines fold-and-thrust belt of western Lucania, southern
Italy. The data inferred from this study made it possible to
reconstruct the complete deformation history of the central
province of the southern Apennine belt, where documentation
of well-constrained deformation episodes is integrated with
recognition of previously unreported structures. The study area
is located between the Melandro and Agri valleys, and
comprises the villages of Savoia di Lucania, Vietri di Potenza,
Marsico Vetere and Viggiano (Fig. 1).
_________________________
(*) Dipartimento di Scienze della Terra, Università di Siena
(**) Dipartimento di Scienze Geologiche, Università della Basilicata
(°) Istituto per le Metodologie di Analisi Ambientale (IMAA) – Consiglio
Nazionale delle Ricerche (CNR)
312
GEOLOGY OF THE MELANDRO AND AGRI
VALLEYS
The geological history of the area that extends between the
Melandro and Agri valleys mimics that of the Lucanian
Apennines, an arcuate fold-and-thrust belt developed due to
imbrication of different tectonic units, namely the Ligurian,
Apenninic and Lagonegro Units, onto the Apulian foreland.
These tectonic units, differentiated since Triassic time, were
originated in distinct palaeogeographic domains that are are,
from West to East: i) the ocean-derived Ligurian Basin; ii) the
Apennine Carbonate Platform; iii) the Lagonegro Basin, and iv)
the Apulia Platform. Differentiation of the paleogeographic
domains was controlled by syn-sedimentary, pre-orogenic
normal faults developed during the rifting stage that led to
opening of the Mesozoic Tethys Ocean and to drifting of the
African (i.e. Adria) and European continental plates Our
investigation has led to recognition of previously unreported
Fig. 1 – Tectonic sketch map of the Southern Apennines showing the location
of the study area.
pre-orogenic normal faults whose Jurassic age is contrained by
the stratigraphic record of syn-rift deposits. From Eocene time
onwards the paleogeographic domains experienced contraction
related to the subduction of the Tethys Ocean, to the collision
of the European and African plates, and to the contraction of
the Adria continental margin, with development of the thrustbounded
tectonic units. Consistently with observations by
PATACCA &SCANDONE (2007) and by MAZZOLI et alii (2001),
thrust propagation was locally preceded and accompanied by
buckling of the rheologically more competent stratigraphic
units embedded between less competent shaly and marly units.
Development of kink and box folds at both regional to local
scales can be related to this early shortening episode. The most
remarkable box fold is exposed along the left flank of the Agri

iver. Here, the competent multilayer consists of well bedded
pelagic limestones and cherts of the Calcari con Selce and
Scisti Silicei formations (Late Triassic to Jurassic) that overlie
shales with thin-bedded limestone intercalations of Late
Triassic age (Sorgente dell’Acero Member). This unit shows
development of intense cleavage and widespread calcite veins
since it represents the detachment level that allowed buckling
of the overlying Late Triassic-Jurassic strata. The occurrence of
shale and marl of the Lower Cretaceous Galestri Formation
above the competent multilayer further facilitated the buckling
process. The box fold shows steeply dipping to overturned
limbs and a nearly constant N10-trending axis. Different orders
of parasitic folds are particularly well developed in the
transitional interval between the Calcari con Selce and the
Scisti Silicei formations. Orientation and asymmetry of
parasitic folds is consistent with trend, geometry and style of
the host, large-scale box fold.
Pre-orogenic normal faults related to the opening of the
Tethys Ocean were overprinted by thrust propagation, as
outlined by relations observed in the central part of the
investigated area where the Apennine Platform Unit overrides
the Lagonegro Units. In this sector brittle and ductile structures
can observed at both mesoscopic and macroscopic scales.
Between Vietri di Potenza and S. Angelo le Fratte, the thrust of
the Apennine Platform Unit is associated to a 5 km long, NW-
SE oriented shear zone in the Lagonegro Units, mainly
developed in the transitional interval between the Calcari con
Selce and Scisti Silicei formations. Along the shear zone, slices
of the Calcari con Selce Formation are often arranged into 20-
30 m thick duplex structures, whereas marly and clayey
lithologies of the Transition Interval and of the Scisti Silicei
Formation are involved in overturned folds, often with evidence
for hinge collapse, S-C shear fabrics, small-scale duplex
structures and imbricated horses.
Klippen of platform dolomites, outcropping east of the
shear zone, show the extent of the Apennine platform in the
hanging-wall of the main thrust. Interestingly, the base of the
klippen truncates earlier folds within Lagonegro Units and
involves slices of the basinal Flysch Rosso Fm. of Cretaceous-
Oligocene age. The easternmost part of the shear zone is
characterized by outcrops of a tectonic mélange containing
disrupted sandstone layers of the Miocene Monte Sierio
Formation, including olistoliths of Jurassic limestones from
Apennine Platform Units. Stacking of the tectonic pile
continued regionally throughout the Early Miocene-Pleistocene
time interval and progressively migrated eastwards, i.e. towards
the Apulian foreland. From Late Miocene time onwards
thrusting was followed by the onset of extensional deformations
that overprinted contractional structures and migrated
progressively towards the front of the belt.
The most recent structures related to the extensional
episode are high-angle normal faults that are clearly visible
along the northeastern edge of the Agri Valley. These faults are
replaced to the south by left-lateral strike-slip faults, analogue
to those described at the Lucania-Calabria boundary by
CATALANO et alii (1993). High-angle normal faults truncate
and offset at least two older generations of tectonic contacts,
313
that dip at moderate to low angles producing mainly
extensional displacements. At odds with older thrusts and with
more recent high-angle normal faults, the kinematics of these
low-angle tectonic contacts is not always well-constrained, and
thus their tectonic significance remains problematic.
Observations carried out in the northern edge of the Agri valley
strongly support the hypothesis that these contacts are, in fact,
low-angle normal faults, although a thrust origin for analogue
structures found elsewhere in the investigated area cannot be
ruled out.
CONCLUDING STATEMENT
The area that extends between the Melandro and Agri
valleys has recorded a complex history of superposed
deformations, that correlates well with the evolution of the
southern Apennines of western Lucania. Most structures
described in this investigation can easily be related to wellconstrained
episodes that have long been reported in a wide
regional literature, whereas others don’t appear to fit current
tectonic models. The origin and development of the latter
structures thus require an explanation in terms of their plausible
geodynamic significance.
REFERENCES
CATALANO S., MONACO C., TORTORICI L. & TANSI, C. (1993) -
Pleistocene strike-slip tectonics in the Lucanian Apennine
(Southern Italy). Tectonics, 12, 656-665.
MAZZOLI, S., BARKHAM, S., CELLO, G., GAMBINI, R.,
MATTIONI, L., SHINER, P. AND TONDI, E. (2001) -
Reconstruction of continental margin architecture
deformed by the contraction of the Lagonegro Basin,
southern Apennines, Italy. Jour. of the Geol. Soc. of
London, 158, 309-319.
PATACCA E. & SCANDONE P. (2007) – Geology of the Southern
Apennines. Boll. Soc. Geol. It., Spec. Issue n. 7, 75-119.
SESSIONE 10

SESSIONE 10
Key words: Agri Valley, geological map, Lucania, Southern
Apennine fold-and-thrust belt, structural analysis.
INTRODUCTION
This contribution aims at anticipating the results of a recent
structural study that has been carried out in the central domain
of the Lucanian Apennines in southern Italy. Compilation of an
original 1:25,000 scale geological map, integrated with
stratigraphic data and structural/kinematic evidence along the
NE edge of the Agri Valley, provides critical elements that
make it possible to discriminate the effects of recent,
seismically active deformations, related to the dissection of the
southern Apennine fold-and-thrust belt, from those related to
pre-orogenic deformations of Mesozoic age, inherited from
rifting and drifting of Adria.
This study aims at investigating the controlling factors of
repeated inversion and fault-reactivation phenomena, both
positive and negative, within orogenic domains. The study has
been carried out in the seismically and tectonically active Agri
Valley basin, in the axial zone of the southern Apennines of
Italy. Fieldwork was based on the compilation of an original
1:25,000 scale geological map of about 120 Kmq, on the
construction of cross sections, and on the kinematic analysis of
the major tectonic structures outcropping along the NE edge of
the Agri Valley.
The deformation history was reconstructed through the
recognition of macroscopic and mesoscopic structures, and
illustration of their mutual cross-cutting relationships. Regional
and detailed geological and structural mapping was coupled
with landscape and geomorphic analysis.
The tectonic evolution of the investigated domain was
characterized by the development of folds and related thrusts of
Miocene-Pliocene age, that were formed during the Alpine
orogenesis. These structures affected a highly heterogeneous
sedimentary cover, made of Triassic-Tertiary sedimentary
_________________________
Geology of the north-eastern margin of the High Agri Valley
(western Basilicata, southern Italy)
FRANCESCO BUCCI (*), ROCCO NOVELLINO (*), PAOLA GUGLIELMI (**),
ENRICO TAVARNELLI (*) & GIACOMO PROSSER (**)
(*) Dipartimento di Scienze della Terra, Università di Siena,
tavarnelli@unisi.it
(**) Dipartimento di Scienze Geologiche, Università della Basilicata,
Potenza
314
successions, that were deposited within pelagic basins and onto
adjacent carbonate platforms. One of the main results of the
present research is that thrust propagation across this
mechanically heterogeneous sedimentary sequence was
strongly influenced by the architecture of the precursor basinplatform
transition zone.
The present morphologic-structural frame of the high Agri
Valley results from the superposition of late- and/or postorogenic
extensional tectonics onto a pre-existing contractional,
thrust-dominated architechture. Low-angle extensional faults,
active during the Pliocene-Pleistocene time interval, were
responsible for early tectonic exhumation and unroofing
processes, mostly localised at the front of the Campania-
Lucania Platform. Extension within the structurally uppermost
units is documented by the occurrence of highly discontinuous
slivers of platform rocks pertaining to the Campania-Lucania
unit, bounded by shallow tectonic contacts and sandwiched
between pelagic deposits pertaining to the Ligurian and
Lagonegro domains, respectively. Kinematic complexities and
remarkable differences in fault rocks suggest that original thrust
contacts were truncated and/or partly reactivated as low-angle
detachments. Low-angle normal faults were, in turn, truncated
by more recent, high-angle normal fault sets that became the
dominant structural features since Pleistocene time onwards,
leading to the development of the Agri Valley basin. The
geometrical and kinematic relationships amongst faults of
different generations suggest a positive feedback between uplift
and erosion during post-orogenic extension; it seems likely that
progressive exhumation and unroofing were achieved by
activation of sequentially deeper detachments located below the
sole thrust of the Lagonegro Units.
One key feature outlined by this new survey is the
recognition and mapping of the Sorgente dell’Acero Member, a
stratigraphic unit that previous workers had only described as
part of the Calcari con Selce Formation. Furthermore the
present research provides important constraint on the study of
active tectonics in the High Agri Valley. In order to
characterize the recent faults and develop a correct census of
the sismogenic structures it is fundamental to reconstruct a
correct sequence of tectonic events that occurred in the area,
separating the effects of fossil from those of active structures.

Neogene-Quaternary Tectonic Stratigraphy of the eastern Southern
Alps, NE Italy: geodynamic implications for Adria
RICCARDO CAPUTO (*), MARIA ELIANA POLI (°) & ADRIANO ZANFERRARI (°)
Key words: mesostructural analysis; conglomerates; stress field
In order to reconstruct the Neogene-Quaternary Tectonic
Stratigraphy of the eastern Southern Alps (ESA), the late
Tortonian-lower Pleistocene foredeep clastic sequences, cropping
out in the Veneto and Friuli piedmont areas have been
extensively investigated focusing on the contractional features
observed in the frequent conglomerate layers (pitted pebbles).
The ESA is the result of a typical polyphase tectonic activity
initiated in Late Oligocene, characterised by the occurrence of
several non-coaxial stress regimes. Based on careful analyses of
the pebbles' surfaces (shape and orientation of the indented
features) and following a systematic and statistical approach, the
mean orientation of the maximum compressive stress axis (s 1)
has been obtained for more than 30 sites of measurements along
the ca. 120 km-long investigated piedmont area. The affected
lithostratigraphic units and the orientation (pre- versus posttilting)
of the stereonets density peaks make it possible to
recognize four distinct deformational events and characterize
them in terms of mean s 1 direction and timing (Fig. 1): late
Tortonian (s 1=313°/00°), late Messinian-Early Pliocene
(338°/04°), Late Pliocene (314°/03°), and Early-Middle
Pleistocene (160°/03°). It is noteworthy that these events do not
represent 'simple' local variations of the stress field because for
all datasets the corresponding sites of measurements are spread
along the entire investigated area and in many cases, the same
localities and sedimentary units are affected by more than one
dataset (viz. stress field). In particular, the 4 events could be
recognized and distinguished based on i) a different mean
direction of compression and ii) their timing of activity. More
exhaustive information about site location, deformed sedimentary
units, number of measurements per site and s 1 orientation can be
found in CAPUTO et al., 2010).
If we also consider the well-documented "Serravallian-
Tortonian" tectonic phase and the fact that it was also
characterized by a NNW-SSE trending compression (e.g.
CASTELLARIN et al., 1992; CAPUTO, 1996), during the last ca. 10
Ma we observe repeated variations of the s 1 axis from a mean
NNW-SSE to a mean NW-SE direction and viceversa (Twist
_________________________
(*) Dipartimento di Scienze della Terra, Università di Ferrara
rcaputo@unife.it
(°) Dipartimento di Georisorse e Territorio, Università di Udine
eliana.poli@uniud.it, adriano.zanferrari@uniud.it
315
Tectonics).
By integrating the results of the mesoscopic structural
analyses with geological and tectonic macroscopic observations,
and taking into account the reciprocal geometrical relationships,
Fig. 1 – Synthetic diagram showing the Tortonian p.p.-Pleistocene
sedimentary stratigraphy (units), the period of activity for the major tectonic
structures (thrusts; CASTELLARIN et al., 1992; ZANFERRARI et al., 2008), the
direction of maximum compression estimated from the meso-structural
analyses (s 1), the tectonic stratigraphy of the eastern Southern Alps with the
principal deformational events (darker sectors) and the corresponding table
including all datasets (S. Alps event), the direction of relative motion of
Africa with respect to Europe (AFR/EUR) and the major periods of couplingdecoupling
along the basal detachment of the Northern Apennines
(Apennines events). Stratigraphic units are from ZANFERRARI et al. (2008). In
column AFR/EUR, numbers refer to normal magnetic anomalies, while
arrows thickness is proportional to the amount of relative convergence
(MAZZOLI &HELMAN, 1994). In the last column, darker sectors represent
periods of frontal thrust propagation (i.e. decoupling) as inferred from largescale
unconformities in the Apennines foredeep (GHIELMI et al., 2009)
alternating to periods of possible coupling and transmission of compressional
stresses to the Southern Alps. The size of the arrows is tentatively
proportional to the stress contribution of the Apennines within the
SESSIONE 10

SESSIONE 10
the timing of activity for the major deformation structures (Fig. 1)
represented by, and associated with, the Valsugana and Belluno
thrusts, the Bassano-Valdobbiadene and Cansiglio-Maniago
thrusts as well as the Frontal Thrust System seems confirmed.
Accordingly, the Neogene to Present evolution of the ESA shows
a typical spasmodic migration of thrusting and deformation
towards the external sectors of the fold-and-thrust belt, where the
major structures have typical periods of activity of few million
years.
In order to fit our results within the evolution of the ESA and
the Late Tertiary geodynamic framework of the Central
Mediterranean, we observe that both assumed timing and
shortening orientation of the Chattian-Burdigalian phase
(CASTELLARIN et al., 1992; CAPUTO, 1996) are in agreement with
the relative motion of Africa with respect to Europe, the latter as
inferred from the analysis of magnetic anomalies for this period
(Fig. 2a). A similar statement is also appropriate for the second
major tectonic phase (Serravallian-Tortonian) affecting the ESA
(Fig. 2b). Indeed, notwithstanding the abrupt change in the
relative motion between Africa and Europe about 15 Ma ago, the
new NNW-SSE orientation of crustal shortening, largely
documented in the broader Southern Alps, nicely parallels the
direction of convergence between the two plates during Langhian
and early Tortonian. Considering that the Adria lithospheric
block likely behaved consistently with the major Africa plate, it is
likely that relative plate motion and stress field at the Africa-
Europe plate boundary along the Southern Alps are directly
linked by a cause-effect relationship. As a consequence, along the
boundary with Europe (i.e. northern Adria), the pervading stress
field was fully controlled by the relative plate motion of Africa
with respect to Europe.
However, notwithstanding a stable direction of plate
convergence since late Tortonian-Messinian (Fig. 2c) and the
assumed parallelism between the relative plate motion and the
mean stress trajectories at the plate boundary, from late
Messinian, the progressively approaching Northern Apennines
started to play a crucial role within the investigated area.
Alternating short-lived phases (1-2 Ma) of coupling and
decoupling along the basal detachment of the Apennines
accretionary wedge (Fig. 1) caused temporary perturbations of
the 'local' stress field and complex accommodation structures in
this region of ongoing crustal collision.
REFERENCES
CAPUTO R. (1996) - Mem. Sc. Geol., 48, 93-106.
CAPUTO R., POLI M.E. & ZANFERRARI A. (2010) - Tectonics, doi:
10.1029/2009TC002625.
316
Fig. 2 – Sketch maps of the Central Mediterranean suggesting how and why
the maximum horizontal stress trajectories varied in time within the eastern
Southern Alps. The three frames roughly correspond to the Chattian-Early
Miocene (a), Langhian-Serravallian (b) and late Tortonian-Messinian (c)
geodynamic reconstructions (see CAPUTO et al., 2010 for a complete
reference list). The major 'tectonic genetic components' governing the stress
field within the study area (small box) are associated with the relative plate
motion of Africa with respect to Europe (large arrows) and after Tortonian
also with the propagating accretionary wedge of the Apennines (smaller
arrows). The thin dashed lines depict the inferred direction of the s 1 axis
within the growing orogenic prisms. In the youngest frame, the crossing
stress trajectories schematically indicate the two principal stress fields, which
possibly alternate in time due to the prevailing Apennines versus Africa
remote forces.
CASTELLARIN A., CANTELLI L., FESCE A.M., MERCIER J.L.,
PICOTTI V., PINI G.A., PROSSER G. & SELLI L. (1992) -
Annales Tectonicae, 6(1), 62-94.
GHIELMI M., MINERVINI M., NINI C., ROGLEDI S., ROSSI M. &
VIGNOLO A. (2009) - Rend. online Soc. Geol. It., 9, 32-35.
MAZZOLI S. & HELMAN M. (1994) - Geol. Rund., 83, 464-468.
ZANFERRARI A., AVIGLIANO R, GRANDESSO P., MONEGATO G.,
PAIERO G., POLI M.E. & STEFANI C. (2008) - Note illustrative
della Carta geologica d’Italia alla scala 1:50,000 – Foglio
065 “Maniago”; 224 pp. Graphic Linea, Tavagnacco (UD).

The Apenninic-Maghrebian orogen in Southern Apennines and
Sicily: a multidisciplinary approach
Key words: Apenninic-Maghrebian orogen, paleogeography,
Sicily, Southern Apennines.
INTRODUCTION
Decades of field works, integrated with stratigraphical
observations, facies analysis, geometric and kinematic studies,
seismic lines interpretation, sometimes confirmed by specific
researches (thermo-chronology, organic petrography and so on)
allow to define a well constrained model of the Apenninic-
Maghrebian Orogen. In particular after the CROP Project it is
very clear the relationship between the distribution of the
different crustal characters and the geodynamic evolution
detected by means of the geological analysis. The oceanic
crusts were floored by deep sea sequences and suffered more or
less complete subduction; while the continental or thinning
crusts show shallow water deposits (mainly carbonate
platforms) and a tendency to a collisional stage.
In the Central Mediterranean Area clearly appears the
distribution of the structural Domains. The foreland domains
are represented by two continental blocks, the Apulian Block to
the north and the Pelagian Block to the south, respectively
belonging to the Adria and to the Africa plates. They are
separated since Permo-Triassic times by the oceanic crust of
the Ionian Sea. The Apenninic-Maghrebian Orogen is located
between two oceanic crusts: the old Ionian crust, at present time
subducting beneath the Calabrian Arc, and the new crust of the
opening Tyrrhenian Sea (LENTINI et alii, 2006 and references
therein).
The orogenic belt is represented by a multilayer
allochthonous edifice, composed of the Calabride Chain (CC)
tectonically overlying the Apenninic-Maghrebian Chain
_________________________
(*) Dipartimento di Scienze Geologiche, Università di Catania,
carbone@unict.it
SERAFINA CARBONE (*), FABIO LENTINI (*) & GIOVANNI BARRECA (*)
317
(AMC), which in turn overthrust onto the Upper Miocene and
Pliocene top-levels of a deep seated thrust system, originating
by the deformation, since Tortonian times, of the innermost
carbonates of the Pelagian/Apulian blocks (External Thrust
System: ETS), that means in contemporaneous with the
Tyrrhenian basin opening (LENTINI et alii, 2006).
The ETS, named Apulian Thrust System in the Lucania
Region, and Pelagian-Sicilian Thrust Belt in Sicily, crops only
at Mt. Alpi (Southern Apennines) and in western Sicily, but it
has been detected by the seismic lines and represents an
important target for petroleum researches. To the north it is
very probable the continuity with the Central Apennines
carbonate platforms. A way to recognize the belonging to
outermost units has been the age of the first terrigenous covers:
since middle-late Miocene in the ETS. That’s why we consider
equivalent the carbonate units exposed in Lazio-Abruzzo
region: the terrigenous covers are Late Miocene in age. As well
as at Mt. Alpi and in western Sicily the Meso-Cenozoic
sequences display a terrigenous cover younger than Middle-
Late Miocene.
The AMC tectonic units derive from the orogenic transport
during Oligo-Miocene times of sedimentary sequences
deposited in palaeogeographical domains located between the
Europe and the Afro-Adriatic plates. These units are composed
of Meso-Cenozoic shallow-water carbonate successions
detached from a continental type crust sector, the
Panormide/Apenninic Block, recognizable by means of seismic
lines shot in the Tyrrhenian offshore of Southern Apennines
and Northern Sicily. The Meso-Cenozoic basinal units, that
compose the AMC, can be distinguished into two main groups
of sequences, originally located on oceanic crusts separated by
the Panormide/Apenninic Block: the external ones (Ionides)
related to an original basin belonging to branches of the Ionian
Palaeobasin involved in the orogenesis, and the internal ones
ascribed to the Alpine Tethys (Sicilide Units).
The Calabride Chain originated by the delamination of the
European margin. This roof thrust system includes nappes of
Hercynian basement with remains of the original Meso-
Cenozoic covers deformed during the Paleogene and sutured by
the Late Oligocene-Early Burdigalian Capo d’Orlando Flysch.
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SESSIONE 10
The terrigenous deposits of the basinal sequences belonging
to the Ionides are represented by Tertiary foreland/foredeep
deposits (i.e. Numidian Flysch), whose relationships with the
substratum are occasionally preserved, although large
detachments occurred with further forward transport, which
generated repeated slices with an apparent increase to the
original thickness. Petrological analysis represents a constrain
about the external location of the Numidian Flysch.
A well constrained description of the tectono-stratigraphy of
the units, which compose the allochthonous edifice of the
AMC, and some geological cross-sections allowed to restore
times and modalities of thrust propagation, emphasizing indeed
the general decoupling of the Tertiary flysch-type covers,
which represents a fundamental character for interpreting the
surface geology.
The geological, geophysical data and the volcanological
characters permit to restore the palaeogeography and the
geodynamic evolution. Between Europe and the Afro-Adriatic
margins the Alpine Tethys, characterized by an oceanic or
thinned crust, was located. The Palaeoionian Sea was a basin
intervening since Permo-Triassic times between the
Apulian/Pelagian Blocks, and branches of the Palaeoionian
basin were floored by the Ionides.
It is possible to recognize three orogenic stages (LENTINI et
alii, 2006): the Eo-Alpine, originated during Cretaceous-
Eocene times, evident in the western Calabria, in the
Tyrrhenian basin and the Alpine Corsica; the Balearic stage
(Late Oligocene-Early Miocene), in which the Corsica-Sardinia
block rotated and collided with the Adria-Africa margins with
thrusting of the Alpine Tethydes over Panormide/Apenninic
platforms (which at that time represented the foreland domain);
and the Tyrrhenian stage (Middle Miocene to Present), when
the onset of the Tyrrhenian back-arc basin occurred and after
the closure of the interposed Palaeoionian branches the Ionides
were tectonically transported onto the foreland blocks.
The seismic lines clearly indicate that both the foreland
blocks extend below the orogenic belt, reaching the Tyrrhenian
shorelines, with a gradual thinning and a transition to a Palaeo-
Ionian slab, probably not active at present time, from which the
Ionides detached and overrode the ETS.
At the present time the seismogeological data indicate that
the Panormide/Apenninic continental crusts are colliding with
the Pelagian/Apulian Blocks. The geological evidence of this
collisional stage is manifested in the NW-SE oriented South
Tyrrhenian System (STS), characterized by dextral faults,
affecting both the offshore and the onshore of Sicily. A
specular structural setting has been recognized along the
perityrrhenian sea in front of the southern Apennines (Cilento).
There a sinistral fault system is developed both offshore and
onshore.
Thus at present time two collisional settings have been
recognized in western Sicily and in southern Apennines. The
trascurrent fault systems drive the Calabria-Peloritani Arc
toward SE.
318
The distribution of the hypocenters of the earthquakes and
the clear images of the CROP project showing the Ionian slab
indicate that Southern Calabria and north-east Sicily represent
the only segment of the arc still subducting.
Geological mapping, integrated with stratigraphical and
structural analysis, widely carried out in Sicily, show that this
area is dominated by a strike-slip tectonics, connected with the
geodynamic evolution of the Tyrrhenian stage. Beside to the
NW-SE oriented right lateral faults, antithetical NE-SW
system, associated with N-S normal faults and south-verging
thrusts, occur. All these structures are compatible with an
unique contemporaneous kinematic picture.
It is evident that the South Tyrrhenian System, well
developed in the southern sector of the Tyrrhenian Sea,
dominates also the onshore areas of the Island. Some examples
can be observed in western Sicily. There, the east-west oriented
carbonate ridges, belonging to the Pelagian-Sicilian thrust
system (M. Kumeta, Rocca Busambra), are bounded by reverse
faults and controlled by NW-SE oriented trascurrent faults with
dextral component. The sigmoidal characters of the ridges, as
well as those of the fold axis, indicate a dextral movement.
The Patti area (NE Sicily), affected by frequent seismic
events, is characterized by a set of dextral faults belonging to
the STS, NE-SW sinistral faults and N-S oriented normal
faults. These latter belong to the Vulcano line, a NNW-SSE
oriented fault, that represents a boundary between the
collisional setting to the west and the still subducting Ionian
slab to the east. It crosses the Eolian Islands and separates the
areas with volcanic activity to the east (Vulcano, Panarea,
Stromboli) from the western islands (Alicudi, Filicudi), where
active volcanic phenomena seem to have stopped at present
time.
On the other hand the M. Etna volcano is located close to
the boundary between the collisional area and the still
subducting Ionian slab, and it is bounded by two major strikeslip
shear zones. Between them some sigmoidal N-S oriented
normal faults are recognizable. This picture can provide a
convincing hypothesis about the origin of the volcano.
REFERENCES
LENTINI F., CARBONE S. & GUARNIERI P. (2006) – Collisional
and post-collisional tectonics of the Apenninic-Maghrebian
Orogen (Southern Italy). In: Y. DILEK and S. PAVLIDES
(Eds.), “Post-collisional Tectonics and Magmatism in the
Eastern Mediterranean Region”. Geol. Soc. Amer., Special
Paper, 409, 57-81.

The Poggio La Torre Conglomerate (Enza Valley): an enigmatic
‘alpine’ deposit of the Northern Apennine Epiligurian Basin
Key words: Alpine-derived conglomerate, Val d’Enza syncline.
The Poggio La Torre Conglomerate is an “alpine” clastic
deposit of the Oligo-Miocene Epiligurian Basin outcropping in
eastern Northern Apennine (Enza Valley ).
The alpine composition (metaophiolites, metaradiolarites,
calceschistes) of very coarse orthoconglomerate (with boulders of
50 cm in diameter) in the appennic succession (Epiligurian
Succession) draping Ligurian Units, represents a very stimulating
geological puzzle.
An important question of this enigmatic case, consists in the
position of Poggio La Torre Conglomerate in relation to the core
of the overturned syncline of the Enza Valley in Emilian sector of
the Northern Apennine.
The correct solution of this structural problem is substantial to
decide the stratigraphical position of the conglomerate in relation
to the Burdigalian marls (Antognola Formation) and platform’s
Langhian sands (Pantano Formation of Bismantova Group) of the
Epiligurian Basin.
This question is discussed to reassemble the puzzle caused by
the ‘out of place’ geological clastic body in relation to a
theoretical model of transpressional structuration of the Northern
Apennine.
_________________________
(*) Istituto di Geoscienze e Georisorse – C.N.R., Pisa, cerrina@igg.cnr.it
ANDREA CERRINA FERONI (*)
319
SESSIONE 10

SESSIONE 10
___________________
Transpressive evolution of the Ligurian Alps - Northern Apennines
system – 2: a perspective from the Northern Apennines
ANDREA CERRINA FERONI (*), ALESSANDRO ELLERO (*), RITA CATANZARITI (*), ANNA D’ATRI (°°),
ANDREA IRACE (°), PIETRO MOSCA (°), FABRIZIO PIANA (°) & DARIO VARRONE (°)
Key words: Northern Apennines, transpression, Western Alps.
INTRODUCTION
The convergent evolution of the European and Adriatic
continental margins of the Liguria-Piemonte ocean, has been
thought by some Authors (SCHOLLE, 1970; SCANDONE, 1979;
PRINCIPI & TREVES, 1984) as partitioned into two distinct
branches with peculiar geometric and kinematic characters . The
northern branch was characterized by an east dipping (“Alpine”)
subduction, while the southern one by a west dipping
(“Apenninic”) subduction.
From the kinematic point of view, this interpretation, that
explains a large amount of geological observation, implies the
presence of a regional transfer zone (active for several tens
millions years) between these opposite-dipping branches of the
Liguria-Piemonte realm. This transfer zone, was assumed to run
at the northern-eastern boundary of the Western Ligurian Alps,
and in the region between these units and the Northern
Apennines.
In this region, the occurrence of strike-slip or transpressional
tectonics since the Cretaceous up to Late Miocene times is largely
documented by recent data and re-interpretation of large data sets
on the Western and Eastern Ligurian Alps sectors and in the
Tertiary Piemonte basin, as well as on the external boundary of
the Ligurian units of Northern Apennines and their adjacent
Miocene foredeep basins of the Emilia Apennines.
Oblique convergent evolution of both European and Adriatic
margins of the southern branch of the Liguria-Piemonte ocean is
suggested, to justify a consequent development of several enechelon
kinematic transfer zones, developed distinctly through
Cretaceous-Early Miocene times, that could be envisaged, as a
whole, as the regional kinematic transfer required by the model.
(*) CNR - Istituto di Geoscienze e Georisorse, Pisa
(°) CNR - Istituto di Geoscienze e Georisorse, Torino, f.piana@csg.to.cnr.it
(°°) Dipartimento di Scienze della Terra, Università di Torino
320
As a major consequence, the presence of a single, precisely
located, transfer zone between Ligurian Alps and Northern
Apennines is not necessary if a transpressive-transtensive
evolutionary model for the whole Alps-Apennines junction zone
is suggested.
This topic will be discussed in two separate contributions,
examining the problem respectively from the "Alpine" and
"Apennines" point of view.
The first contribution regards the Ligurian Alps perspective
on the problem, while the second contribution focuses on the
Apennines perspective.
THE NORTHERN APENNINES PERSPECTIVE
This contribution focuses attention on the geological
structures and tectonic phases that characterize the apenninic
domain in the early-middle Miocene, to get the comparison with
coeval structures in the Ligurian Alps.
A duplication of the Northern Apennine chain along an
orogen-parallel dextral transcurrent system, shifting the eastern
tectonic domain to the south for several hundred kilometres
(CERRINA FERONI, 1988; CERRINA FERONI et alii, 2002, 2004) at
the “Front of the Tuscan Nappe”, is suggested. In this view it is
proposed that the major appenninic tectonic elements, classically
regarded as bounded by thrust or by high angle normal faults, in
many cases correspond to domains limited by strike-slip faults.
Oblique kinematics with predominantly dextral sense of shear and
displacement of one-two hundred kilometres, allow to restore the
deposits of Tertiary Piedmont Basin with the Epiligurian
Succession of the Apennines and to explain the presence of
Miocene and Plio-Pleistocene longitudinal high angle fault
systems, as well as the double vergence of the chain.
REFERENCES
CERRINA FERONI A. (1988) – La duplicazione della catena a
falde, per trascorrenza longitudinale, nell'Appennino
settentrionale: una soluzione alternativa. Rend. Soc. Geol.
It., 11, 325-328.

CERRINA FERONI A., OTTRIA G., MARTINELLI P., MARTELLI L. &
CATANZARITI R. (2002) – Structural-Geological Map of the
Emilia-Romagna Apennines (1:250.000). SELCA, Firenze.
CERRINA FERONI A., OTTRIA G. & ELLERO A. (2004) – The
Northern Apennine, Italy: geological structure and
transpressive evolution. In: U. Crescenti, S. D’Offizi, S.
Merlini & L. Sacchi (Eds.) - Geology of Italy - Special
Volume of the Italian Geological Society for the IGC 32
Florence – 2004, 15-32.
PRINCIPI G. & TREVES B. (1984) – Il sistema Corso-Appenninico
come prisma di accrezione. Riflessioni sul problema generale
del limite Alpi Appennini. Mem. Soc. Geol. It., 28, 548-576.
SCANDONE P. (1979) – Origin of the Tyrrhenian Sea and
Calabrian Arc. Boll. Soc. Geol. It., 98, 27-34.
SCHOLLE P.A. (1970) – The Sestri-Voltaggio line: a transform
fault induced tectonic boundary between the Alps and the
Apennines. Am. J. Sci., 269, 343-359.
321
SESSIONE 10

SESSIONE 10
Key words: Pseudoverrucano, southern Tuscany, stratigraphy,
structural setting.
INTRODUCTION
The Pseudoverrucano-bearing successions of the coastalsouthern
Tuscany (inner Northern Apennines) represent a still
uncertain, controversial and debated subject, relatively to their
significance and stratigraphic – palaeogeographic / structural
position. This is due mainly to the strongly scattered and rare
outcrops, where stratigraphic and tectonic relationships with the
other units/formations are often characterized by severe tectonic
complexity. Nevertheless such successions play a key role for the
reconstruction of the Western Mediterranean palaeogeographic
puzzle, starting from the Mesozoic. “Pseudoverrucano” is an
informal term to indicate a close similarity with the Verrucano
lithofacies, this last belonging to the Tuscan metamorphic
formations. The Pseudoverrucano lithofacies occurs at the bottom
of the sedimentary successions/tectonic units. These last ones are
part of the inner Northern Apennines orogenic nappe stack, with
a structural position between the Tuscan Nappe below and the
Subligurian Unit (Argille e calcari Unit) above. The
Pseudoverrucano successions crop out only close to the
Tyrrhenian coast near Grosseto in few outcrops, which are the
Punta delle Rocchette outcrop near Castiglione della Pescaia, the
Montebrandoli area east to Grosseto, the Uccellina Mts. south to
Grosseto and the Collecchio area east to the Uccellina Mts..
In this research, mainly based on new field mapping and
stratigraphic/structural analyses, a new hypothesis about the
“role” and the significance of the Pseudoverrucano-bearing
successions for the Tuscan stratigraphic/structural framework is
proposed.
_________________________
Stratigraphic and structural setting of the “Pseudoverrucano”
lithofacies in southern Tuscany
PAOLO CONTI (*) (°), GIANLUCA CORNAMUSINI (*) (°), FABRIZIO UCCELLETTI (°) & ANTONIO BALDETTI (°)
(*) Dipartimento di Scienze della Terra, Università di Siena,
cornamusini@unisi.it
(°) Centro di Geotecnologie, Università di Siena
322
DATA AND DISCUSSION
The Pseudoverrucano corresponds to a lithofacies mainly
made of beds of coarse quartz-breccia with a diffuse dark red
colour, very similar to the classical Verrucano lithofacies.
However, the Pseudoverrucano and the Verrucano lithofacies
occupy different stratigraphic positions, as consequence of
deposition in different palaeogeographic settings. The
Pseudoverrucano-bearing successions, similarly at what
previously introduced and discussed by other Authors, occur in
two tectonic units, respectively the lowermost Uccellina Mts.
Unit and the Vacchereccia-Montebrandoli-Collelungo Unit,
referring to the Pisa-Siena school’s terminology. We identify a
structural setting for the whole areas characterized by the stacking
of the following tectonic units, from the lowest upward: the
Tuscan Nappe; the Talamone-Torre Cannelle Unit (with
Verrucano at the base and Calcare cavernoso, separated by a
detachment surface); the Uccellina Mts. Unit (with
Pseudoverrucano at the base, the Salto del Cervo Fm., the
Calcare massiccio, the Calcare rosso-ammonitico, the Calcare
selcifero, the Marne a Posidonomya, the Diaspri and the Scaglia
toscana, see Fig. 1); the Vacchereccia-Montebrandoli-Collelungo
Unit (from the base upward, the Pseudoverrucano, the Calcare di
Montebrandoli, the Punta delle Rocchette Fm. locally subdivided
in Calcare rosso-ammonitico at the base and Calcare selcifero,
the Marne a Posidonomya, the Diaspri, the Scaglia toscana and
the Macigno Fm. at the top, which could be hypothetically
indicated as Macigno costiero). At Punta delle Rocchette the
geological setting is characterized by the stack of two tectonic
subunit both belonging to the Vacchereccia-Montebrandoli-
Collelungo Unit, the lowest from the Pseudoverrucano up to the
Calcare selcifero, while the uppermost from the Pseudoverrucano
up to the Macigno Fm. The Montebrandoli area, inland east to the
Punta delle Rocchette, is characterized by a complex tectonic unit
stack, where the Pseudoverrucano succession, in particular the
Vacchereccia-Montebrandoli-Collelungo Unit, is involved in a
few thrust slices. The lowest one shows the Pseudoverrucano –
Scaglia toscana (mainly calcarenites, probably to be referred as
“Nummulitic”) succession, with the occurrence of polygenic
breccia levels; the intermediate tectonic slice shows the
succession Pseudoverrucano – Calcare di Montebrandoli, with a
clear conformable and gradual boundary, passing upward

Fig. 1 – Scheme of the stratigraphic-structural relationships of the Uccellina Mts. Unit and of the Vacchereccia-Montebrandoli-Collelungo Unit
for the Rocchette, Collelungo, Salto del Cervo and Collecchio areas: V1-V2 Pseudoverrucano, FSC Salto del Cervo Fm., CMB Calcare
Montebrandoli, MAS Calcare massiccio, MPR Marne Punta delle Rocchette, RSA Calcare rosso-ammonitico, LIM Calcare selcifero, POD
Marne a Posidonomya, DSD Diaspri, STO Scaglia toscana, MAC Macigno.
unconformably to the Scaglia toscana; the uppermost slice shows
the Pseudoverrucano only. We infer that the Vacchereccia-
Montebrandoli-Collelungo Unit overlies the Uccellina Mts.. Unit
and this the Tuscan Nappe. The northern Uccellina Mts. along the
coast, south to Punta delle Rocchette, are the widest outcrops of
the Pseudoverrucano-bearing successions. There, particularly at
Collelungo and Salto del Cervo localities, we observe a complex
tectonic unit stack, from the bottom upward: - the Talamone-
Torre Cannelle Unit, the Uccellina Mts. Unit and the
Vacchereccia-Montebrandoli-Collelungo Unit. The Uccellina
Mts. Unit is formed of, from the bottom, the Pseudoverrucano,
the Salto del Cervo Fm., the Calcare massiccio, the Calcare
rosso-ammonitico and the Calcare selcifero. The Vacchereccia-
Montebrandoli-Collelungo Unit is formed by Pseudoverrucano at
the base, the Calcare di Montebrandoli, the Marne di Punta delle
Rocchette Fm., the Scaglia toscana (mainly quartz-rich
Nummulitic calcarenites) and the Macigno Fm, also if in a few
areas the Scaglia toscana directly overlies unconformably the
Pseudoverrucano lithofacies. The inland Collecchio area, east to
the northern Uccellina Mts., is characterized by a geological
setting similar to the area before mentioned. In the Collecchio
area we recognize a lowest Uccellina Mts. Unit, made of the
Calcare massiccio, the Calcare rosso-ammonitico, that locally
passes upward to the Diaspri, the Marne a Posidonomya and the
Scaglia toscana. More often, the Calcare massiccio-Calcare
rosso-ammonitico succession is directly overlain by a thick
tectonic breccia, developed along a cataclastic shear zone. This
shear zone, which marks the detachment boundary with the above
323
standing Vacchereccia-Montebrandoli-Collelungo Unit, is locally
dominated by the Calcare rosso-ammonitico, or the Marne a
Posidonomya, or the Diaspri clast-lithologies. The latter unit is
made of there by the Pseudoverrucano at the bottom, which is
unconformable overlain by the Diaspri?-Scaglia toscana-Macigno
Fm. succession; locally the Pseudoverrucano seems to pass
upward to the Calcare di Montebrandoli.
Finally, due to the stratigraphic-structural features and the
relationships among the units, we hypothesize a palaeogeographic
setting for the successions involving the Pseudoverrucano, as
those of the Uccellina Mts. Unit and of the Vacchereccia-
Montebrandoli-Collelungo Unit, placing them in the westernmost
part of the Adria continental paleomargin, as the Innermost
Tuscan Domain (“Ultra Tuscan subdomain”), adjacent to the
Subligurian Domain. In such framework the innermost unit would
be the Vacchereccia-Montebrandoli-Collelungo Unit, whereas the
Uccellina Mts. Unit would originate from an intermediate
position with it and the Tuscan Nappe. To this respect, the
Pseudoverrucano lithofacies could represent a partially
diachronous depositional unit. It could be hypothetically locate at
the western margin of a like-aborted Triassic-?early Jurassic
intraTuscan Domain rift, then, starting from the Jurassic, totally
made uniform with the development and subsidence of the whole
Tuscan Basin, whereas the Ligurian-Piedmont rift-to-drift
processes developed innermost, separating them from the
European continental margin (Sardinia-Corsica Massif).
SESSIONE 10

SESSIONE 10
Relationships among stratigraphy, fold-and-thrust structures and
transversal tectonics in the northern Chianti Mountains
(Northern Apennines)
Key words: Northern Chianti Mts. stratigraphy, transverse and
fold-thrust tectonics, Tuscan Nappe.
INTRODUCTION
The Chianti Mts. Range represents a crucial area in the
Northern Apennines. It is in fact the central part of a broader
NNW-SSE 250 km long structural ridge (“Mt. Orsaro-Cetona”
Ridge Auctt.), which divides two different structural domains: a
western one (inner), affected by crustal delamination and thinning
and an eastern one (outer), affected by crustal thickening. The
Chianti Mts. Range is bounded to the west by the allochthonous
Ligurian thrust-sheets (made of the Ophiolitic and Morello units)
and by the Siena-Val d’Elsa Neogene basins and to the east by
the Upper Valdarno Pliocene-Quaternary Basin. The Chianti Mts.
Range is a classical fold-thrust belt system, developed in an
accretionary wedge. The deformative structures affecting the
apenninic orogenic stack are particularly evident in the Tuscan
Nappe tectonic unit, which extensively crops out in the area. In
more details, the Chianti Mts. Range corresponds to a structural
high, where the Tuscan Nappe is structured into a complex megaanticline
dissected by several fault generations. The Chianti Mts.
also represents an important study area for stratigraphic
investigations, as the “Scaglia Toscana” and “Macigno” Fm.,
which have been here formalized with their own stratotype logs.
In this work we show the main northern Chianti Mts. Range
structural features. This has been pursued thanks to detailed field
mapping and both stratigraphical and structural logging. In
particular, the relationships between stratigraphy, thrusting and
transverse tectonic have been emphasized. Such relationships
mainly forced the syn-collisional development the Chianti Mts.
Range. Mutual controlling factors, which determined several
stratigraphical and tectonic settings, have been recognized. They
_________________________
GIANLUCA CORNAMUSINI (°) (*), ALESSANDRO IELPI (°), FILIPPO BONCIANI (*),
IVAN CALLEGARI (*) & PAOLO CONTI (°) (*)
(°) Dipartimento di Scienze della Terra, Università di Siena,
cornamusini@unisi.it
(*) Centro di Geotecnologie, Università di Siena
324
proceeds longitudinally to the main thrust-belt structure; in fact,
several transverse lineament, bounding different geological
domains (differences in stratigraphy, grade and style of tectonic
deformation), have been highlighted. The whole ridge has been
also dissected by a set of plio-quaternary normal faults. The most
recent papers describing the geological structure of this range are
those of ELTER &SANDRELLI (1995), FAZZUOLI et alii (1996),
BONINI (1999).
DATA AND DISCUSSION
The Tuscan Nappe crops out with its lower lithostratigraphic
terms in two small erosional windows (Cintoia and Lucolena),
where a Jurassic to lower Cretaceous succession crops out
(Calcare Selcifero, Marne a Posidonomya, Diaspri and
Maiolica). The “Scaglia Toscana” crops out extensively along the
axial zone of the ridge. Finally, wide outcrops of “Macigno” Fm.
characterize both the eastern and western flanks of the main
anticline. The “Scaglia Toscana” has been subdivided in some
hierarchical minor lithostratigraphic units, on the base of different
lithological associations and stratigraphical occurrence. Such
units show on the outcrop different thickness and frequent lateral
heteropy. Significant stratigraphical variations have been in fact
observed between the northern and the southern sector of the
study area (Fig. 1): in the northern sector (from Cintoia to
Lucolena) the “Scaglia Toscana” is made by (from the bottom)
the “Argilliti di Brolio”, the “Marne del Sugame” and the
“Argilliti di Cintoia”. The southern sector instead (from
Badiaccia a Montemuro to Gaiole in Chianti) shows a succession
made by the “Argilliti di Brolio”, the “Argilliti di Cintoia”, the
“Calcareniti di Montegrossi” and the “Argilliti e calcareniti di
Dudda” Interbeddings and heteropies are more frequent in these
latter three units. While all the stratigraphical peculiarities have
been determined by the Jurassic to Oligocene basinal architecture
and physiography, (mainly controlled by the syndepositional
tectonics), the deformative evolution of the Chianti Mts. has been
likely driven by sharp lithologic contrasts and by
inheritance/reactivation phenomena of the former syndepositional
faults. As a result, distinct domains along the main
structure came out, characterized by different stratigraphy,

Fig. 1 – Significant cross-sections transversal to the Chianti Anticline. E-E’ northern sector near Cintoia; D-D’ northern sector near Lucolena; B-B’ southern
sector near Badiaccia Montemuro-Piazza di Siena. At the top, the Macigno Fm., below the Scaglia toscana succession and to follow the other Tuscan Nappe
fms.
shortening rates and tectonic styles. Such domains are bounded
by WSW-ENE transversal lineaments, which are parallel to the
main transversal lines of the Northern Apennines. In particular,
the southern domain, characterized by stronger lithological
contrasts, shows a higher complexity; minor imbricate thrustslices
as well as thrust-duplex structures occur, thrusting the
“Scaglia Toscana” onto the “Macigno” Fm. Differently, the
northern domains, characterized by softer lithologic contrasts and
by a lower lateral heteropy, show a simplier structure, dominated
by a main asymmetric anticline, affected by minor east-vergent
overturned folds in the eastern side.
REFERENCES
BONINI M. (1999) – Basement-controlled Neogene post
collisional polyphase cover thrusting and basin development
along the Chianti Mountains ridge (Northern Apennines,
Italy). Geol. Mag., 136, 133-152.
ELTER F.M. & SANDRELLI F. (1995) – Inquadramento strutturale
dei Monti del Chianti. Boll. Soc. Geol. It., 114, 537-547.
FAZZUOLI M., PANDELI E. & SANDRELLI F. (1996) – Nuovi dati
litostratigrafici sulla Scaglia Toscana (Scisti Policromi) dei
325
Monti del Chianti (Appennino settentrionale). Atti Soc. Tosc.
Sc. Nat., Serie A, 103, 95-104.
SESSIONE 10

SESSIONE 10
__________________
Burial and exhumation processes along the Apennine chain
Key words: Burial, clay mineralogy, exhumation,
thermochronology, vitrinite reflectance.
INTRODUCTION
The Apennine orogen is often cited as a type example of a
retreating convergent subduction boundary, but a number of
fundamental questions regarding its orogenesis remains, and there
are alternative models to explain extension in the Apennines,
including slab detachment and spreading of an overthickened
critical wedge in response to underplating. The timing and nature
of late Cenozoic topographic development is also controversial.
In an effort to better distinguish between contrasting models a
valid contribution derives from reconstruction of paths and rates
of exhumation. The advent of fission-tracks studies since the
early sixties allowed to date the last portion of exhumation paths
thanks to low closure temperatures of zircon and apatite
(respectively about 240 and 110°C). Furthermore the
improvement of knowledge about He diffusion allowed the
development in the last 10 years of a new technique that provides
quantitative constraints to the very final path of exhumation down
to 40°C. As a matter of fact apatite fission track and apatite (U–
Th)/He are the most widespread thermochronometers for
investigating the tectonic and climate-driven interactions within
the top few kilometers of the crust. These techniques are also
widely used for investigating burial conditions in sedimentary
basins in different tectonic settings and in the external portions of
orogens (namely fold and thrust belts), where maximum burial
amounts (due to either sedimentary loading or overthusting)
never exceed a few kilometers. Low temperature
thermochronology is then generally coupled with paleothermal
indicators as a combined approach can provide information on
both time and extent of burial and cooling evolution. Among the
existing paleothermal indicators, the most widespread is vitrinite
reflectance that provides detailed resolution in diagenesis and
very low grade metamorphism as it increases irreversibly with
(*) Dipartimento di Scienze Geologiche - Univ. Roma TRE
(**) Dipartimento di Geoscienze – Università degli Studi di Padova,
massimiliano.zattin@unipd.it
SVEVA CORRADO (*), MASSIMILIANO ZATTIN (**) & LUCA ALDEGA (*)
326
temperature and depth. Paleo-thermal indicators from clay
mineralogical assemblages, measured by X-ray diffraction, such
as Kübler Index and illite content in mixed layer illite-smectite (I-
S) may be used for reconstructing maximum burials as well. The
main purpose of this contribution is to provide a discussion of the
existinting literature on thermal and thermochronological
indicators for the Apennines fold-and thrust belt with special
regard to sedimentary units. It may represent a robust starting
point for validating structural and geodynamic models that
include modelling of the vertical movements within the orogen.
NORTHERN APENNINES
Northern Apennines have been studied in details since the
‘80s and today they yield a very dense dataset obtained by
different low-temperature thermochonological techniques: zircon
fission-track (ZFT), apatite fission-track (AFT) and (U-Th)/He on
apatite (AHe). For a review, see CORRADO et alii (2010).
Futhermore, a huge amount of samples both from surface and
bore-holes have been analyzed by the vitrinite reflectance
technique. Within the pile of Ligurian and Tuscan nappes, the
coal rank increases generally from top to bottom, to reach the
low-grade metamorphism in the lowermost nappe. Data from
wells in the foredeep successions show values up to advanced
organic metamorphism whereas at surface both vitrinite
reflectance and thermochronology data show a general decrease
of the burial conditions from Tyrrhenian to Adriatic coast.
Except for some magmatic post-orogenic thermal events, the
main coalification cause can be generally ascribed to nappes
emplacement during the Apennine orogeny in the Miocene. This
feature is evident both in the central region of the chain than in
the external area. On the other hand, late orogenic extensional
tectonics is clearly younger than time of maximum burial
throughout the chain.
The exhumation history follows the same pattern observed for
the burial conditions. In fact, both AFT and AHe techniques
indicate a general eastward decrease of the exhumation ages.
More in detail, the youngest AHe ages (ca. 1 to 2 Ma) have been
detected close to the core of the range whereas youngest AFT at
about 4 Ma close to the reset front. The onset of exhumation of
the chain is recorded from the oldest ages, located west of the
topographic divide. Here AFT data range up to about 13 Ma.

CENTRAL APENNINES
Thermochronological dataset is here very limited as only a
few AFT ages have been obtained from the Gran Sasso and the
Trasimeno Lake area. However, the dataset related to thermal
indicators of maximum burial is more abundant. Mean vitrinite
reflectance data from the Meso-Cenozoic pelagic successions at
the top of the thrust stack of the Central Apennines indicate the
immature stage of hydrocarbon generation. For the Umbria-
Marche basin, the Montagna dei Fiori structure shows low
thermal maturity levels. On the other hand, along the Gran Sasso
range, fission tracks have been totally reset. RUSCIADELLI et alii
(2005) tried to do some thermal modelling on these ages by
integration with some vitrinite reflectance data. Their results
seems to indicate an exhumation phase in the last 5 m.y.,
confirming the geological evidence of the existence of a Middle
Pliocene unconformity. Thermal constraints for the Molise and
Sannio Basins were provided only by X-ray diffraction. Data for
the Upper Oligocene(?)-Lower Miocene varicoloured clays
indicate early diagenetic zone and low burial temperatures. Synorogenic
siliciclastics are mainly preserved at the footwall of
regional thrust sheets that are progressively younger from
hinterland to foreland with ages bracketing between the Upper
Tortonian and the Messinian. Upper Tortonian foredeep and
Lower Messinian? thrust-top basin deposits cropping out along
the Latina Valley at the footwall of the Volsci Range display low
levels of thermal maturity. Lower Messinian siliciclastics at the
footwall of the Sabina structures in pelagic facies, show
palinofacies with vitrinite reflectance of indigenous macerals
between Ro = 0.25 and 0.35%. Lower Messinian siliciclastics
cropping out to the West and to the East of the Montagna Grande
carbonate ridge show an extremely low thermal maturity. Slightly
higher values are detected to the south of the ridge at the footwall
of the Meta Mountains carbonate thrust sheet as result of tectonic
loading.
In the Laga Basin, Messinian siliciclastics show increasing
vitrinite reflectance as function of depth in the basin depocentre
and values of 0.45-0.5% in the immediate footwall of the Gran
Sasso Range and of the Sibillini thrust front. The AFT dataset
(RUSCIADELLI et alii, 2005), given the “young” depositional age,
indicate that burial temperatures never exceeded the 120°C.
SOUTHERN APENNINES
Thermal and thermochronological constraints indicate that the
Southern Apennines can be divided into two distinct
thermotectonic plates: an upper plate that records limited burial
and only minor heating, and a lower plate that has been
extensively tectonically buried and heated. The upper plate
consists of the rocks of the Apennine Platform domain with the
tectonically overlying “internal” units (Ligurian and Sicilide).
The former range in the early diagenetic zone and the immature
327
to early mature stage of hydrocarbon generation and by no
annealing of AFTs. Thermal modelling suggests the minor effect
of burial (never exceeding 2 km) for the rocks of the Apennine
Platform domain. To the South, rocks from the Apennine
Platform Domain (Pollino ridge) experienced higher levels of
thermal maturity with an age of exhumation of 6.0 ± 1.1 Ma. The
Ligurian unit shows and early to late diagenetic conditions and
mature stage of hydrocarbon generations with a cooling age of
11.4± 1.2 Ma.
The lower plate includes rocks of the Lagonegro Basin, the
Monte Croce, and the Apulian Platform domains. For the
Lagonegro Basin successions, organic and inorganic thermal
indicators show an increase of thermal maturity as a function of
depth. For the Miocene siliciclastic deposits transgressive on the
Lagonegro unit, data show an eastward general decrease in
thermal maturity between the mature and the immature stage of
hydrocarbon generation. The data from Monte Alpi, representing
the unique outcrop of Apulian Platform rocks, consistently fall
into the late diagenetic zone and late mature stage of hydrocarbon
generation (MAZZOLI et alii, 2006). As opposed to the rocks
belonging to the upper plate, all samples from the lower plate
were affected, during the Neogene, by maximum temperatures
higher than total annealing temperature. Thermal modelling
indicate slight differences in thermal maturity along the strike of
the chain related to different amounts of tectonic loads and in the
timing of exhumation. Generally, AFT data indicate a late
Miocene onset of exhumation of previously deeply buried rocks
in the southern Apennines.
REFERENCES
CORRADO S., ALDEGA L. & ZATTIN M. (2010) - Sedimentary vs.
tectonic burial and exhumation along the Apennines (Italy).
In: M. Beltrando, A. Peccerillo, M. Mattei, S. Conticelli and
C. Doglioni (Eds.) - The Geology of Italy, Journal of the
Virtual Explorer, Electronic Edition, 36, paper 15.
MAZZOLI S., ALDEGA L., CORRADO S., INVERNIZZI C. & ZATTIN
M. (2006) - Pliocene-Quaternary thrusting, syn-orogenic
extension and tectonic exhumation in the southern Apennines
(Italy): insights from the Monte Alpi area. In: Styles of
Continental Contraction, Geological Society of America,
Special paper, 414, 55-77.
RUSCIADELLI G., VIANDANTE M.G., CALAMITA F. & COOK A.C.,
(2005) - Burial-exhumation history of the central Apennines
(Italy), from the foreland to the chain building:
thermochronological and geological data. Terra Nova, 17,
560–572.
SESSIONE 10

SESSIONE 10
_______________________
Direction change of the Calabrian Arc: causes and effects
Key words: Seismic reflection, strike-slip tectonics, Subduction
Transform Edge Propagator (STEP).
INTRODUCTION
The oblique and diachronous collision of the Apennine-
Maghrebian Chain with the Apulian and Pelagian continental
forelands, respectively in the North-East and in the South, has
determined the characteristic arcuated structure of this orogen.
The observed interactions between subduction of oceanic crust,
collisional processes and Tyrrhenian backarc extension, suggest
the presence of tears along the lithospheric discontinuities
bordering the Ionian slab, and different behaviours of the
foreland sectors due to their different rheological properties.
Above the discontinuities and across the Calabrian Arc,
significant strike-slip systems have developed, that accommodate
different movements of the main sectors of the chain. A
correlation between the start of the strike-slip systems and their
direction (Fig.1) suggests a clock-wise rotation of the arc
migration during the Plio-Quaternary. This development, with
main left throw of the faults, allowed to transmit the compressive
stress to the zone where low buoyant Ionian lithosphere was
present (DEL BEN et alii, 2008).
MAIN TECTONIC FEATURES
In the Central Mediterranean, some regional lateral
discontinuities separate different crustal domains:
- the old oceanic crust (Tethys), low buoyant and
consequently easily subducting;
- the intermediate crust, related to a continental domain
involved in important extensive tectonics in the Mesozoic time;
- the carbonate platform domain, partially involved in an
extensive regime, generally characterized by lower and upper
crust of normal thickness and by a thick carbonate layers: it
represents a "buoyant" foreland on respect to subduction.
The boundary between these different foreland domains of the
South Apennine-Calabrian Chain, originated tear faults (or STEP,
(*) Dipartimento di Geoscienze, Università degli Studi di Trieste,
delbenan@units.it
ANNA DEL BEN (*)
328
as called by GOVERS &WORTEL, 2005) along the W- Apulia
margin (Policastro and Sibari Gulf) and along the N and E-Sicily
margins: these are deep-seated lithospheric tears which allowed
separation of the subducting Ionian oceanic foreland on respect to
the Apulia and Pelagian continental forelands.
Migration of the chain was joined to some strike-slip faults
that took on different directions in different times. These
directions, as also the chain migration, rotated clock-wise. During
the Upper Miocene-Lower Pleistocene time these faults generally
testify an extensive component, whereas since the Middle
Pleistocene age the new and the reactivated faults crossing the
chain are, except the Vulcano strike-slip, predominantly
transpressive with a left throw. The reactivated faults maintained
the original direction, but in the new stress field they assumed
sometimes a new role (i.e.: the Palinuro fault, activated as left
transcurrent in Upper Miocene-Lower Pliocene age, is extensive
during the Pleistocene; the Bovalino strike-slip fault , transtensive
during the Upper Pliocene/Lower Pleistocene, was reactivated as
transpressive in Middle/Upper Pleistocene time).
Fig. 1 – Main strike-slip faults across the Calabrian Arc: their
different directions show a clockwise rotation in defined stages of
Upper Miocene/Lower Pliocene, Upper Pliocene/ Lower Pleistocene
and Middle/Upper Pleistocene times. In the South Apulia, inversion
tectonics are highlighted (adapted from DEL BEN et alii, 2008; the
magnetic anomalies in the Marsili Basin is from NICOLOSI et alii,
2006).

During the Late Pliocene/Lower Pleistocene time (ESE
migration of the Calabrian Arc), an extensive phase originated
the Marsili Basin, as well documented by NICOLOSI et alii (2006),
that recognize a NNE-SSW trend of the magmatic anomalies
(Fig.1). During the Middle Pleistocene the Marsili Seamount rose
contemporary to a very slow spreading: this phase is probably
related to a right trastensive regime along the newly generated
Vulcano strike-slip, connected to the SSE direction of the
Calabrian Arc.
Also the origin of the Strait of Messina is interpreted in the
context of regional tectonics. Its northern and southern sectors,
characterized respectively by an ENE–WSW and a NNE–SSW
trends, were generally considered to have been originated at
different times, respectively Lower Pleistocene (and possibly
former time) and Middle/Upper Pleistocene (by OGNIBEN 1974;
SELLI 1978; DEL BEN et alii, 1996). This evolution suggests the
relation of the southern sector with the ESE migration of the
chain, and of the northern sector with the more recent SSE
migration.
Several authors analyzed the Calabrian uplift (FERRANTI et
alii, 2006, with references), begun in Middle Pleistocene, with
maximum rate during the Holocene time and in the Strait of
Messina area. This may be related to the direction change of the
chain: a more complex relation between the chain and the
foreland, here affected by lateral crustal discontinuity, occurred
when the ESE-ward migration along the N-Sicily margin became
SSE-ward, parallel to the E-Sicily margin.
The Southern Apennine compression was active until Lower
Pleistocene (PATACCA &SCANDONE, 2007) whereas, since the
Middle Pleistocene, extensional and strike-slip tectonics with
volcanic activity affect the chain. These data confirm the
changing direction in Middle Pleistocene: the migration
concentrated toward the Ionian foreland, involving almost
exclusively the Calabrian sector, and neglecting the Southern
Apennine, where a rebound of the external foreland began.
The South-Apulia represents the foreland of the chain, since
the Miocene. During Pliocene/Lower Pleistocene the collision of
the chain with the Apulia carbonate platform originated important
compressive structures (Gran Sasso, Majella, Monte Alpi, etc.)
while the Calabrian Arc migrated in an oceanic foreland, tilted
below the front. This tilting pulled down also the western margin
of the Apulia platform, affected by coeval extensive faults.
During the Middle Pleistocene the tangential compression
between the chain and the thick foreland caused a deep
compression, highlighted by inversion tectonics and gentle
compressive structures (DEL BEN, 2009).
The fault systems of the Sicily Channel Rift Zone, regionally
attributed to a pull-apart tectonics, show a gradual clockwise
rotation during the Upper Miocene - Present. This seems to be
connected to the changing compressive regime in N-Sicily,
originating and preserving right strike-slip tectonics.
329
CONCLUSION
The main cause of the tectonic events in the Central
Mediterranean area is the regional Africa-Eurasia convergence.
Subduction of the low buoyant oceanic crusts and migration of
the overlaying chains were driven by main unhomogeneities of
the foreland: continental-oceanic boundaries and carbonate
platform margins generally represent the sharing across
differently extended crustal thicknesses.
The Calabrian Arc migrated on the Ionian foreland with
different directions, depending by the inherited main boundaries.
The effects can be recognized in the chain (strike-slip faults,
uplift), in the foreland (STEP, rebound, inversion tectonics,
clock-wise rotation of fault systems) and in the back-arc area
(strike-slip, opening of the Marsili Basin).
REFERENCES
DEL BEN A. (2009) - Earthquakes and shallow structures in
South Adria: evidence of recent inversion tectonics. In: P.
Guarnieri (Ed.) Recent Progress on Earthquake Geology,
Nova Science Publishers, Inc. ISBN: 978-1-60876-147-0.
DEL BEN A., BARNABA C. & TABOGA A. (2008) - Strike-slip
systems as the main tectonic features in the Plio-Quaternary
kinematics of the Calabrian Arc. Mar. Geophys. Res., 29, 1-
12.
DEL BEN A., GARGANO C. & LENTINI R. (1996) - Ricostruzione
strutturale e stratigrafica dell’area dello Stretto di Messina
mediante analisi comparata dei dati geologici e sismici.
Mem. Soc. Geol. It., 51, 703–717.
FERRANTI L., ANTONIOLI F. et al. (2006) - Markers of the last
interglacial sea-level high stand along the coast of Italy:
tectonic implications. Quat. Intern., 145-146, 30-54.
GOVERS R. & WORTEL M.J.R. (2005) - Lithosphere tearing at
STEP faults: Response to edges of subduction zones. Earth
Planet. Sc. Lett., 236, 505-523.
NICOLOSI I., SPERANZA F. & CHIAPPINI M. (2006) - Ultrafast
oceanic spreading of the Marsili Basin, southern Tyrrhenian
Sea: evidence from magnetic anomaly analysis. Geology, 34,
717–720.
OGNIBEN L (1974) - Relazione geologica sullo Stretto di
Messina. GPM, 1–257.
PATACCA E. & SCANDONE P. (2007) - Geology of the Southern
Apennines. Boll. Soc. Geol. It., Spec. Issue No.7, 75-119.
SELLI R (1978) - Appunti sulla geologia del Mar Tirreno. Rend.
Semin. Fac. Sci. Univ. Cagliari, 43, (suppl), 327–349.
SESSIONE 10

SESSIONE 10
Neogene-Quaternary polyphase inversion tectonics in the Central
Apennines (Italy): Implication for seismic hazard assessment
Key words: Central Apennines, polyphase inversion tectonics,
seismic hazard.
INTRODUCTION
The reactivation of pre-existing extensional features is a
fundamental aspect in the evolution and tectonic style of orogenic
belts. Positive inversion occurs when extensional faults linked to
any basin or zone of subsidence and sedimentation reverse their
movement during compressional tectonic and converted the
original subsidence zone to region of uplift. Conversely, negative
inversion occurs in area where uplift was converted subsidence
(e.g., COWARD, 1994).
The Central Apennine chain is an arcuate fold and thrust belt,
strongly influenced during its formation by the Mesozoic
paleomargin architecture and by NNE-SSW oblique thrust ramps
like the Olevano-Antrodoco-Sibillini and the Sangro-Volturno
(e.g., SATOLLI & CALAMITA, 2008 and references therein), that
sign the separation between the different sectors of the Apennines
(e.g., PATACCA et alii, 1990). During Neogene, the Apennines
were characterized by coeval occurrence of normal and thrust
faults along the western and eastern belt margins, respectively
(ELTER et alii, 1975).
The axial part of the chain is characterized by NW-SE normal
fault sets with evidence of Quaternary activity (CALAMITA &
PIZZI, 1994; PIZZI & GALADINI, 2009).
We analyze the relationships between thrusts and normal
faults in the Central Apennines, particularly along the Olevano-
Antrodoco-Sibillini oblique thrust ramp. Geological evidence
reveals a tectonic history characterized by polyphase positive
orogenic and negative post-orogenic tectonic inversion.
POLYPHASE INVERSION TECTONICS
The Central Apennine is characterized by polyphase positive
orogenic and negative post-orogenic inversion tectonics.
During the Neogene orogenesis, positive inversion affected
_________________________
ALESSANDRA DI DOMENICA (*), SARA SATOLLI (*) & FERNANDO CALAMITA (*)
(*) Dipartimento di Scienze, Università “G.d’Annunzio” of Chieti-Pescara,
calamita@unich.it
330
pre-thrusting normal faults, which were either truncated by thrusts
propagating with a shortcut trajectory or reactivated with reverse
kinematics (e.g., BUTLER, 1989), depending on their orientation
with respect to the new compressive regime. The NW-SE and
WNW-ESE trending pre-thrusting normal faults in the backlimbs
of the anticlines were displaced and passively translated in the
hanging-wall blocks of the thrust planes, thus exhibiting shortcut
geometry (shortcut anticlines). Conversely, pre-orogenic normal
faults in the N-S trending anticlines were reactivated in a
transpressive deformational context (reactivation anticlines). The
slip tendency analysis (MORRIS et alii, 1996; COLLETTINI &
TRIPPETTA, 2007) indicates that fault planes of the shortcut
anticlines are misoriented with respect to the compressive stress,
while the fault planes of the reactivation anticlines are welloriented
and prone for reactivation (CALAMITA et alii, 2009).
The Quaternary negative inversion event reactivated the NW-
SE normal faults, while did not affected the Olevano-Antrodoco-
Sibillini and WSW-ENE Gran Sasso oblique thrust ramps, which
represented barriers for the NW-SE active normal faults growth,
as also documented by PIZZI & GALADINI (2009).
CONCLUSION
We propose a model of Neogene positive and Quaternary
negative inversion tectonics in which NNE-SSW cross-structures
have been interpreted as pre-thrusting normal faults that
undergone reactivation, during Messinian-Pliocene positive
inversion, while NW-SE faults represent pre-thrusting normal
faults displaced by thrusts, according to a shortcut trajectories,
and subsequently reactivated as normal faults during Quaternary
negative inversion (Fig. 1).
In such a context the NNE-SSW Olevano-Antrodoco-Sibillini
and the E-W Gran Sasso thrust ramps individualize three
independent sectors of the Quaternary extensional activity,
assuming a role of barriers. This observation is in accordance
with the distribution of the recent seismic sequence of L’Aquila
that displays an evident gap close to the E-W Gran Sasso oblique
thrust ramp that split the whole seismicity of the Laga Mountains,
related to the Monte Gorzano fault, from the L’Aquila seismicity,
associated with the Paganica fault.
As a consequence, evaluating the ability of pre-existing crossstructure
to control the growth of NW-SE trending normal
propagating fault is crucial in fault segmentation analysis and,

Fig. 1 – 3D polyphase inversion tectonics model (not in scale): I) prethrusting
normal faults; II) Neogene positive inversion tectonics thought
reactivation of the NNE-SSW trending normal fault and shortcut of the NW-
SE trending normal faults; III) Quaternary negative inversion tectonics of the
NW-SE trending normal faults. Light grey represents the sedimentary cover
(5-9 km thick). White and black lines represent active and inactive
structures, respectively.
hence, in seismic hazard assessment.
REFERENCES
BUTLER R. W. H. (1989) - The influence of pre-existing basin
structure on thrust system evolution in the western Alps. In:
M. A. Cooper and G.D. Williams (Eds.) - Inversion tectonics.
Geol. Soc. Lon. Spec. Publ., London, 105-122.
331
CALAMITA F., ESESTIME P., PALTRINIERI W., SCISCIANI V. &
TAVARNELLI E. (2009) – Structural inheritance of pre- and
syn- orogenic normal faults on the arcuate geometry of
Pliocene-Quaternary thrusts: examples from the Central and
Southern Apennine Chain. Ital. J. Geosci., 128/2, 381-394.
CALAMITA F. & PIZZI A. (1994) – Recent and active extensional
tectonics in the southern umbro-marchean Apennines (central
Italy). Mem. Soc. Geol. It., 48, 541-548.
COLLETTINI C. & TRIPPETTA F. (2007) - A slip tendency analysis
to test mechanical and structural control on aftershocks
rupture planes. Earth Plan. Sci. Lett., 255, 402-413.
COWARD M. P. (1994) – Inversion tectonics. In: P. L.Hancock
(Ed.), Continental Deformation: Oxford, Pergamon, p. 289-
304.
ELTER, P.,GIGLIA G., TONGIORGI M. & TREVISAN L. (1975),
Tensional and compressional areas in recent (Tortonian to
Present) evolution of north Apennines. Boll. Geofis. Teor.
Appl., 17, 3-18.
MORRIS A., FERRIL A. & HENDERSON D. B. (1996) - Slip
tendency analysis and fault reactivation. Geology, 24 (3),
275-278.
PATACCA E., SARTORI R. & SCANDONE P. (1990) – Tyrrhenian
basin and Apenninic arcs: Kinematic relations since late
tortonian time. Mem. Soc. Geol. It., 45, 425-451.
PIZZI A. & GALADINI F. (2009) – Pre-existing cross-structures
and active fault segmentation in the northern-central
Apennines (Italy). Tectonophysics, 476, 304-319.
SATOLLI S. & CALAMITA F. (2008) – Differences and similarities
between the Central and Southern Apennines (Italy):
examining the Gran Sasso vs. the Matese-Frosolone salients
using paleomagnetic, geological and structural data. J.
Geophysical Res., 113, B10101. doi: 10.1029/2008JB005699.
SESSIONE 10

SESSIONE 10
Geological and structural evolution of the Onshore-Offshore Murge
and its tectonic implications (Adria/Apulia plate boundary, SE Italy)
Key words: Adria, Apulia, Murge, Rosaria Mare intraplatform
Basin.
INTRODUCTION
In the context of a research project focused on the solution of
geological problems related to the Mesozoic kinematics of the
Adria/Apulia plate boundary, here we present new data on the
structural evolution of the Onshore-Offshore Murge mainly
focused within the Rosaria Mare intraplatform Basin area
(R.M.i.B.; NICOLAI &GAMBINI, 2007, see Fig.1 for location).
This basin developed within the Apulian Carbonate Platform
domain (A.C.P.) during the Upper Cretaceous-Miocene, and
represents a key structural feature to assess the kinematics of the
Adria/Apulia plate boundary during early convergence between
African and Eurasian plates (SCHETTINO &TURCO, 2009).
The main aim of this work is the formulation of a conceptual
tectonic model of the central A.C.P. by integrating offshore
seismic data with available onshore stratigraphic data. The
current work was carried out by employing the following
methodologies: i) stratigraphic analysis of onshore and offshore
log data obtained from commercial deep exploration wells, ii)
structural interpretation of offshore seismic reflection profiles, iii)
geological mapping of Cretaceous-to-Miocene carbonate rocks
cropping-out in the selected area, and iv) 3D modelling of both
stratigraphic horizons and fault surfaces (by using the TrapTester
6 software, Badley Geoscience Limited).
ONSHORE-OFFSHORE MURGE
Onshore, a regional unconformity marked by bauxites
deposits of Upper Cenomanian-Turonian age, highlights
differential emersion within the A.C.P.. This differential emersion
was followed by transgression of shallow water carbonatic facies
during the Coniacian-Lower Campanian. Subsequently, a new
_________________________
FABRIZIO FELICI (*), PIETRO PAOLO PIERANTONI (**) & EUGENIO TURCO (**)
(*) Dipartimento di Scienze della Terra, Università degli Studi di Perugia,
fabriziofelici79@gmail.com
(**) Scuola di Scienze e Tecnologie, Sezione Geologia, Università di
Camerino.
332
tectonic phase, led to the drowning of the south-eastern sector of
the A.C.P. (PIERI &LAVIANO, 1989; BORGOMANO, 2000) within
the studied area, as also recorded by the R.M.i.B. opening during
the Campanian-Maastrichtian stages.
Offshore seismic reflection profiles, carried-out across this
basin and areas nearby, show a complex structural setting related
to the Upper Cretaceous tectonic. Normal faults, folds and
transpressional lineaments influenced the sedimentation of
platform-to-basin carbonates and, furthermore, led to the
disarticulation and instability of the A.C.P. margin. Seismic
profiles interpretation, 3D reconstructions and other geological
evidences, allow us to conceptualize the presence of a possible
negative flower geometry, associated to a deep transcurrent fault,
in correspondance of the R.M.i.B..
CONCLUSIONS
Summarizing, a transpressional regime begun to be active in
the Murge onshore/offshore during the Cenomanian and it
preceded the instauration of a left-lateral strike-slip tectonic
regime from, at least, the Campanian.
This tectonic phase probably continued during the Paleocene-
Eocene but the lack of sedimentation, both in the platform and the
basin, does not allow to well constraint the tectonic activity
during that lapse of time.
During the Oligocene, reactivation and inversion of WNW-
ESE normal faults and strike slip faults within the R.M.i.B.,
suggest a change in the direction of the convergence vector
between the Eurasian and the African plates.
Northernmost, along the E-W trending Mattinata-Gondola
line, a Cretaceous tectonic activity has been previously
documented and it has been linked, even if not fully constrained,
to strike-slip movements that occurred from the Upper
Cretaceous/Lower Paleocene (MORELLI, 2002; ARGNANI et alii,
2009).
This means that, at least during the Upper Cretaceous, two
main parallel E-W fault zones (in present-day coordinates),
Mattinata-Gondola and R.M.i.B., were active within the Apulian
region and the Southern Adriatic Basin.
In conclusion we link that tectonic assemblage to a wide zone
of deformation related to the incipient Adria/Apulia continental
transform plate boundary.

Fig.1 - Geological map of the Apulian region between the Gargano promontory and the town of Brindisi (redrawn from Carta Geologica d’Italia, APAT, 2004
and integrated with offshore data from NICOLAI &GAMBINI, 2007). Black square inset indicates the location of the studied area.
REFERENCES
ARGNANI A., ROVERE M. & BONAZZI C. (2009) - Tectonics of the
Mattinata fault, offshore south Gargano (southern Adriatic
Sea, Italy): Implications for active deformation and
seismotectonics in the foreland of the Southern Apennines.
GSA Bulletin, 121, 9/10, 1421–1440.
BORGOMANO J.R.F. (2000) - The Upper Cretaceous carbonates
of the Gargano-Murge region, southern Italy: a model of
platform-to-basin transition. AAPG Bulletin, 84, (10), 1561-
1588.
MORELLI D. (2002) - Evoluzione tettonico-stratigrafica del
margine Adriatico compreso tra il promontorio garganico e
Brindisi. Mem. Soc. Geol. It., 57, 343-353.
NICOLAI C. & GAMBINI R. (2007) - Structural architecture of the
Adria platform-and-basin system. Boll. Soc Geol. It. (Ital. J.
Geosci.), Spec. Issue, 7, 21-37.
PIERI P. & LAVIANO A. (1989) - Tettonica e sedimentazione nei
depositi Senoniani delle Murge sud-orientali. Boll. Soc. Geol.
It., 108, 351-356.
333
SCHETTINO A. & TURCO E. (2009) - Break-up of Pangaea and
plate kinematics of the central Atlantic and Atlas regions.
Geoph. J. Int., 178, 1078-1097.
SESSIONE 10

SESSIONE 10
High-pressure external continental units (HECU) belt at the
boundary between Alpine and Hercynian Corsica: a key for the
understanding the Tertiary subduction and exhumation processes
along the European plate margin
ALESSANDRO MALASOMA (*), MICHELE MARRONI (*) (°) & LUCA PANDOLFI (*) (°)
Key words: Continental crust, Corsica, exhumation, HP/LT
metamorphism, subduction, Tertiary.
INTRODUCTION
In Alpine Corsica, pervasive deformation associated with
high-pressure/low-temperature (HP/LT) metamorphism has been
recognized not only in oceanic units (Schistes Lustrés Complex),
but also in tectonic slices derived from the continental margin of
the Corsican/European plate. Findings of mineral assemblages
indicative of HP/LT metamorphism in the continental units has
been reported in the literature (e.g. MOLLI &TRIBUZIO, 2004),
but it has generally been under-evaluated.
The recent data indicate that the HP/LT peak metamorphism
in the continental-derived tectonic units is more widespread than
previously reported, and the occurrence along the Hercynian and
Alpine Corsica boundary of a continous belt of HP/LT
metamorphic (HECU) units.
THE HECU BELT
The HECU belt extends from the Balagne region (northern
zone), to the Asco and Golo valleys (central zone) and the Corte
region (southern zone). The units belonging to HECU belt have
been thrust westward onto the “autochthon” domain represented
by the Variscan basement covered by a thin eocenic sedimentary
sequence. In turn, the HECU belt is overlain by several units
belonging both to the Nappes supérieures and to the Schistes
Lustrés Complex. All the units from the HECU belt includes
metamorphic rocks derived from a succession representative of
the European continental margin. Taking into account the
stratigraphies from the different units, the original succession
_________________________
(*) Dipartimento di Scienze della Terra, Università di Pisa
(°) Istituto di Geoscienze e Georisorse, CNR
Lavoro eseguito nell’ambito del progetto PRIN con il contributo finanziario
dell’Università di Pisa.
334
consisted of Variscan basement rocks topped by Late
Carboniferous-Early Permian volcano-sedimentary deposits,
Triassic dolomites and dolomitic limestones, carbonate deposits
(Jurassic?), polymict coarse-grained breccias (from Cretaceous?
Tertiary?) and Middle Eocene siliciclastic turbidite deposits.
In the northern zone, the HECU units crop out in two
different structural positions. The Fuata-Pedanu Unit (FPU) crops
out below the ophiolite-bearing Balagne Nappe. Below the FPU,
another continental-derived unit, referred as Palasca-Moltifao
Unit (PMU), crops out along the western boundary of the nortern
zone. The PMU, as the FPU, displays an Alpine polyphasic
deformation associated with HP metamorphic recrystallization.
In the central zone, the HECU belt consists as a stack of km-size
units bounded by sub-vertical, N-S trending shear zones. These
units, cropping out below the ophiolite-bearing Schistes Lustrés
Complex and Pineto unit, are represented, from west to east, by
Popolasca-Castiglione Unit (PCU), the Croce d’Arbitro Unit
(CAU) and Piedigriggio-Prato Unit (PPU). In all of these units a
HP/LT mineral assemblage has been recognized. In the Corte
region, the HECU belt is characterized by the same tectonic
setting described for the central zone. In this region, the HECU
belt is classically divided (AMAUDRIC DU CHAFFAULT &SALIOT,
1979) in two main tectonic units, hereafter referred to as Punta di
Zurmulu Unit - PZU and Punta di Corbu Unit - CRU,
respectively.
The HECU record a polyphase deformation history of Alpine
age, characterized by superimposed foliations and folds
structures, developed mainly inside the meta-sedimentary covers.
In contrast, the basement rocks (mainly metagranitoids) are
characterized by heterogeneous deformation with development of
map-scale cataclastic-mylonitic shear zones.
All tectonic units are affected by two main ductile
deformation phases (D1 and D2), acquired to deep structural
levels. A third phase (D3), characterized by asymmetric eastverging
folds, overprints the previous structures. The structural
evidences suggest that all these units were coupled before the D3
phase. About the D1 and D2 phases, no evidences that these
deformations are synchronous in all the studied units have been
detected, but the very similar deformation features and the
HP/LT character of the metamorphism related to the D1 phase

suggest that these phases have been achieved by the studied units
in the same geodynamic setting.
The D1 phase structures are generally preserved as relict
structures inside the microlithons of the main foliation (S2). The
S1 foliation can be easily observed in the hinge zone of the
second phase folds (F2), while along the F2 folds limbs some S1
fabric elements occur as relicts re-aligned along the S2 foliation.
Therefore, the resulting surface, derived by the superposition of
the S1 and S2 foliations, can be considered as a S1+S2 composite
foliation. Associated to D1 phase deformation, low-grade
blueschist facies peak metamorphism was recognized. The
estimated P-T conditions are: 0.40–0.55 GPa and 250-350 °C for
both granitoids and eocenic deposits from the PCU (BÉZERT &
CABY, 1988); 0.50–0.80 GPa and 300–370 °C for the basement
rocks from the CAU (MALASOMA et alii, 2006); 0.60 ± 0.15 GPa
and 325 ± 20 °C for the coarse-grained polymict breccias
(Volparone Breccia) from the FPU (MALASOMA &MARRONI,
2007). To the D1 phase can be referred also the low-temperature
cataclastic-mylonitic deformation in the sheared metagranitoids
where a development of continuous foliation, (Sp) associated to a
stretching/mineral composite lineation (Lp) is found. The
kinematic criteria inferred from metagranitoids indicate a top-tothe-W
sense of shear. The presence of domains in which synkinematic
Na-amphibole and Si-rich phengite are growth along
the Sp foliation, testifies the development of the shear zones
under HP/LT conditions.
The D2 phase is characterized by asymmetric, noncylindrical,
sometime rootless, tight to isoclinal folds (F2) also
recognized at map-scale. The asymmetric F2 folds provide a topto-the-W
shear sense. The S2 axial-plane foliation can be
classifiable as a continuous and pervasive schistosity. The
composite mineral/stretching L2 lineation is formed by aligned
quartz and feldspar porphyroclasts and by aggregate of quartz
ribbons. During the D2 phase, the metamorphic P-T conditions
show a transition from the blueschist to greenschist facies.
The D3 phase structures are mainly represented by
asymmetric E-verging F3 folds. Usually, the S3 foliation can be
observable as brittle disjunctive cleavage in the more competent
beds and as a pervasive gradational crenulation cleavage in the
fine-grained beds. Asymmetric E-verging F3 folds deform and
sometimes overturn the main contacts between the HECU
stacked tectonic units. In addition, the F3 folds, with flat-lying
axial planes and horizontal fold axes, can be interpreted as
originating from vertical shortening and folding of pre-existing
non-horizontal layers.
CONCLUSIONS
As a whole, a continuous belt of continental slices
characterized by HP/LT metamorphism of Tertiary age can be
identified from the Balagne (N of studied area) to the Corte area
(S of studied area).
In the HECU units, the three main deformation phases (D1,
335
D2, D3) are younger than Middle Eocene (age of the turbiditic
deposits involved in the D1 deformation phase) but older than
Burdigalian (the age of the oldest undeformed deposits of the
Francardo–Ponte Leccia Basin). Thus, the D1, D2 and D3 phases
can be regarded as ranging in age from Late Eocene to Early
Miocene. On the base of structural features and metamorphic
conditions the D1 phase recognized in the HECU can be
interpreted as related to the deformations achieved during their
underplating at ~15-25 km of depth into the accretionary wedge
(as testified by development of HP/LT metamorphic mineral
assemblages), while the D2 and D3 phases can be related to the
exhumation history. Particularly, the D2 phase was associated to
the first stage of exhumation driven by a syn-contractional
westward thrusting onto the eastern margin of the Hercynian
basement and the D3 phase can be interpreted as related to the
last stage of exhumation history during the Oligo-Miocene
extensional tectonics.
This picture supports the hypothesis that large portions of the
Corsican/European continental margin (previously regarded as
weakly metamorphosed or non-metamorphosed) were deformed
under HP/LT metamorphic conditions during their involvement
in the tectonics connected with Alpine subduction. All these units
were subsequently juxtaposed against the metamorphic and nonmetamorphic
oceanic units during the following complex
exhumation history.
REFERENCES
AMAUDRIC DU CHAFFAULT S. & SALIOT P., (1979) - La région de
Corte: sectèur-clè pour la comprèhension du mètamorphisme
alpine en Corse. B. Soc. Geol. Fr., 21, 149-154.
BEZERT P. & CABY R. (1988) - Sur l’âge post-bartonien des
évenements tectono-metamorphiques alpins en bordure
orientale de la Corse cristalline (Nord de Corte). B. Soc.
Geol. Fr., 8, 965-971.
MALASOMA A. & MARRONI M., (2007) - HP/LT metamorphism
in the Volparone Breccia (Northern Corsica, France):
evidence for involvement of the Europe/Corsica continental
margin in the Alpine subdution zone. J. Metamorph. Geol.,
25, 529-545.
MALASOMA A., MARRONI M., MUSUMECI G. & PANDOLFI L.,
(2006) - High-pressure mineral assemblage in the continental
unit of Alpine Corsica: new findings in the parautochtonous
units from Popolasca-Francardo area. Geol. J., 41, 49-59.
MOLLI G. & TRIBUZIO R. (2004) - Shear zones and metamorphic
signature of subducted continental crust as tracers of the
evolution of the Corsica/Northern Apennine orogenic system.
In: G.I. Alsop, R.E.Holdsworth, K.J.W. McCaffrey & M.
Hand (Eds.) - Flow Processes in Faults and Shear Zones.
Geol. Soc. London, Spec. Pub., 224, 321–335.
SESSIONE 10

SESSIONE 10
Neotectonics in the inner Northern Apennines: evidence from late
Quaternary alluvial sediments of the northern Siena Basin
Key words: Alluvial sediments, inner Northern Apennines,
neotectonics, Quaternary, Siena Basin.
INTRODUCTION
In this presentation we document the occurrence of faults
affecting late Quaternary alluvial terraced deposits related to the
hydrographic evolution of the Arbia River.
This river, located in the northern sector of the Siena Basin
(southern Tuscany), is characterized by several fluvial terraces
developed along its fluvial pattern. One of the lower terraced
episode, with an elevation that varies between about 230 and 210
meters a.s.l., is well evident along one of its right tributary (the
Bozzone Creek). This terrace is probably very recent in age
(maybe Late Pleistocene-Holocene), due to the reduced elevation
on the actual valley bottom (about 10 m). Architecture and
sedimentological features of this alluvial terraced deposit are
evident in a small quarry on the right side of the creek.
Sediments consist of gently inclined, alternated beds of sand
and gravel, prograding on sub-horizontal sandy layers. Gravel
ranges in size from pebble to large cobble and single beds
generally show rich sandy matrix. Open-framework layers are
also present.
The whole outcrop is affected by high-angle normal faults,
N100°-120° striking, show normal offsets ranging from few
decimeters to maximum one meter. They are arranged in grabenlike
association and represent the expression of a soft-sediment
deformation. So, their kinematics cannot be defined with
certainty.
The fault zones, millimeter thick, result mineralized suggesting
their fundamental role for channeling fluids. Faults dissecting
pebbly levels result hydrothermally altered as highlighted by the
occurrence of widespread iron-hydroxides within the matrix, and
locally bounding each pebble. The whole evidences indicate that
an hydrothermal system was coeval during the faults activity.
Such a scenario is coherent with neotectonics evidences as
documented in the north-eastern side of the Siena Basin
(Rapolano area), where N45°-N70° and N100°-N120° striking
_________________________
IVAN MARTINI (*), ANDREA BROGI (*), ENRICO CAPEZZUOLI (*) & FABIO SANDRELLI (*)
(*) Dipartimento di Scienze della Terra, Università di Siena,
martini.ivan@unisi.it; brogiandrea@unisi.it, capezzuoli@unisi.it
sandrelli@unisi.it
336
oblique to left-lateral strike-slip faults were responsible for a
widespread hydrothermal circulation and travertine deposition
(BROGI &CAPEZZUOLI, 2009).
On the whole, neotectonics activity in a transtensional tectonic
setting is supported by new evidences also from the northern
Siena Basin.
REFERENCES
BROGI A. & CAPEZZUOLI E. (2009) - Travertine deposition and
faulting: the fault-related travertine fissure-ridge at Terme S.
Giovanni, Rapolano Terme (Italy). Int. J. Earth Sci. (Geol.
Rundsch.), 98, 931–947
.

Hot fluid pumping along shallow level collisional thrusts: the Monte
Rentella Shear Zone, Umbria Apennine, Italy
FRANCESCA MENEGHINI (*), FLAVIA BOTTI (*), LUCA ALDEGA (°), CHIARA BOSCHI (**),
SVEVA CORRADO (°), MICHELE MARRONI (*) (**) & LUCA PANDOLFI (*) (**)
Key words: Cataclastic flow, dilational jogs, fluid migration,
thrust deformation, Umbria Apennine.
INTRODUCTION
Evidences of fluid circulation along fault-related fracture
systems comes from in situ measurements in active tectonic
regions and from the occurrence of mineral-infused vein systems
in ancient orogenic belts. All the exploited hydrothermal mineral
deposits on earth and many reservoirs or conduits for gas rely on
the availability of large volumes of fluids flowing along faults.
Also, the control of overpressured fluid on the state of stress
along fault zones is considered as a crucial factor controlling the
seismic character of faults. We report here on the
multidisciplinary investigation we carried out on a well-exposed
shallow shear zone, responsible for imbrication and thrust sheet
development of the Apennine foredeep successions during
Miocene continental collision.
THE RENTELLA SHEAR ZONE
The studied thrust crops out in the Lago Trasimeno area as a
ramp segment of the system of internal thrusts in the Rentella
Unit, a unit of foreland-foredeep succession deposited in a
paleogeographic domain between the Tuscan and the Umbria-
Marche Domains. The thrust zone is infused by a complex system
of calcite veins. With the main goal of reconstructing the
structural and temperature fluid rock-interaction during shear
zone activity we associated a detailed field and microstructural
analysis of the MRSZ structure and deformation fabrics, with
vitrinite reflectance measurements, XRD analysis on clay
minerals and C, O stable isotopes analyses. The Monte Rentella
_________________________
(*) Dipartimento di Scienze della Terra, Università di Pisa,
fbotti@dst.unipi.it
(**) Istituto di Geoscienze e Georisorse, C.N.R, sezione di Pisa
(°) Dipartimento di Scienze Geologiche, Università degli Studi Roma TRE
Lavoro eseguito con il contributo finanziario dell’Università di Pisa
337
Shear Zone (MRSZ, 160°-170°/60°-70°SW) is a 45-50 m thick
thrust zone juxtaposing varicoloured pelagic and emipelagic
marls (Monte Rentella Fm) over siliciclastic turbidites
(Montagnaccia Fm). Disruption concentrates in the marls of the
Monte Rentella Fm, allowing to a MRSZ asymmetrical
architecture, with a 3.5 m thick core zone (COZ) bounded by
strikingly different footwall and hangingwall damage zones. The
footwall damage zone (FDZ) develops in massive sandstones
with deformation accommodated by a fracture and dissolution
foliation. Fractures are arranged as R- and R'-type Riedel planes
associated with a main shear surface striking 130°-160°/20°-
40°SW and showing a top-to-NE sense of shear. Fabric in the 3.5
m thick core zone (COZ) is very penetrative and includes many
typical features of brittle shear zones in pelitic to marly
lithotypes, such as: a strongly penetrative scaly foliation, brittle
S-C structures, shear-related asymmetric folds and extensive
veining. Foliation is defined by an anastomosing set of polished
and striated fracture planes with mm scale spacing. Brittle S-C
structures develop at all scales and their arrangement indicates a
top-to-E-NE sense of shear. Foliation is also folded by strongly
asymmetric, tight to isoclinal folds with boudinaged limbs. The
HDZ develops in the central-upper portion of the Monte Rentella
Fm also deforming marly lithotypes. HDZ fabric is characterized
by well-developed S-C brittle structures, similar to those
observed in the core, but distributed with less frequency and
intensity.
S- and C- planes are infused by a complex network of calcite
veins. Vein density in the fault core is up to 2 times higher that
that observed in the damage zone, suggesting extremely high
fluid circulation focused in the fault core. Veins arranged along
the C-type shear planes seem to have accommodated
deformation, being characterized by many crack-and-seal
episodes, and a texture comparable to that already described in
literature for dilational jogs or for striped veins. Jogs of different
veining episodes show frequently a staircase shape that can be
used as a shear sense indicator, always consistent with a top-tothe-NE
sense of shear. The characteristics of calcite twins in the
veins allows to a qualitative estimate of temperature of formation
ranging from 150° to 300°C. The vitrinite reflectance and clay
mineralogy analyses suggest temperature range from 60° to 100-
110°C, and represents the maximum value reached by the whole
unit and by any episode of internal imbrication, as is the MRSZ.
SESSIONE 10

SESSIONE 10
These paleo-temperature values across the MRSZ section indicate
that the Rentella Unit experienced a tectonic burial from 3 km, in
the western sector, to around 2 km toward the E, in the frontal
part of the unit, using a thermal gradient at surface of 30°C and
10°C. The stable isotope data indicate a small but systematic
variation in δ 18 O values across the section, with δ 18 O values of
the veins lower than that of the adjacent host rocks, and δ 18 O
values of the veins and host rocks series decreasing regularly
from the underformed rocks to the fault core. δ 18 O values of veins
lower than those of the host rocks suggest that fluids responsible
for the veins precipitation were not in equilibrium and/or
isotopically buffered by surrounding host rock. Externally
derived hotter fluids, migrating along the fault and not in isotope
equilibrium with the host rocks, are believed to be responsible for
the observed vein system. In fact, a fluid with temperature of
150°C interacting significantly with the host rock would produce
the shifting to lighter δ 18 O observed from the veins to the
neighbouring host rock. At the same time, since most of the fluid
flow is focused in the core zone the significant interaction of host
rock and fluids would explain the decrease in δ 18 O values of both
host and veins from the undeformed zone to the core. The
temperature of ca. 150°C would fit with the qualitative estimate
based on the shape of calcite twins in the vein infilling.
In concert, all these observation picture a thrust zone evolving
through cycles of delocalization and localization allowing to a
complex, asymmetric fault zone geometry. Shear strain
distribution is heterogeneous, with deformation accommodated
by brittle fractures in the competent blocks and by viscous flow in
the marl matrix. Cataclastic flow and pressure solution during
shear are the main deformation processes active. The build-up of
overpressure in fluids and their attempt to escape to the surface at
failure are suggested as the cause of syntectonic development of
the hydrofracture system described in both the core and the
damage zones of the MRSZ. The cyclic opening and closure of
fractures create distinct mechanical and permeability
heterogeneities that focus and transmit fluid flow along and
across the fault zone. The intense involvement of hot fluids (150-
200 °C), focused mainly in the core zone, produced both a
precipitation of carbonate veins and a partial recristallization and
geochemical modification of the host rocks. A possible origin of
these high temperature fluids could be found at depth, where
metamorphic reactions and mechanical expulsion release large
quantities of fluids toward the surface. The provenance of fluids
from deeper portions of the collisional belt would also explain the
contrast between this estimated temperature and the burial depth
reconstructed for thrust.
338
Fig. 1 – Structural profile across thrust dip showing structural features

Key words: Depocentre migration, Messinian salt, Northern
Apennines, tectono-sedimentary evolution, Volterra Basin.
The internal side of the Northern Apennines is characterised
by the presence of Late Miocene-Quaternary basins resting on top
of the already structured thrust-fold belt. Their origin has been
commonly related to an extensional tectonic regime,
progressively following the northeastward migration of the thrust
front, either in the frame of back-arc extension, or of gravity
spreading collapse. In this scenario, thrusting has been assumed
to pre-date hinterland basin development.
The Volterra Basin is one of the largest Neogene basins in
central Tuscany. Pliocene marine sediments fill its central part,
whereas Tortonian-Messinian, fluvio-lacustrine and shallow
marine deposits, often displaying a vertical to steeply dipping
attitude, crop out at its margins. Specifically to the Messinian, the
succession has been classically subdivided into brackish-shallow
marine mudstones (Pycnodonta clays auct.), referred to the preevaporitic,
final early Messinian, overlain by a sedimentary
complex including primary and resedimented evaporites
variously interbedded with terrigenous deposits, on the whole
recording the late Messinian Salinity Crisis (MSC) and the
subsequent lago-mare realm. Around Saline di Volterra, in the
southern portion of the basin, halite, exploited since the last
century, gypsum and terrigenous deposits characterise the buried
Messinian succession.
A kind collaboration with the Solvay Chimica Italia S. p. A.
allowed us to analyse in detail a new core drilled in the Messinian
succession east of Saline di Volterra, which, from biostratigraphic
analyses of ostracod and palynomorph assemblages, is referred to
the latest Messinian (i.e lago-mare) (BERTINI et alii, 2008). The
core has almost completely recovered about 170 meters of Mio-
Pliocene sediments extending about 10 meters below the halite
deposits. Within the upper Miocene portion, the stratigraphic and
sedimentologic analysis has allowed to establish distinct units
including terrigenous deposits, reworked gypsum and three halite
_________________________
Messinian tectono-sedimentary evolution of the Volterra Basin
(Northern Apennines)
GIOVANNA MORATTI (*), MARCO BENVENUTI (**) & PAOLO SQUARCI (°)
(*) CNR, Istituto di Geoscienze e Georisorse, Firenze, gmoratti@geo.unifi.it
(**) Dipartimento di Scienze della Terra, Università di Firenze,
marcob@geo.unifi.it
(°) p.squarci@gmail.com
Lavoro eseguito nell’ambito del progetto PRIN 2006 (UO Firenze,
Responsabile Adele Bertini).
339
intervals. This core has represented the starting point for a
revision of the surface geology, through a detailed mapping at the
1:10,000 scale with a profitable field correlation of sedimentary
facies and structural description and interpretation.
In stratigraphic terms this revision has ascertained the lack of
an outcropping equivalent of the buried halite, which evidently
deposited in restricted depocentres and possibly in a very short
time interval. Furthermore, evaporites exposed in the southern
Volterra basin, which are mainly clastic, may be referred to the
late Messinian (post-MSC). This suggests that the primary
evaporites, recording all over the Mediterranean basins the late
Messinian Salinity Crisis, have been almost completely eroded
and redistributed as clastic deposits during the post-evaporitic
time.
The geologic-structural data outline a high degree of
deformation of the Messinian units, less expressed but still
occurring also in the overlying Pliocene deposits, with the
development of reverse faults and polyphasic folds at different
scales. The different degree of deformation in the various units is
outlined by the occurrence of angular unconformities. A major
unconformity separates the lower Messinian Pycnodonta clays,
which are usually tightly folded and often steeply dipping, from
the overlying post-MSC units, which are more gently folded. All
these structural lines of evidence suggest crustal shortening as
responsible for the formation and development of the different
depocentres along with their overall northeastward migration.
The highest degree of deformation is found in correspondence
of major compressive structures evident in the subsoil from the
interpretation of a series of published commercial seismic lines.
This, joined to the reinterpretation of several core stratigraphies
from the Solvay Company and from oil exploration, has allowed
to extend to the subsoil the surface geology determining the
definition of a new tectono-sedimentary model for the Messinian
evolution of the southern Volterra basin.
REFERENCES
BERTINI A., FARANDA C., GENNARI R., GLIOZZI E., GROSSI F.,
LUGLI S., MENICHETTI E. & TESTA G. (2008) - Integrated
stratigraphic analyses of the Messinian succession in the
Montecatini Val di Cecina-Pomarance area (Tuscany,
Volterra Basin). In: F. Lozar (Ed.) - Alba e tramonto della
crisi messiniana, 10-11 ottobre 2008, Alba (Cn), Riassunti,
pp. 11-12.
SESSIONE 10

SESSIONE 10
Neogene deformation in metamorphic units of eastern Elba island,
(northern Apennine): insight from Calanchiole and Felciaio
mylonitic marbles in the Porto Azzurro pluton contact aureole
Key words: Igneous bodies, late Neogene tectonics northern
Tyrrhenian Sea-northern Apennines, upper crustal
structures.
In the northern Tyrrhenian Sea, late Miocene intrusive rocks
namely the Monte Capanne pluton and the Porto Azzurro pluton
(8 - 5.9 Ma) were emplaced at upper crustal level (< 0.2 GPa) in
the thrust systems of Elba Island. The emplacement of intrusive
rocks is currently explained in the context of late Miocene
extensional tectonics with eastward translation of the upper most
tectonic units from central to eastern Elba along two fault zones:
the Central Elba Fault and the Zuccale Fault. We report new
detailed structural data undertaken along a continuous natural
cross section through the contact aureole of Porto Azzurro pluton
(Fig. 1), where spatial and temporal relationship between granite
emplacement, contact metamorphism and deformation are clearly
exposed. Along this section, the contact aureole consists of a
rheologically inhomogeneous multilayer stack which attains a
thickness of 1.3 km and shows a complex pattern of metamorphic
zones associated with strain localization in carbonate mylonites
within west dipping decameter-scale shear zones namely the
Calanchiole and Felciaio shear zones (Figs 2a, b).
These shear zones are marked by strongly sheared carbonate
hornfels showing NS trending and west dipping mylonitic
foliation (Fig 2c), sheath folds and upright folds (Fig. 2d). Mesoand
microstructural features (Figs 2e, f) of the mylonitic marble
hornfels are consistent with the development of deformation
structures as result of progressive deformation coeval with
contact metamorphism. In particular mylonitic marble fabrics
highlights that the most of the deformation and displacement
closely followed the contact metamorphism thermal peak and
were coeval with the retrograde evolution. This matches the
dominant occurrence of mylonitic fabrics developed under
amphibolites to greenschist facies conditions with high grade
mineral assemblage and high-temperature microstructures
preserved into low strain domains.
____________________
(*) Dipartimento Scienze della Terra, Pisa, gmi@dst.unipi.it
(**) Istituto Geoscienze e Georisorse - CNR Pisa, luca.vaselli@igg.cnr.it
GIOVANNI MUSUMECI (*) & LUCA VASELLI (**)
340
The westward dipping of shear zones and mylonitic foliation
coupled with a top to the east sense of movement indicate that
they correspond to decametre thick ductile thrust zones, which
activity led to internal stacking of contact aureole.
Therefore, the Porto Azzurro contact aureole in eastern Elba
Island gives clear evidence of synkinematic contact
metamorphism which is related to emplacement of intrusive
rocks during active tectonics.
In particular the geometry of deformation structures and the
internal stacking of the contact aureole are consistent with
shortening coeval with late Miocene (5.9 Ma) emplacement and
cooling of the Porto Azzurro pluton, as already recognized in the
hinterland portion of northern Apennines and in particular in the
southern portion of the Larderello geothermal field.
Fig 1 - Porto Azzurro contact aureole. a) geological sketch map and b) schematic
cross section

Fig. 2 - a) Calanchiole shear zone; b) Felciaio shear zone; c) mylonitic foliation and d) sheath folds; microfabrics in
Calanchiole shear zone (e) and Felciaio shear zone (f)
2
341
SESSIONE 10

SESSIONE 10
Key words: Triassic Evaporites, Northern Apennines.
The trending of Triassic evaporites cropping out at Sassalbo
(Tuscany) and in Secchia Valley (Emilia Romagna) represents
one of the most important trans-Apennines lineaments to gain
informations about the structural evolution of the apenninic chain
from the collisional to the more recent extensional tectonic
phases.
Two groups of outcrops have been distinguished: 1) Sassalbo
group; 2) Secchia Valley group.
Taking into account abundant published data and new field
observations some considerations on their tectonic evolution and
emplacement are proposed.
These deposits, with their associated sedimentary sequence,
belong to the internal Tuscan realm. In spite to the common
origin and provenance, at a certain time of the geological history
(Tertiary) they have been dismembered and a portion has been
translated towards the Adriatic-Padan region, originating the salt
outcrops of Secchia Valley, the most external triassic evaporites
nucleo of the apennine mountain building.
_________________________
The Triassic evaporites of Sassalbo and Secchia Valley (Tuscan-
Emilian Apennines): geometric and kinematic data
(*) Dipartimento Scienze della Terra, Pisa, pertusati@dst.unipi.it
PIERO CARLO PERTUSATI (*), LIVIO BONINI (*) & CHIARA MONTOMOLI (*)
342

“Alpine” Corsica and Northern Apennine: two orogenic complexes
or the same? Arguments for discuss about
GIANFRANCO PRINCIPI (*) (**), VALERIO BORTOLOTTI (*), ENRICO PANDELI (*) (**), FRANCESCA GARFAGNOLI (*)
FRANCESCO MENNA (*) & GIUSEPPE NIRTA (*)
Key words: Alpine Corsica, geodynamics, northern Apennines,
regional geology.
Up to now, at least three main hypotheses have been advanced
in the geological literature to explain the geodynamic events
allowing to the present Northern Apennines orogenic chain.
These models agree with that concern the Oligo-Miocene
evolution, but are strongly different regarding the oldest orogenic
stages. In particular, the first model is based on a double orogen
(characterized by an older “alpine” and by a younger “apenninic”
defomation stages) and theorizes an inversion of the subduction
plane at the Oligocene boundary. The second model hypothesizes
that the present day “Apenninic” stage (with a west dipping
subduction) was active also during the older stage. Finally, the
third model, tacking into account the Oligocene age of the
Sardinia-Corsica offshore “arc-type” magmatism and of the
coheval inception of the Ligure-Balearic back-arc basin,
considers the old stage as effect of an important intraoceanic leftlateral
wrench movement until the Early Oligocene that predates
the “Apennine” stage development.
The occurrence of Late Cretaceous? to Tertiary subduction
events, accompanying the main stage of the Apennines
tectogenesis is well documented both along the Corsica-Northern
Apennines transect and in Calabria sector.
The major evidences are:
the presence of continental basement and ophiolitic roks
affected by HP-LT metamorphism (up to eclogite facies),
Cretaceous?-Eocene-Lower Oligocene in age, and of Oligocene
to Lower Miocene HP-LT and Green Schist metamorphism also
in the continental margin of Adria.
The presence of post Barthonian HP-LT parageneses on both
the Corsican European margin and the overlying Neogene
neoauthocthonous close to the contact with metamorphic
ophiolitic nappes (Schistes Lustrés auctt.).
The presence in the Late Cretaceous helminthoid Flysch of
the southern Tuscany (Monteverdi M.mo U.) of ophiolitic
_________________________
(*) Dipartimento di Scienze della Terra, Università di Firenze,
pandeli@geo.unifi.it
(**) IGG (Istituto di Geoscienze e Georisorse)-CNR - Firenze
343
olistostromes and olistolites.
The presence of a Late Paleocene-Early Eocene epiligurian
deposit (Lanciaia Fm.)covering unconformably the Vara Unit
and the underlying Monteverdi M.mo Unit.
The development of Eocene/Oligocene to Early Miocene
calc-alkaline volcanic alignment to the west of the Sardinia-
Corsica massif.
The contemporaneous westwards growth of the Ligure-
Balearic backarc basin.
Furthermore recent data about the ages of the arc-type
magmatism (38.3 Ma) and about the sismic thomography seem to
put new argument in favour of the second model. This latter is
also supported by the eastward migration of the Corsica-fed
siliciclastic turbiditic sedimentation and of the emplacement of
ophiolitic olistostromes and olistoliths towards east in the oceanic
realm since Cretaceous to Eocene. Moreover, Late Paleocene-
Early Eocene epiligurian sediments (i.e. Lanciaia Fm.) are
present in the Northern Apennines orogenic stack and predate
the development of the HP-LT metamorphism of the Schistes
Lustrés.
This speech aims to stimulate an open debate about to the socalled
Alps-Apennines boundary.
SESSIONE 10

SESSIONE 10
New stratigraphic constrains of the para-autocthonous Caporalino-
Sant’Angelo Unit belonging to the “Alpine Corsica” (Corte-Ponte
Leccia area, Corsica)
ALBERTO PUCCINELLI (*), ANTONIO CASCELLA (**) & NICOLA PERILLI (*)
Key words: Biostratigraphy, Calcareous nannofossils, Corsica,
Eocene, France, Lithostratigraphy.
ABSTRACT
This paper is aimed to give new insights useful to enlighten
the relationships between the Alpine Units (Alpine Corsica
Auctt.) outcropping in the NE sector of Corsica and hence helpful
to reconstruct the geodynamic history of this sector of the alpine
belt. In Corsica, the Alpine Units consists of a stack of
(frequently laminated) oceanic and continental units which
overlying the Variscan basement (Hercynian Corsica Auctt.) of
the Corso-European foreland. In some areas, the pile of the
Alpine Units is still a puzzle and both lithostratigraphy and age of
some units are still debatable. In the Omessa area, between Corte
and Ponte Leccia, the tectonic pile includes the Tenda Unit (cfr.
Tenda Massif Auctt.), the Caporalino-Sant’Angelo Unit, the
Santa Lucia Nappe and the Schistes lustrés s.l. Among these
units, the type of deposit and the age of the succession assigned
to the Caporalino-Sant’Angelo Unit is still matter of debate.
Earliest geologist consider the Caporalino-Sant’Angelo unit as a
continuous sedimentary succession which spans in age from
Lower Jurassic to Eocene. Later, some of these authors confirmed
the continuity of the sedimentation of the Lower Jurassic to
Eocene deposits assigned to the Caporalino-Sant’Angelo Unit
and interpret the Caporalino limestone as a shallow-water
platform deposit or a pelagic succession characterized by
carbonate platform input. In contrast with this interpretation, the
Caporalino-Sant’Angelo Unit was considered as coarse grained
deposits with huge olistoliths sedimented in a distinct Eocene
basin.
Aim of this paper is to improve the lithostratigraphy and the
biostratigraphy of the Caporalino-S.Angelo Unit in order to the
make clear the type of deposit and the age of this (Alpine) unit
and to suggest the palaeogeographic location of its sedimentary
_________________________
(*) Dipartimento di Scienze della Terra, Università degli Studi di Pisa,
perilli@dst.unipi.it
(**) Istituto Nazionale di Geofisica e Vulcanologia, Pisa,
cascella@pi.ingv.it
344
basin.
Based on a new geological mapping of the Corte-Pontee
Leccia area and the lithostratigraphy of the three key compositesections,
the Caporalino-Sant’Angelo Unit consists of three
coarse-grained clastic intervals and eight levels. The lower
interval is composed of breccias conglomerates and sandstones.
The middle interval mainly consists of breccias conglomerates
and olithosliths (e.g. Caporalino Limestone); in the upper part of
this interval are marls and breccias with clasts of Caporalino
Limestone. Fine-grained sandstones with pelitic intercalation and
rare conglomeratic beds characterize the upper interval.
According to the recovered microfossil (calcareous nannofossils
and foraminifera) assemblages the entire Caporalino-Sant’Angelo
Unit is Early to Middle Eocene in age.
Consequently, the previous model of a continuous Jurassic-
Eocene stratigraphic succession is no longer valid and the
following scenario could be outlined:
1) during the Early-Middle Eocene the Caporalino-S.Angelo
unit settled in an siliciclastic basin which received coarse grained
deposits such as breccias and conglomerates, olistostromes and
olistoliths (mainly composed by Upper Jurassic platform
limestones) and sandstones and intercalation of silty marls and
conglomerates,
2) the coarse-grained clastic sediments and the Upper Jurassic
calcareous olistoliths , could have an inner place of origin (they
probably represent the remnants of a carbonate platform
emplaced over the Corso basement);
3) consequently the Caporalino Sant’Angelo Unit was a
foredeep basin, situated between the outer margin represented by
the European foreland, and the inner margin, constituted yet by
the corso basement and its calcareous cover,
4) later the Santa Lucia Nappe and the Schistes lustrés were
thrusted on the Caporalino-S.Angelo basin.

Magma emplacement in a transfer zone: the Miocene mafic Orano
dyke swarm of Elba Island, Tuscany, Italy
Key words: Dyke swarm, Elba Island, transfer zone.
Dykes represent the common pathways of magmas ascending
through the crust and offer the potential to reconstruct stress
fields at the time of their intrusion because they directly record
the strain associated with emplacement. However, the
reconstruction of the paleostress can be biased by other factors,
such as the magma driving pressure as well as structure of the
crust and its rheological heterogeneities. In this respect, the study
of dyke swarms emplaced in a granitic host can mitigate this
overall complexity affecting paleostress reconstruction. Indeed,
because of the high degree of mechanical isotropy of the granitic
host, these dykes have the potential to provide more
straightforward information about the stress field active during
dyke emplacement than do dykes in layered sedimentary or
metamorphic host rocks.
The Late Miocene Monte Capanne pluton of Elba Island
(Tuscany, Italy) is crosscut by the late- to post-plutonic mafic
Orano dyke swarm, which provides information on the activity
within a regional transfer zone and its relationships with the
Miocene-Quaternary magmatism throughout the northern
Tyrrhenian region.
In particular, the magmatic activity in the western part of Elba
Island at the north end of the Tyrrhenian Sea, which lasted
approximately 1.5 Ma during the late Miocene, built an intrusive
complex of nested Christmas-tree laccoliths, a 10 km-diameter
pluton (Monte Capanne) and, finally, the steeply dipping Orano
dyke swarm. This igneous activity occurred in an extensional
regime at a magmatic centre in the wake of the eastwardmigrating
compression of the Apennine front. The Orano dyke
swarm consists of hybridized mantle-derived magmas,
constituting about 200 dykes totalling a length of approximately
90 km. These dykes intruded the north-western part of the pluton
and its contact aureole, as well as several kilometres of
sedimentary rock above. Dyke emplacement occurred near the
end of pluton crystallization, above a source region marked by a
_________________________
(*) Dipartimento di Scienze della Terra, Università di Pisa,
rocchi@dst.unipi.it
(**) Istituto di Geoscienze e Georisorse, CNR, Pisa
(°) Department of Geology, Norwich University, VT, USA
SERGIO ROCCHI (*), ANDREA DINI (**) & DAVID S. WESTERMAN (°)
345
positive magnetic anomaly located in the north-western part of
the pluton. Dyke orientations are dominated by a major system
trending N78E, associated with a minor system of dykes with
N38W and N22E trends.
The emplacement patterns of the Orano dykes preserve the
strain that resulted in exploitation of Riedel fractures in a NE–
SW dextral shear zone; local internal zones of sinistral shear
account for one set of the minor system. This shearing occurred
between offset segments of the Elba Ridge in the Western Elba
transfer zone, where strain concentrated magma flow to build the
western Elba magmatic complex. This zone developed as a result
of differential extension rates during the formation of the northtrending
Neogene–Quaternary sedimentary basins. Such basins
are connected regionally by NE-trending lineaments, along which
all the magmatic centres in the northern Tyrrhenian–Tuscan area
are distributed. The magmatic activity developed as a wave
moving northeastward across the region, suggesting that
magmatism was focused by transfer zone development, as backarc
extension migrated in that direction and reactivated older
faults.
SESSIONE 10

SESSIONE 10
The northern Tyrrhenian-northern Apennine system: constraints on
the geodynamic setting from a new reprocessing and interpretation
of seismic line M12A
FEDERICO SANI (*), FRANCESCO MAZZARINI (**), EUSEBIO M. STUCCHI (°),
ANDREA TOGNARELLI (°°) & GIOVANNI MUSUMECI (^)
Key words: Igneous bodies, late Neogene, tectonics northern
Tyrrhenian Sea-northern Apennines, upper crustal structures.
The central Mediterranean is one of the most interesting and
complex areas of the World. Its evolution has been tested through
classical geodynamic models, but because of its complexity, some
of them often fail and therefore the interpretation of this area is
still debated. In this context, the Tyrrhenian Sea and Apennine
chain represent key areas recording parts of the geological history
of the central Mediterranean region. The convergence between
Africa and Eurasia can be considered the first-order system in
which the following second-order elements are: (i) the advancing
Apennine front along the Padan-Adriatic margin, (ii) the
Calabrian Arc subduction system and (iii) back-arc basins at the
rear of the chain. The evolution in time and space of seismicity,
magmatic activity and the sedimentary record since the late
Miocene attests to the complexity of this dynamic context.
We present a new reprocessing of the CROP M12A seismic
line located in the northern Tyrrhenian Sea strikes NE-SW south
of Elba Island, extending from the Corsica basin to the west to
the Punta Ala basin to the east (Fig. 1). This line was acquired in
the framework of the Italian CROP project, which aims to
investigate the deep structure of the crust in Italy. Therefore,
researchers focused on data recorded at depth, paying little
attention to near-surface or shallow reflectors. In the present
study, seismic line M12A was reprocessed and reinterpreted in
_________________________
(*) Dipartimento Scienze della Terra, Firenze, fsani@geo.unifi.it
(**) Istituto Nazionale geofisica e vulcanologia Pisa, mazzarini@pi.ingv.it
(°) Dipartimento Scienze della Terra, Milano, eusebio.stucchi@unimi.it
(°°) Consorzio di Geofisica, Università di Pisa, antogna@gmail.com
(^) Dipartimento Scienze della Terra, Pisa, gm@dst.unipi.it
Lavoro eseguito nell’ambito del progetto PRIN2005 con il contributo
finanziario delle Università di Firenze, Pisa e Milano.
346
order to investigate the nature of tectonic structures in the upper
crust of the northern Tyrrhenian Sea and their relationships with
late Miocene magmatic bodies, some of which crop out on Elba
Island, north of the line (Fig. 1). This seismic line was chosen for
the following: (i) the possibility to investigate the structures of
the northern Tyrrhenian Sea from the Tuscan shelf to the inner
portion of northern Apennine; (ii) the availability of original data
in digital format in order to perform reprocessing; (iii) the
possibility to use geological data (Elba Island, Pianosa Island and
Martina 1 well) to constrain the interpretation of seismic line. On
the basis of the reprocessing results (Fig. 2), a new interpretation
of seismic line M12A is presented. Reprocessed seismic data
reveal: (i) the absence of low angle eastward-dipping normal
faults, (ii) the occurrence of Late Miocene-middle Pliocene
eastward thrusting throughout the line and (iii) the occurrence of
intrusive bodies emplaced at the core of thrust-anticlines. These
new observations suggest a late Miocene-early Pliocene
compressive setting for the northern Tyrrhenian Sea-northern
Apennine system, in marked contrast with the extensional setting
of the southern Tyrrhenian Sea. On these bases we highlights the
geological complexity of the central Mediterranean and the
different behavior of the Apennine lithosphere in the northern and
southern regions of the Tyrrhenian Sea.

Fig. 1- Geological sketch of the Appenines chain and Tyrrhenian Sea; b) Geological sketch map of northern Tyrrhenian Sea – northern Apennines with location of
CROP M12A seismic line. 1: Punta Ala basin; 2: Calamita ridge; 3: Montecristo basin; 4: Pianosa ridge; 5: Corsica basin; MTR: Mid Tuscan ridge; LGF: Larderello
geothermal field.
Fig. 2 – Final stack version of the reprocessed seismic line CROPM12A.
347
SESSIONE 10

SESSIONE 10
Inversion tectonic in the Umbria-Marche region (Apennines, Italy):
Preliminary results from a new paleomagnetic approach
SARA SATOLLI (*), SIMONE AGOSTINI (*), ANTONIO TURTÙ (*) & FERNANDO CALAMITA (*)
Key words: Apennines, inversion tectonic, paleomagnetism,
structural geology.
INTRODUCTION
The Umbria–Marche region belongs to the NE-verging Northern
Apennines fold-and-thrust belt, developed since Oligocene times
in response to the convergence between the African and the Euro-
Asian plates. Compressive deformation affected the Triassic-
Cenozoic sedimentary successions of the Adria paleomargin.
The Apennine belt has been strongly influenced during its
formation by the Mesozoic paleomargin architecture. During the
Neogene orogenesis, positive inversion affected pre-thrusting
normal faults, which were either truncated by thrusts propagating
with a shortcut trajectory, generating footwall shortcut and
related anticlines, or reactivated with reverse kinematics,
depending on their orientation with respect to the new
compressive regime (CALAMITA et alii, 2009).
We propose paleomagnetism integrated to structural analysis
as an innovative tool to discriminate the presence of inverted
structures.
PALEOMAGNETIC AND STRUCTURAL ANALYSIS
We performed a paleomagnetic study in the southern sector of
the Umbria-Marche carbonate mountain ridge, constituted by a
series of NE-verging folds with gentle backlimbs and vertical to
slightly overturned forelimbs. We sampled 21 sites between
Colfiorito and Camerino cities in Diaspri, Maiolica, Marne a
Fucoidi and Scaglia Formations, collecting on average 14
cylindrical samples from each site.
Cores were drilled during winter 2009/2010 using a petrolpowered
portable drill and oriented in-situ with a magnetic
compass. We corrected the orientation to take into account the
magnetic declination in the analyzed area (+2°).
_________________________
(*) Dipartimento di Scienze, Università G. d’Annunzio di Chieti e Pescara,
Chieti Scalo, s.satolli@unich.it
348
The cores were cut into standard cylindrical samples and
analysed in the magnetically shielded room of the paleomagnetic
laboratory at the Istituto Nazionale di Geofisica e Vulcanologia
of Rome. All samples were stepwise demagnetised by thermal
heating in 14 steps (up to 620°C). For each step, the natural
remanent magnetization was measured with a 2G DC-SQUID
cryogenic magnetometer.
The primary component of magnetization was well defined for
246 over the 297 measured samples. Mean directions were
computed sing either FISHER's (1953) statistics or the MCFADDEN
&MCELHINNY (1988) method.
Different structural data were collected to analyse the local
trend of the main structures and to compare them with the
paleomagnetic records. Meso-structural trend was determined by
measuring:
- minor folds hinges (widespread in the Scaglia Bianca,
Scaglia Rossa and Maiolica Formations);
- cleavage-bedding lineations (L1-0);
- vertical and sub-vertical bedding planes;
- joint sets (only if well expressed).
DISCUSSION
Both in-situ and tilt-corrected paleomagnetic directions are
far from the geocentric axial dipole field direction, suggesting the
absence of pre-folding magnetic overprints.
All the sites, collected both in the N-S and NW-SE structures,
show similar paleodeclinations (Fig. 1). Site MC11, collected in
the Diaspri Formation was rejected from further considerations,
as almost no samples yield a stable magnetic signal.
The structural analysis of the first nine sites has showed the
following trends:
- NW-SE at the MC01, MC05 and MC09 site;
- NNW-SSE at the MC02, MC03, MC04, MC07, MC08 sites;
- N-S at the MC06 site;
From preliminary paleomagnetic and surface geological data,
the structural setting of the study area appears to be influenced by
the inherited Adria paleomargin physiography and by the
subsequent positive inversion of pre-existing extensional faults
occurred during the Neogene deformation.

Fig. 1 – Structural map of the study area with declination of the
paleomagnetic sites.
349
REFERENCES
CALAMITA F., ESESTIME P., PALTRINIERI W., SCISCIANI V. &
TAVARNELLI E. (2009) – Structural inheritance of pre- and
syn- orogenic normal faults on the arcuate geometry of
Pliocene-Quaternary thrusts: examples from the Central and
Southern Apennine Chain. Ital. J. Geosci. (Boll. Soc. Geol.
It.), 128/2, 381-394.
FISHER, R. A. (1953) – Dispersion on a sphere. Proc. R. Soc.
London Ser. A, 217, 295-305.
MCFADDEN, P.L.,&M.W.MCELHINNY (1988) – The combined
analysis of remagnetization circles and direct observations in
palaeomagnetism. Earth Planet. Sci. Lett., 87, 161-172,
doi:10.1016/0012-821X(88)90072-6.
SESSIONE 10

SESSIONE 10
The Neogene positive inversion of late Paleozoic-Triassic basins in the
structural evolution of the Umbria-Marche carbonate mountain ridge
(northern Apennines)
VITTORIO SCISCIANI (*), SIMONE AGOSTINI (**), FERNANDO CALAMITA (**), ANDREA CILLI (°), ITALIANO GIORI (°),
PAOLO PACE (**) & WERTER PALTRINIERI (**)
Key words: Foreland fold-and-thrust belt, inversion tectonics,
late Paleozoic-Triassic basins, Northern Apennines
The integrated analysis of geological and geophysical data
allowed us to define the structural setting of the Umbria-Marche
carbonate mountain ridge and to construct a crustal geological
cross-section from the Umbria Valley to the northern portion of
the Laga basin.
The Umbria-Marche carbonate mountain ridge corresponds to
a structural culmination of the outer Northern Apennines foldand-thrust
belt. In this mountain ridge the exposed succession is
represented by early Jurassic shelf carbonates (Calcare Massiccio
Fm.) and middle Jurassic to early Tertiary pelagic carbonates
with marls and cherts (Umbria-Marche pelagic succession).
Siliciclastic foredeep deposits (i.e., the Marnoso Arenacea Fm.,
the Arenarie di Camerino Fm. and the Laga Fm.) directly overlay
the previous units and show a younger age towards the east
(BOCCALETTI et alii, 1990).
The subsurface stratigraphy has been reconstructed by few
exploration wells that encountered a variable thickness of
evaporites of at least 2000 m (Anidriti di Burano Fm.), overlying
slightly metamorphosed sediments (mainly phyllites) of
undefined age and referred to the Verrucano Fm. (MARTINIS &
PIERI, 1963; ANELLI et alii, 1994).
The structural setting of the region reflects the
superimposition of three distinct tectonic events: (i) an
extensional phase, from late Paleozoic-late Triassic and
culminated during Middle Jurassic (ALDINUCCI et alii, 2008 and
references therein); (ii) a late Miocene-early Pliocene
compressional phase during the Apenninic orogeny, expressed in
this area by NNW-SSE and NE-SW trending folds and thrusts
_________________________
(*) Dipartimento di Geotecnologie per l'Ambiente ed il Territorio – Università
“G. d’Annunzio” di Chieti-Pescara, scisciani@unich.it
(**) Dipartimento di Scienze – Università “G. d’Annunzio” di Chieti-Pescara
(°) Eni Exploration & Production Division, San Donato Milanese.
Lavoro eseguito nell’ambito del progetto MIUR-Prin 2008 (F. Calamita) e con
il contributo finanziario ex 60% (F. Calamita – V. Scisciani)
350
(CALAMITA & DEIANA, 1988); (iii) and a late Pliocene-
Quaternary extensional event with NW-SE normal faults
responsible for the development of intramountain basins and for
the present-day seismicity (BONCIO & LAVECCHIA, 2000;
CALAMITA et alii, 2000; PIZZI et alii, 2002).
Detailed field structural surveys along the outcropping thrust
faults has been carried out in order to define the faults kinematic,
to constrain geological cross-sections, to reconstruct cut-off lines
and to estimate the amount of shortening. The structural data
collected in the field indicate ramp relationships for the thrust
faults both for hanging-wall and footwall blocks.
Seismic reflection profiles interpretation, tied to surface
geology, led us to construct a crustal geological cross-section
along the studied area and to define the main structural features.
Moreover, the resulting cross-section, with special regards to
basement location, has been tested by a gravity-magnetic
modelling performed in collaboration with the ENI - Exploration
& Production Division.
The depth of the metamorphic basement below the Umbria-
Marche carbonate mountain ridge, in agreement with the seismic
line interpretation (i.e., MIRABELLA et alii, 2008), with respect to
the strong structural elevation of the top-carbonate succession
and the reduced amount of shortening, is compatible with the
positive inversion and the resulting extrusion of a buried late
Paleozoic-Triassic extensional basin. The basin infill exceeds
4000 m in thickness underneath the mountain ridge.
In conclusion, the crustal structural setting of the study area
appears to be influenced by the inherited Adria paleomargin
physiography and by the subsequent positive inversion with
reactivation of pre-existing extensional faults occurred during the
Neogene collisional deformation of the Northern Apennines.
REFERENCES
ALDINUCCI M., GANDIN A. & SANDRELLI F. (2008) - The
Mesozoic continental rifting in the Mediterranean area:
insights from the Verrucano tectonofacies of southern
Tuscany (Northern Apennines, Italy). Int. J. Earth Sci. (Geol.
Rundsch.), 97, 1247–1269.

ANELLI, L.GORZA M., PIERI M. & RIVA M. (1994) - Subsurface
well data in the Northern Apennines (Italy). Mem. Soc. Geol.
It., 48, 461-471.
BOCCALETTI M., CALAMITA F., DEIANA G., GELATI R., MASSARI
F., MORATTI G. & RICCI LUCCHI F. (1990) - Migrating
foredeep-thrust belt system in the northern Apennines and
southern Alps. Paleogeography-Paleoclimatology-
Paleoecology, 77, 3-14.
BONCIO P. & LAVECCHIA G. (2000) - A structural model for
active extension in central Italy. J. Geodyn., 29 (3-5), 233-
244.
CALAMITA F., COLTORTI M., PICCINI D., PIERANTONI P. P., PIZZI
A., RIPEPE M., SCISCIANI V. & TURCO E. (2000) - Quaternary
faults and seismicity in the Umbro-Marchean Apennines
(Central Italy): evidence from the 1997 Colfiorito
earthquake. J. Geodyn.,, 29, 245-264.
CALAMITA F. & DEIANA G. (1988) - The arcuate shape of the
Umbria-Marche Apennines (Central Italy). Tectonophysics,
146, 138-147.
MIRABELLA F., BARCHI M., LUPATELLI A., STUCCHI E. & CIACCIO
M. G. (2008) - Insights on the seismogenic layer thickness
from the upper crust structure of the Umbria-Marche
Apennines (Central Italy). Tectonics, 27, TC1010,
doi:10.1029/2007TC002134.
MARTINIS B. & PIERI M. (1964) - Alcune notizie sulla formazione
evaporitica del Triassico Superiore nell'Italia centrale e
meridionale. Mem. Soc. Geol. It., 4(1), 649-678.
PIZZI A., CALAMITA F., COLTORTI M. & PIERUCCINI P. (2002) -
Quaternary normal faults, intramontane basins and sismicity
in the Umbria-Marche-Abruzzi Apennine Ridge (Italy):
contribution of neotectonic analysis to seismic hazard
assessment. Boll. Soc. Geol. It ., Vol. sp. 1, 923-929.
351
SESSIONE 10

SESSIONE 10
___________________
Magnetic anomalies and deep Apennine setting: towards a lower
crustal perspective?
Key words: Basement, lower crust, magnetic anomalies,
magnetic basement, tectonics, thick-skinned tectonics, thinskinned.
INTRODUCTION: MAGNETIC ANOMALIES AND
CRUSTAL SETTING
Magnetic anomaly maps are important tools for unravelling
the deep structure of the crust. Igneous rocks and, to a lesser
extent, metamorphic rocks colder than 600°C are often
characterized by high magnetic susceptibilities and produce
potentially detectable magnetic anomalies. Rocks hotter than
600°C do not produce significant anomalies because magnetite,
which is the most common and most susceptible ferromagnetic
mineral in the crust, becomes paramagnetic above 600°C (at
depth) and its susceptibility drastically decreases. Therefore,
magnetic anomalies can give significant insights on the crustal
structure between the top surface of the magnetic rocks and the
depth of the 600°C isotherm (likely 20-30 km in regions of
normal geothermal gradient). This part of the crust is often poorly
understood as it is not penetrated by drill-holes and is sparsely
and often poorly imaged by seismic reflection data.
THE AGIP (1981) AEROMAGNETIC MAP AND ITS
INFLUENCE OF EARLY TECTONIC MODELS OF THE
APENNINES
Along peninsular Italy, the Apennine belt and adjacent
Adriatic-Apulian foreland consist of a 5-10 km thick Triassic-
Pleistocene sedimentary succession (diamagnetic or lowsusceptibility)
on top of possibly magnetic Triassic to
Carboniferous shales (the so-called “Verrucano”) and poorly
known higher-grade metamorphic rocks. Therefore magnetic
anomaly data were thought to be sensitive to the depth and
geometry of the magnetic basement (or basement), i. e. the crustal
section comprised between the top (or bottom?) of Verrucano
shales and the depth of the 600°C metamorphic rocks.
The first magnetic anomaly map of Italy was issued by AGIP
(*) Istituto Nazionale di Geofisica e Vulcanologia, Roma
fabio.speranza@ingv.it
FABIO SPERANZA (*) & MASSIMO CHIAPPINI (*)
352
(1981) by measuring the magnetic field over Italy at an average
altitude of about 3000 m using a cesium magnetometer. This map
showed a residual field gradually increasing southeastward, with
negative values on the Po Plain and strongly positive values over
the Ionian Sea. Because the isoanomaly lines were almost
orthogonal to the main Apenninic compressive fronts, the
magnetic residual anomalies were considered a key piece of
evidence for the interpretation of the external Apennines as a
“thin-skinned” orogen (BALLY et alii, 1986; MOSTARDINI &
MERLINI, 1986). According to this interpretation, the external
Apennine thrust sheets are Meso-Cenozoic carbonates detached
from an undisturbed magnetic basement along Triassic evaporite
horizons. The magnetic basement is then a southwest dipping
regional monocline, gradually plunging beneath the chain, and
located at 10-15 km depth in the axial northern Apennines.
Because in the northern Apennines the sedimentary cover is 5-6
km thick, the tectonic stacking of two or more sedimentary slices
was needed to “fill the gap” between the surface and the deep and
undeformed basement. The Apennines were thus considered to
have undergone very large (in the order of hundreds of km)
shortening (BALLY et alii, 1986), raising the question of what
happened to hundreds of km of (subducted?) continental
basement.
THE CHIAPPINI ET ALII (2000) MAGNETIC MAP AND
SUBSEQUENT INTERPRETATIONS
CHIAPPINI et alii (2000) obtained a new residual magnetic
map of the Apennine belt-Adriatic/Apulian foreland by
integrating pre-existing ground and offshore data sets. Negative
anomalies were documented over the Adriatic-Apulian foreland
areas, whereas the external Apennine belt was characterized by a
ubiquitous low-amplitude (< 30 nT), long-wavelength positive
anomaly. In the central-northern Apennines, three ~ 100 km wide
more intense (100-200 nT) round-shaped anomalies are
superimposed to the long-wavelength feature. Finally, in the
Tyrrhenian Sea and margins, high-intensity, short-wavelength
positive-negative couplets coincide with magmatic outcrops or
bodies at shallow depth. SPERANZA & CHIAPPINI (2002)
suggested that the low-amplitude anomaly pattern over Italy
indicated that the magnetic basement beneath the Triassic
evaporites was ubiquitously incorporated in the external belt
compressive fronts, implying a thick-skinned tectonic style for the
external Apennines. They also presented magnetic models along

two NE-SW transects orthogonal to the northern (along the
CROP-03 profile) and southern Apennines. They suggested that
in the northern Apennines the basement rises southwestward
along the thrust fronts from 6-7 km depth in the Adriatic foreland
to 2-3 km depth in the axial belt, where some exploration wells
have penetrated basement. SPERANZA &CHIAPPINI (2002) also
observed that in the southern Apennines, a remarkable positive
magnetic anomaly is parallel with and tens of kilometers
southwest of the belt front. Therefore, they argued that the
observed magnetic anomaly is produced by strongly magnetic
basement beneath the belt, likely an internal crustal wedge
tectonically interposed between the Apulian carbonate sequences
and basement.
RECONCILING AEROMAGNETIC AND GROUND
LEVEL DATA SETS
CARATORI TONTINI et alii (2004) have recently re-processed
the AGIP (1981) data set, by using a more appropriate reference
magnetic field. They evidenced a magnetic anomaly pattern along
the Apennines belt completely similar to the one apparent in the
CHIAPPINI et alii (2000) map. In particular, a positive magnetic
anomaly belt few tens of nT in intensity, runs along the external
Apennine belt, while both the internal belt and the foreland are
mainly characterized by negative magnetic residuals.
MAGNETIC RESIDUALS AND MOUNTAIN BELTS:
TOWARDS A LOWER CRUSTAL PERSPECTIVE?
Besides a first-order agreement, the aeromagnetic and ground
level data sets can yield complementary information about the
crustal Apennine setting. Ground data by CHIAPPINI et alii (2000)
undoubtedly testify the existence of medium susceptibility value
rocks (~10 -3 SI, possibly corresponding to crystalline basement)
in the upper crust of the external northern Apennines. Conversely,
re-processed aeromagnetic data from AGIP (1981), being more
distant from the source, are more sensitive to deeper, yet more
strongly magnetic, rocks. The magnetic analysis of lower crustal
rocks exposed in the Ivrea-Verbano body has shown that
serpentinites and other similar lower crustal lithologies may
pretend to the title “most strongly magnetic rocks available on
Earth”, yielding magnetic susceptibility values even exceeding
10 -1 SI (ROCHETTE, 1994).
As a consequence, the positive anomalies along the external
Apennines apparent in the revisited AGIP (1981) map, probably
testify the magnetic contribution of the Adriatic foreland lower
crust. Along the northern Apennines, this fingerprint vanishes
moving towards the belt interior. This is consistent with recent
seismological data (CHIARABBA et alii, 2009), showing that the
Adriatic lower crust is subducted along with underlying mantle
beneath the northern Apennines, while the uppermost 20 km of
the Adriatic crust are incorporated in the Apennine orogenic
353
wedge.
We conclude that magnetic anomalies, classically considered
as key datum to constrain the depth of crystalline rocks within a
mountain belt, may be more sensitive to understand deeper
setting of the chain, at lower crustal (i.e. at 20-30 km) depths.
There is increasing evidence, in fact, that in some cases the
magnetization of crystalline rocks and sediments may compare,
and be 2-3 orders of magnitude lower than that of a mafic lower
crust. Thus the concept of “magnetic basement”, as well as the
main bearings of magnetic residuals on the deep tectonic setting
of mountain belts, need to be revised.
REFERENCES
AGIP SpA. (1981) - Italia, Carta Magnetica - Anomalie del
Campo magnetico residuo, scale 1:500,000, S. Donato
Milanese (Italy).
BALLY A. W., BURBI L., COOPER C. & GHELARDONI R. (1986) -
Balanced sections and seismic reflection profiles across the
central Apennines. Mem. Soc. Geol. It., 35, 257-310.
CARATORI TONTINI F., STEFANELLI P., GIORI I., FAGGIONI O. &
CARMISCIANO C. (2004) – The revised aeromagnetic anomaly
map of Italy. Ann. Geophys., 47 (5), 1547-1555.
CHIAPPINI M., MELONI A., BOSCHI E., FAGGIONI O., BEVERINI N.,
CARMISCIANO C. & MARSON I. (2000) - Onshore- offshore
integrated shaded relief magnetic anomaly map at sea level
of Italy and surrounding areas, scale 1:1,500,000. In: Annali
di Geofisica, 43 (5), Plate 1.
CHIARABBA C., DE GORI P. & SPERANZA F. (2009) - Deep
geometry and rheology of an orogenic wedge developing
above a continental subduction zone: Seismological evidence
from the northern-central Apennines (Italy). Lithosphere, 1
(2), 95-104, doi:10.1130/L34.1.
MOSTARDINI F. & MERLINI S. (1986) - Appennino centro
meridionale, sezioni geologiche e proposta di modello
strutturale. Mem. Soc. Geol. It., 35, 177-202.
ROCHETTE P. (1994) – Comments on “Anisotropic magnetic
susceptibility in the continental lower crust and its
implication for the shape of magnetic anomalies” by G.
Florio et al.. Geophys. Res. Lett., 21 (24), 2773-2774.
SPERANZA F. & CHIAPPINI M. (2002) - Thick-skinned tectonics in
the external Apennines, Italy: New evidence from magnetic
anomaly analysis. Journal of Geophysical Research, 107,
2290, doi: 10.1029/2000JB000027.
SESSIONE 10

SESSIONE 10
Oblique-slip fault growth by segment linkage: a case from
Basilicata, southern Italy
ENRICO TAVARNELLI (*), VALERIA PASQUI (*), FRANCESCO BUCCI (*), ROCCO NOVELLINO (*) & GIACOMO PROSSER (**)
Key words: Transtension, oblique-slip fault propagation,
Potenza Basin, Agri Valley, Southern Apennines.
INTRODUCTION
Faults and fractures are the dominant modes by which the
upper brittle crust accommodates deformation, and an extensive
documentation of their geometrical and kinematic features is
critical for a better understanding of how these structures
enucleate and evolve through time. The map distribution and
cross-sectional profile of macroscopic normal faults suggest
that these structures enucleate as smaller isolated segments, and
that individual segments are linked to produce larger faults as
their tips propagate laterally and down-dip. By contrast,
documentation of these relationships in outcrop-scale examples
is relatively less abundant, and mesoscopic information on the
modes of linkage of isolated fault segments is quite rare: yet,
minor structures are often well exposed, thus allowing for a
detailed determination of the processes responsible for their
development. In this study we document a situation from the
Potenza Basin (Southern Apennines, Italy) where a mesoscopic
transtensional fault array grew by linkage of smaller isolated
fault segments. Observations of the zones of fault segment
overlap provide the basis for a kinematic deformation model of
stepped ramp-flat fault surface development. Because of the
need of investigating at the early stages of faulting, we
restricted our analysis to very small structures, where the
overprinting relationships among minor fabrics are particularly
clear. The present investigation represents the methodological
continuation of two earlier contributions (Tavarnelli & Pasqui,
1998, 2000), and aims at comparing the results from fault
analysis in the Potenza Basin with those recently obtained for
the high Agri Valley (BUCCI, 2009).
_________________________
(*) Dipartimento di Scienze della Terra, Università di Siena
(**) Dipartimento di Scienze Geologiche, Università della
Basilicata, Potenza
354
GEOLOGICAL SETTING
The Southern Apennines are an arcuate fold-and-thrust belt
developed due to imbrication of tectonic units which were
originated in different palaeogeographic domains characterised
by mainly carbonatic deposition (Tavarnelli & Prosser, 2003).
These domains, differentiated since Triassic time and for the
subsequent Mesozoic-Tertiary interval, are from West to East:
i) the Campania-Lucania platform; ii) the Lagonegro Basin, and
iii) the Apulia platform. Stacking of the tectonic pile began in
late Oligocene time in the westernmost provinces and
progressively migrated eastwards until recent. Thrusting was
accompanied by clastic deposition which was abundant in the
foredeep domains between the evolving Apennine chain and the
Apulian foreland, and in restricted piggy-back basins located
on top of moving thrust sheets. The Potenza Basin, to the West
of the present-day Apennine chain-Apulia foreland boundary,
developed as a piggy-back basin passively carried on top of
deformed sediments mainly belonging to the Lagonegro Units.
The local stratigraphic sequence consists of two distinct cycles:
the Altavilla Fm. of Early Pliocene age, which is
unconformably overlain by the Ariano Fm. of Middle Pliocene
age.
Since Middle Tortonian time, the Apennine belt was
affected by eastward-migrating extension which caused the
opening of the Tyrrhenian Sea, while compression was still
going on in the outermost provinces. Compressional and
extensional deformations were locally separated by left-lateral
strike-slip tectonics, which were important in the Pollino and in
the Cilento areas, South and West of the Potenza Basin,
respectively. Quaternary transtensional deformations related to
the strike-slip regime could have affected and partly controlled
the recent evolution of pre-existing Pliocene depressions.
Moreover, map-scale transtensional faults were also recognised
in the Potenza Basin. The field examples from which we derive
a kinematic model for fault growth provide additional,
independent mesoscopic evidence for Pleistocene-to-Recent
transtensional tectonics in the Potenza Basin.
TRANSTENSIONAL DEFORMATIONS IN THE
POTENZA BASIN
At Bucaletto, in the eastern edge of the Potenza Basin, the
Middle Pliocene Ariano Fm. consists of gently WSW-dipping

alternating sandstones and siltstones. The sandstone beds have
an average thickness of 30 cm, are laterally very persistent over
1 km long horizontal distances, and are separated by siltstone
layers whose thickness ranges from 30 to 70 cm. These rocks
retain internal dishomogeneities related to a different degree of
induration: sandstone beds appear well lithified, whereas the
siltstone layers are poorly consolidated.
Using the criteria outlined by, we performed a detailed
investigation along five well exposed cliffs whose trends range
from N 47° E to N 170° E. Here, the Ariano Fm. is locally
affected by an array of mesoscopic extensional faults which
produce little vertical displacements never exceeding 2 m;
however, most commonly observed displacements range
between 2 and 10 cm. These faults mean strike N 171° E, and
mean dip 60°-80° towards both the WSW and the ENE. Rare
exposures of the fault surfaces off the cliffs show mechanical
striations and slickensides which reveal an oblique component
of movement. The fault striae mean plunge 28° towards N 346°
E, thus permitting to kinematically define these structures as
right-lateral transtensional faults.
Several faults exhibit variations in displacement, both
along-strike and down-dip. Although many faults propagate
through the whole exposed stratigraphic section, some faults
only offset a limited number of sandstone-siltstone layer pairs.
These structures are observed to gradually lose displacement
and to terminate at structurally complex tip points to be
described below.
Most observed faults are grouped and arranged in broad
deformation zones up to 3 m thick, whereas more rarely some
faults also occur as isolated structures, in which case their
thickness never exceeds 10 cm. A plot of maximum fault
displacement versus fault zone width, which was constructed
using mesoscopic structures of different magnitudes, reveals a
surprisingly regular trend. This indicates that the deformation
zones progressively broaden with increasing slip along the fault
surfaces. The local occurrence of calcite mineralizations along
the fault surfaces renders the hypothesis of deformation zone
broadening by fluid induced strain-hardening mechanisms
plausible.
The morphology of isolated faults is relatively simple: many
fault surfaces are localised (1-3 cm thick), sharp and planar in
the sandstone beds, and become diffuse (up to 5 cm thick),
wavy and irregular in the siltstone layers. This geometrical
variability reflects a different mechanical behaviour, which is
probably related to the different degree of lithification of the
deformed sediments during faulting. By contrast, the
morphology of the grouped faults is much more complex.
These structures generally consist of a 1-3 m thick deformation
zone, bounded by two sub-parallel, steeply dipping fault
surfaces. Bedding outside the fault zone is sub-horizontal. In
the vicinities of the fault zone the sandstone beds are bent
consistently with the shearing sense inferred from slickensides
on the fault surfaces. The fault zone consists of an array of
anastomosing shearing surfaces which produce offsets ranging
from 1 to 10 cm. The whole structure produces a total
displacement of about 2 m.
355
FAULT GROWTH BY SEGMENT LINKAGE: A
KINEMATIC MODEL
Observations of transtensional faults and related minor
fabrics, and the overprinting relationships among the latter,
provide a key for unravelling the history of fault development
at Bucaletto. Based on minor structures and their overprinting
relationships, we propose a kinematic model for transtensional
fault propagation. Initially fault slip is accommodated by
localised and isolated fault segments, whose tips produce a
damage zone of diffuse deformation. The faults lengthen by tip
migration across the damage zone, the fault surfaces overlap,
and development of P shear surfaces across the deformation
zone allows for displacement transfer between the two formerly
isolated fault segments. Kinematic linkage of the two formerly
isolated fault segment is then enhanced by development of R
shear surfaces which truncate all pre-existing fabrics. The final
geometry is that of a consistent, larger fault structure.
REFERENCES
BUCCI F. (2009) – Growth and dissection of a collisional
chain: tectonic evolution of the southern Apennines within
the high Agri Valley (Basilicata, Italy) deformation record.
PhD thesis, University of Siena, November 2009, pp. 1-213.
TAVARNELLI E. & PASQUI V. (1998) – Transtensional fault
growth by isolated segment linkage: an example from the
Potenza Basin, southern Apennines, Italy. Boll. della Soc.
Geol. Ital., 117, 261-269.
TAVARNELLI E. & PASQUI V. (2000) – Fault growth by segment
linkage in seismically active settings: examples from the
southern Apennines, Italy, and the Coast Ranges,
California. Journ. of Geodyn., 29, 501-516.
TAVARNELLI E. & PROSSER G. (2003) – The complete
Apennines orogenic cycle preserved in a transient single
outcrop near San Fele, Lucania, Southern Italy. Jour. of the
Geol. Soc. of London, 160, 429-434.
SESSIONE 10

SESSIONE 10
_______________________
(*) Dipartimento di Scienze della Terra, Università di Chieti – Pescara
Preliminary paleomagnetic analysis along the
Olevano-Antrodoco fault zone
ANTONIO TURTÙ (*), SARA SATOLLI (*), FERNANDO CALAMITA (*) & FABIO SPERANZA (**)
Key words: Fault zone, Olevano-Antrodoco, paleomagnetism,
tectonic rotations.
GEOLOGICAL AND PALEOMAGNETIC BACKGROUND
The Apennines are a fold-and-thrust belt formed during
Neogene-Quaternary as a consequence of the convergence
between Africa and Europe. The orogenesis affected Triassic to
Miocene sedimentary successions belonging to basin and
platform paleogeographic domains of the Adria Mesozoic
paleomargin (e.g., BEN AVRAHAM et alii, 1990). Two major arcs
can be distinguished: the northern Apennines Arc and the
southern Apennines-Calabrian Arc, with NE and SE convexity,
respectively. The two major arcs join in the Latium-Abruzzi
region (Central Apennines), bounded by two main approximately
N-S structural features: the Olevano-Antrodoco line (PAROTTO &
PRATURLON, 1975) and the Sangro-Volturno line (GHISETTI &
VEZZANI, 1983). Along the NNE-SSW Olevano-Antrodoco line,
Triassic-Miocene pelagic successions thrust over Messinian
siliciclastic foredeep and the Latium-Abruzzi carbonate platform
southward. This transversal structural feature had an important
paleogeographic role during Lower Jurassic, as it separed the
Latium-Abruzzi carbonate platform and the Umbria-Marche
pelagic domain. Such lineament was reactivated during the
Neogene orogenesis with kinematic considered as transcurrent
(CASTELLARIN et alii, 1978), transpressive (LAVECCHIA, 1985) or
linked to a lithospheric oblique thrust ramp (e.g., SATOLLI &
CALAMITA, 2008).
The Apennines experienced widespread differential vertical
axes rotations in the Middle Miocene-Pliocene time interval,
which have been explained with different models. Data collected
in Mesozoic and Miocene-Lower Pliocene sediments show
(**) Istituto Nazionale di Geofisica e Vulcanologia, fabio.speranza@ingv.it
356
varying amounts of rotation, due to both thrusts and strike-slip
fault activity. Available data from the northern Apennines
document a change in paleomagnetic rotations from
counterclockwise (CCW) to clockwise (CW) moving southward,
while the Sibillini thrust front is characterized by CW rotation in
the central sector (SPERANZA et alii, 1997). In the central
Apennines rotations of different magnitudes and signs have been
documented (SATOLLI et alii, 2005; MATTEI et alii, 1995;
SAGNOTTI et alii, 2000).
PALEOMAGNETIC ANALYSIS
Paleomagnetism, combined with structural geology, is a
powerful tool in understanding the kinematics of curved orogens
of controversial origin. We performed a detailed paleomagnetic
study along the Olevano-Antrodoco line, in order to constrain its
kinematic evolution. We sampled 38 sites in Lower Jurassic to
Miocene rocks, predominantly pelagic (or slope-to-basin)
limestones, collecting on average 13 cylindrical core samples
from each site (11 to 17 oriented cores for each site). Cores were
drilled using a petrol-powered portable drill and oriented in-situ
with a magnetic compass. The magnetic orientations of the cores
were corrected to take into account the magnetic declination at
the Olevano-Antrodoco area during winter 2010 (+2°).
All the samples were cut into standard cylindrical samples and
analysed in the magnetically shielded room of the paleomagnetic
laboratory at the INGV of Rome. All samples were stepwise
demagnetised by thermal heating in 15 steps (up to 620°C). For
each step, we measured the natural remanent magnetization of
samples by a 2G DC-SQUID cryogenic magnetometer.
The samples display two or three magnetization components.
Most samples are characterized by the presence of a low blocking
temperature component of normal polarity, removed before 180
°C, lying close to the geocentric axial dipole field direction
expected at the coordinates of sampled sections. An intermediate
temperature component with a reversed polarity was isolated in a
temperature range comprised between 220°C and 320°C
(maximum 460°C). Normal polarity characteristic magnetization
components (ChRMs) and great circles of remagnetization
(projection of the plane containing different components of
magnetization) were defined for 419 samples over the 509
thermal demagnetized samples. Mean directions were computed
using either FISHER's (1953) statistics or the MCFADDEN &
MCELHINNY (1988) method. Three sites were rejected because
characterised by α95 > 30°, while further two sites (sampled in the

weakly magnetized Maiolica Formation) were included in the
dataset even if characterized by high α95 values, as their
declinations agree with the other sites.
Anisotropy of magnetic susceptibility (AMS) was measured for
all sites with a MFK-1 bridge in order to define the magnetic
fabric acquired during diagenesis or during successive tectonic
defotmation. However, only 5 sites show a well-defined magnetic
lineation, given by the alignment of the maximum axis k1.
DISCUSSION
Both the in-situ and tilt-corrected paleomagnetic directions are
far from the geocentric axial dipole field direction, suggesting the
absence of pre-folding magnetic overprints. Furthermore, the
intermediate temperature component is antipodal to the primary
component in most of the Scaglia samples, suggesting growing of
hematite during diagenesis (according to CHANNELL et alii,
1982), thus a virtually primary nature of the characteristic
component. As a summary, a primary nature for the ChRM
isolated in each site may be reasonably inferred.
The tilt-corrected directions were compared to the coeval
directions expected for the Adriatic-African foreland, in order to
calculate the rotations due to the Apenninic tectonics. As Adria is
considered to have mirrored the African drift, we used reference
African paleopoles from BESSE &COURTILLOT (2002) for the
Jurassic to Pliocene sites.
The preliminary paleomagnetic data collected along the
Olevano-Antrodoco line evidence that the hangingwall of the
thrust is CW rotated with respect to its footwall.
REFERENCES
BEN AVRAHAM Z., BOCCALETTI M., CELLO G., GRASSO M.,
LENTINI F., TORELLI L. & TORTORICI L. (1990) – Principali
domini strutturali originatesi dalla collisione neogenicoquaternaria
nel Mediterraneo centrale. Mem. Soc. Geol. It.,
45, 453-462.
BESSE J. & COURTILLOT V. (2002) – Apparent and true polar
wander and the geometry of the geomagnetic field over the
last 200 Myr. J. Geophys. Res., 107 (B11), 2300,
doi:10.1029/2000JB000050.
CASTELLARIN A., COLACICCHI R. & PRATURLON A. (1978) – Fasi
distensive, trascorrenze e sovrascorrimenti lungo la linea
Ancona-Anzio dal Lias al Pliocene. Geologica Romana, 17,
161-189.
CHANNELL J.E.T., FREEMAN R., HELLER F. & LOWRIE W. (1982)
– Timing of diagenetic haematite growth in red pelagic
limestones from Gubbio (Italy). Earth and Planetary Science
Lett., 58, 189-201.
357
FISHER R. A. (1953) – Dispersion on a sphere, Proc. R. Soc.
London Ser. A, 217, 295-305.
GHISETTI F. & VEZZANI L. (1983) – Deformazioni pellicolari
mioceniche e plioceniche nei domini strutturali esterni
dell’Appennino centro-meridionale (Maiella ed Arco
Morrone-Gran Sasso). Mem. Soc. Geol. Ital., 26, 563-577.
LAVECCHIA G. (1985) – Il sovrascorrimento dei Monti Sibillini:
analisi cinematica e strutturale. Boll. Soc. Geol. It., 104,
161-194.
MATTEI,M.,FUNICIELLO R. & KISSEL C. (1995) – Paleomagnetic
and structural evidence for Neogene block rotations in the
central Apennines, Italy, J. Geophys. Res., 100, 17, 863-883,
doi:10.1029/95JB00864.
MCFADDEN P. L. & MCELHINNY M. W. (1988) – The combined
analysis of remagnetization circles and direct observations in
palaeomagnetism. Earth Planet. Sci. Lett., 87, 161-172,
doi:10.1016/0012-821X(88)90072-6.
PAROTTO M. & PRATURLON A. (1975) – Geological summary of
the central Apennines. Quad. Ric. Sci., 90, 257-306.
SATOLLI S., SPERANZA F. & CALAMITA F. (2005) –
Paleomagnetism of the Gran Sasso Range salient (central
Apennines, Italy): Pattern of orogenic rotations due to
translation of a massive carbonate indenter, Tectonics, 24,
TC4019, doi:10.1029/2004TC001771.
SATOLLI S. & CALAMITA F. (2008) – Differences and similarities
between the Central and Southern Apennines (Italy):
examining the Gran Sasso vs. the Matese-Frosolone salients
using paleomagnetic, geological and structural data. J.
Geophys. Res., 113, B10101. doi: 10.1029/2008JB005699.
SAGNOTTI L., WINKLER A., ALFONSI L., FLORINDO F. & MARRA
F. (2000) – Paleomagnetic constraints on the Plio-
Pleistocene geodynamic evolution of the external centralnorthern
Apennines (Italy), Earth Planet. Sci. Lett., 180, 243-
257.
SPERANZA F., SAGNOTTI L. & MATTEI M. (1997) – Tectonics of
the Umbria-Marche-Romagna Arc (central northern
Apennines, Italy): New paleomagnetic constraints, J.
Geophys. Res., 102(B2), 3153-3166, doi: 10.1029 /
96JB03116.
SESSIONE 10

SESSIONE 10
New insights on shallow to intermediate crustal structures of the
submerged Apenninic-Maghrebian chain (northern Sicily offshore)
coming from the re-processing of the
CROP M6A seismic reflection profile
Key words: Apenninic-Maghrebian chain, Crop-M6A seismic
line, reprocessing, Southern Tyrrhenian Sea.
INTRODUCTION
We present the preliminary results of the re-processing of the
high-penetration CROP-M6A NVR seismic profile. This reprocessing
was carried out to improve the signal-to-noise (S/N)
ratio of the seismic data, with the purpose of obtaining more
informations about the shallow-intermediate crustal features in
the northern Sicily offshore. In the re-processing sequence, we
have paid attention at the removal of both multiple reflectors and
the noise by focussing on solution of some additional problems
rising from both the stratigraphic-structural complexity of the
area and the rough seabottom morphology. That have suggested
in the past different sequences of re-processing (e.g. SCROCCA et
alii, 2003; FINETTI, 2005), focused on the solution of specific
problems like multiple de-reverberation, recovering of the high
frequency reflectors and recovering of deep signals below a thick
(more than 4 km) carbonate platform.
We re-processed the line applying migration methods by
choosing the appropriate algorithm and velocity field to data.
That allowed us to image features that were previously not clearly
visible. In addition, a strong interaction with the geologists in
charge of the profile interpretation and some a priori knowledge
about the possible geological setting characterise the new
processing approach.
The preliminary results show an increment of the signal
quality up to 4-5 s/TWT and, locally, the presence of deep events
up to 7-8 s/TWT.
The re-processed section was used to better constrain the
structural setting of the submerged Apenninic-Maghrebian Chain
along the seismic transect shedding light on the relationships
between the shallower and deepest tectonic elements.
_________________________
VERA VALENTI (*), CINZIA ALBANESE (*), MAURO AGATE (*), ATTILIO SULLI (*) & LUIGI LOMBARDO (*)
(*) Dipartimento di Geologia e Geodesia, Università di Palermo,
valv@unipa.it; cinzia.albanese@unipa.it; agate@unipa.it; attsu@unipa.it;
jijlombardo@hotmail.it
358
GEOLOGICAL SETTING
The 130 km long NNE–SSW trending seismic line explores
the submerged Apenninic-Maghrebian Chain made of, from the
bottom, by different superposed structural levels: a 6-7 km thick
lower wedge of carbonate platform units (Trapanese and
Panormide palaeodomains) underlying a level made up of deep
water carbonate bodies (Imerese palaeodomain), in turn
overthrust by the Oligo-Miocene Numidian Flysch terrains and an
upper level of deep water shales pertaining to the Sicilide
deposits (CATALANO et alii, 2000). This structural setting,
recognized in the southern part of the line, derives from a
Neogene deformation of the original African continental margin,
characterized by two main compressional events (CATALANO et
alii, 2000, AVELLONE et alii, 2010). In the central sector of the
transect, a segment of the Calabrian tectonic element is partially
superposed on the Sicilian-Maghrebian Chain; N-wards, a
transition to sub-oceanic crust locally occurs (PEPE et alii, 2005).
Widely throughout the extension of the investigated transect, the
Plio-Quaternary succession unconformably overlays the
underlying deformed units.
DATA SET
The CROP-M6A seismic line was acquired in the South
Tyrrhenian Sea within the CROP Project in 1991 by the
Osservatorio Geofisico Sperimentale (O.G.S.) of Trieste. Seismic
signals were recorded for 17.0 s two way time (t.w.t) at 4 ms
sample rate. The early processing stream was carried out by OGS
including: geometry definition, sum of two adjacent traces,
amplitude recovery, predictive deconvolution, multiple
attenuation, velocity analysis, normal move out and stack of the
common depth point reflection (CDP), F-K filter, and time
variant filters. However, in the published seismic sections
(SCROCCA et alii, 2003; FINETTI, 2005) multiple reflections and
diffraction hyperbolas are very frequent. Several previously
seismic reflection line interpretations (FINETTI, 2005; PEPE et
alii., 2005), magnetic, gravity (BERNARDELLI et alii, 2005), heat
flow (DELLA VEDOVA & PELLIS, 1992), as well as seismic
refraction data (CASSINIS et alii, 2003) have been used to

constrain, at a regional scale, the crustal sector here considered.
MAIN STEPS OF THE RE-PROCESSING AND
PRELIMINARY RESULTS
We carried out a conventional re-processing sequence
including some key steps for the improvement of the S/N ratio
and the signal continuity, such as the noise and multiple
attenuation, velocity analysis interpretation and the choice of an
appropriate migration algorithm, focussing in an extensive testing
of alternative solutions.
At first, F-K filtering was used in shot domain to try to
remove the sea-bottom multiples, but this method was not very
successful. So, we were able to remove four of the five order of
multiples recognized at the beginning by applying the muting in
Radon domain, using velocities ranging from 1500 to 2000 m/s.
A crucial step during the re-processing of seismic data was the
reconstruction of a velocity field. The NMO correction and stack
phase required a constant evaluation of the geological features to
test and to verify different stacking velocity fields, their effects on
the stack section and their consistency with plausible geological
models.
We first proceed by means of constant velocity stack panels,
from 2000 m/s to 6500 m/s in 500 m/s steps, and then by refining
the velocity field by means of detailed analysis on velocity
spectra, although at few specific locations and for limited depths
of investigation, the determination of the optimal velocity field
benefits from the knowledge of velocities derived from seismic
refraction data (CASSINIS et alii, 2003). This procedure was
iterated until a satisfactory result is obtained.
A post-stack migration was applied to our data by using finitedifference
migration technique (CLAERBOUT, 1985). That was
chosen since it offers relative speed and good handling of the
vertically and horizontally variant velocity field, having also a
good performance with low S/N ratio. The reprocessing
effectively attenuated both seismic noise and sea-bottom multiple,
increasing the resolution power of the data.
CONCLUSIVE REMARKS
The re-processing of the CROP – M6A seismic data has
produced a significant improvement in the quality of the final
migrated section, also bringing additional and valuable
information on deeper features than previously.
The success of the re-processing is not due to a single
operation: it is the consequence of a number of re-processing
steps carefully carried out, also after several iterations.
Furthermore, the knowledge of previous results was of primary
importance since it indicated the difficulties that had to be tackled
by the previous processing and allowed us to focus on some
problems.
359
Our preliminary findings contribute to better image the shallow
to intermediate crustal structures characterizing the submerged
Apenninic-Maghrebian Chain, as well as its structural
relationships with the Calabrian wedge, clarifying also the
tectonic processes responsible for formation of structural highs
(e.g. Solunto High) and sedimentary basins in the offshore North-
Sicily.
The until now obtained results may be considered fairly
satisfactory for a structural interpretation of the main horizons
that will be sounder as soon as more constraints will become
available.
REFERENCES
AVELLONE G., BARCHI M. R., CATALANO R., GASPARO
MORTICELLI M. & SULLI A. (2010) – Interference between
shallow and deep-seated structures in the sicilian fold and
thrust belt, Italy. J. Geol. Soc., 167, 109-126.
BERNARDELLI P., CAVALLI C., LONGONI R. & GIORI I. (2005) –
Gravity and magnetic fields of the Central Mediterranean
Region, in I.R Finetti (Ed.) CROP Project: Deep Seismic
Exploration of the Central Mediterranean and Italy, 57-67,
Elsevier, Amsterdam.
CASSINIS R., SCARASCIA S., & LOZEJ A. (2003) - The deep crustal
structure of Italy and surrounding areas from seismic
refraction data: a new synthesis. Boll. Soc. Geol. Ital. 122,
365–376.
CATALANO R., FRANCHINO A., MERLINI S. & SULLI A. (2000) –
Central western Sicily structural setting interpreted from
seismic reflection profiles. Mem. Soc. Geol. It., 55, 5-16.
CLAERBOUT, J. F. (1985) – Imaging the Earth’s Interior.
Blackwell Scientific Publications, Boston.
DELLA VEDOVA,B.&PELLIS G., (1992) – New heat flow density
measurements in the Ionian sea. Atti VIII Convegno GNGTS,
Roma, 1133-1145.
FINETTI I. (2005) - CROP project: deep seismic exploration of the
central Mediterranean and Italy. In I.R Finetti (Ed.) Atlases
In Geoscience 1, Elsevier, Amsterdam, 1-779.
PEPE F., SULLI A, BERTOTTI G. & CATALANO R. (2005) -
Structural highs formation and their relationship to
sedimentary basins in the north Sicily continental margin
(southern Tyrrhenian sea): implication for the Drepano
thrust front. Tectonophysics, 409, (1-4), 1-18.
SCROCCA D., DOGLIONI C., INNOCENTI F., MANETTI P., MAZZOTTI
A., BERTELLI L., BURBI L. & D'OFFIZI S., (2003) - CROP
Atlas: seismic reflection profiles of the Italian crust. Mem.
Descrittive Carta Geologica d'Italia, 62, 1-194.
SESSIONE 10

SESSIONE 10
Deformation and fluid circulation in an erosive subduction channel:
constraints from structural and isotopic studies
of the ancient analogue of the northern Apennines of Italy
Key words: Fluid-rock interaction, subduction channel,
Sestola-Vidiciatico tectonic Unit.
INTRODUCTION
Convergent margins are particularly rich in migrating fluids
that come from compacting sediments and dehydration
reactions in subducting minerals (BROWN et alii, 2001; SAFFER,
2003; SPINELLI &UNDERWOOD, 2004; SCREATON &SAFFER,
2005; SAFFER et alii, 2008). Most fluid drains along the plate
boundary and from the plate boundary into the fractured upper
plate (MOORE &VROLIJK, 1992; CARSON &SCREATON, 1998;
RANERO et alii, 2008) playing a central role in tectonic
processes shaping convergent margins.
We couple a detailed structural analysis focusing in
particular on calcite veins, with a stable isotope analysis to
characterize the fluid regime that existed during deformation in
an ancient erosive plate boundary exposed in the Emilia sector
of the Northern Apennines of Italy.
Here the fossil plate interface is represented by a 500 mthick
tectonic mélange known as the Sestola-Vidiciatico
tectonic unit active at least from early Miocene to middle
Miocene (VANNUCCHI et alii, 2008). At this plate boundary
basal and frontal tectonic erosion incorporated unlithified,
fluid-rich sediments into the fault zone (VANNUCCHI et alii,
2008).
In fact, in the Early Neogene, the Northern Apennine wedge
was characterized by the removal and underthrusting of its toe,
formed by both the accreted oceanic sediments and the
overlying wedge-top basin fill (Subligurian/External Ligurian
Units and their sedimentary cover: REMITTI et alii, 2007),
implying a process of frontal tectonic erosion (VANNUCCHI et
_________________________
PAOLA VANNUCCHI (*), FRANCESCA REMITTI (**), CHIARA BOSCHI (•),
GIUSEPPE BETTELLI (**) & LUIGI DALLAI (•)
(*) Università di Firenze.
(**) Università di Modena e Reggio Emilia, francesca.remitti@unimore.it
(•) IGG-CNR, Pisa.
360
alii, 2008) with the incorporation of upper plate material inside
a subduction channel.
The collected data lead to several conclusions about the
pattern, scale and temperature of fluid-rock interactions and the
source of fluids involved in the erosive subduction channel.
During the early-middle Miocene the plate boundary of the
Northern Apennines was characterized by several sub-parallel
décollements with two of them, at the top and at the bottom,
easy to identify. The orientation patterns and cross-cutting
relationships among the structures developed in the erosive
subduction channel imply an evolution of the deformation as
the material was transported to deeper and hotter portions of
the channel. The rheology of the material involved in the
subduction channel evolves from diffuse deformation in the
shallow zone to concentrated deformation in the intermediate
and deep zone. The onset of fault-like failure is linked to
cyclical rise and drop of fluid pressure: the subduction channel
material in the intermediate zone can accumulate fluid pressure
until the tensile overpressure condition (Pf > s 3) is locally
reached, therefore the mechanical behaviour of the subduction
channel is linked to fluids.
Three main fluid sources have been identified. While in-situ
fluids in equilibrium with the subduction channel components
were found at all sites, fluids from the underthrusting foredeep
turbidites and fluids from depth have also been identified. The
progressive increase of the deep fluid signature as the deeper
portions of the subduction channel are approached, involves a
complex fracture/fault systems where fluid flow episodes must
have been either highly channelized or had restricted pathways
to maintain the recorded isotopic heterogeneities.
REFERENCES
BROWN K.M., SAFFER D.M., & BEKINS B.A. (2001) - Smectite
diagenesis, pore-water freshening, and fluid flow at the toe
of the Nankai wedge. Earth Pl. Sci. Lett., 194(1-2), 97-109.
CARSON B. & SCREATON E.J. (1998) - Fluid flow in
accretionary prisms: Evidence for focused, time- variable
discharge. Reviews of Geophysics. 36(3), 329-351.

MOORE J.C. & SAFFER D. (2001) - Updip limit of the
seismogenic zone beneath the accretionary prism of
southwest Japan: An effect of diagenetic to low-grade
metamorphic processes and increasing effective stress.
Geology, 29(2), 183-186.
MOORE J.C. & VROLIJK P. (1992) - Fluids in accretionary
prisms. Rev. Geophys, 30, 113-135.
RANERO C.R., GREVEMEYER I., SAHLING U., BARCKHAUSEN U.,
HENSEN C., WALLMANN K., WEINREBE W., VANNUCCHI P.,
VON HUENE R., & MCINTOSH K. (2008) - The
hydrogeological system of erosional convergent margins
and its influence on tectonics and interplate seismogenesis.
Geochem. Geophys. Geosyst., 9, Q03, doi: 10.1029/2007G
C001679.
REMITTI F., BETTELLI G., & VANNUCCHI P. (2007) - Internal
structure and tectonic evolution of an underthrust tectonic
mélange: the Sestola-Vidiciatico tectonic unit of the
Northern Apennines, Italy. Geodin. Acta, 20, 37-51.
SAFFER D.M. (2003) - Pore pressure development and
progressive dewatering in underthrust sediments at the
Costa Rican subduction margin: Comparison with northern
Barbados and Nankai. J. Geophys. Res., 108(B5), 2261.
SAFFER D.M., UNDERWOOD M.B., & MCKIERNAN A.W. (2008)
- Evaluation of factors controlling smectite transformation
and fluid production in subduction zones: Application to
the Nankai Trough. Island Arc, 17(2), 208-230.
SCREATON E. J. & SAFFER D.M. (2005) - Fluid Expulsion and
overpressure development during initial subduction at the
Costa Rica convergent margin. Earth Pl. Sci. Lett., 233,
361- 374.
SPINELLI G.A., & UNDERWOOD M.B. (2004) - Character of
sediments entering the Costa Rica subduction zone:
Implications for partitioning of water along the plate
interface. Island Arc, 13(3), 432-451.
VANNUCCHI P., REMITTI F., & BETTELLI G. (2008) - Geologic
record of fluid flow and seismogenesis along an erosive
subducting plate boundary. Nature, 451, 699-703.
361
SESSIONE 10

SESSIONE 10
Exhumation of the Voltri Massif HP-units, Ligurian Alps
GIANLUCA VIGNAROLI (*), FEDERICO ROSSETTI (*), DANIELA RUBATTO (**), THOMAS THEYE (•), FRANK LISKER (°),
DAVID PHILLIPS (°°) & CLAUDIO FACCENNA (*)
Key words: Exhumation, HP-units, P-T-d-t path, Voltri Massif.
The Voltri Massif of the Ligurian Alps (e.g. CHIESA et alii,
1975; VANOSSI et alii, 1984) is a key area to investigate the
geological parameters and tectonic scenarios driving exhumation
of the Alpine high-pressure (HP)-complexes, because of: (i) it is
located at the junction between the Western Alps and the
Northern Apennines and (ii) it defines a c. 30 km wide
metamorphic domain characterised by a meta-ophiolitic sequence
with an eclogitic core, unconformably covered by the Early
Oligocene to Messinian sediments of the Tertiary Piedmont Basin
(e.g. GELATI & GNACCOLINI, 1998). Moreover, no general
consensus exists about the Pressure-Temperature-deformationtime
(P-T-d-t) path followed by the exhumed HP-units (see e.g.
HOOGERDUIJN STRATING, 1994; CAPPONI AND CRISPINI, 2002;
FEDERICO et alii, 2007; VIGNAROLI et alii, 2009).
By integrating geological mapping with new structural,
petrological, and geo/thermochronological (U-Pb SHRIMP
dating on zircon and titanite, 40 Ar/ 39 Ar dating on phengite and FT
analysis on apatite) studies, a polyphase tectono-metamorphic
history was reconstructed for the HP-units of the Voltri Massif,
consisting of: (i) a D1-M1 stage, corresponding to the peak
metamorphism achieved under blueschist-to-eclogitic facies
conditions, which is placed between ~34 and ~50 Ma (see also
RUBATTO &SCAMBELLURI, 2003; FEDERICO et alii, 2005); (ii) a
D2-M2 stage, assigned to the 30-35 Ma time interval, and
corresponding to the main top-to-the-W/NW retrogressive event
equilibrated within the greenschist facies conditions; and (iii) a
D3-M3 stage (considered to have taken place at ~30 Ma),
representing a continuous exhumation towards brittle-dominated
_________________________
(*) Dipartimento di Scienze Geologiche, Università degli Studi ROMA
TRE, Roma - vignarol@uniroma3.it
(**) Research School of Earth Sciences, Canberra
(•) Institut für Mineralogie und Kristallchemie der Universität, Stuttgart
(°) FB Geowissenschaften, University of Bremen
(°°) School of Earth Sciences, The University of Melbourne
362
environments. This latter event overlaps with main regional
denudation episode and onset of the Tertiary Piedmont Basin
sedimentation (BERTOTTI et alii, 2006).
The reconstructed P-T-d-t path for the Voltri HP-units
supports an exhumation history defined by (i) an initial, nearly
isothermal, phase (from D1-M1 to D2-M2) with highly variable
exhumation rates; and (ii) a second phase (from D2-M2 to upper
crustal levels, D3-M3) during cooling with moderate exhumation
rates in the order of ~1-2 mm yr -1 . This two-stage exhumation
process can be reconciled within a tectonic scenario characterised
by a switch from a syn-orogenic setting along the Alpine-
Apennine convergence zone to post-orogenic back-arc crustal
thinning achieved along low-angle top-to-the-W, ductile-to-brittle
extensional detachment systems.
REFERENCES
BERTOTTI G., MOSCA P., JUEZ J., POLINO R. & DUNAI T. (2006) -
Oligocene to Present kilometres scale subsidence and
exhumation of the Ligurian Alps and the Tertiary Piedmont
Basin (NW Italy) revealed by apatite (U–Th)/He
thermochronology: correlation with regional tectonics. Terra
Nova, 18, 18-25.
CAPPONI G. & CRISPINI L. (2002) - Structural and metamorphic
signature of alpine tectonics in the Voltri Massif (Ligurian
Alps, Noth-Western Italy). Eclogae Geol. Helv., 95, 31-42.
CHIESA S., CORTESOGNO L., FORCELLA F., GALLI M., MESSIGA
B., PASQUARÉ G., PEDEMONTE G.M., PICCARDO G.B. & ROSSI
P.M. (1975) - Assetto strutturale ed interpretazione
geodinamica del Gruppo di Voltri. Boll. Soc. Geol. Ital., 94,
555-581.
FEDERICO L., CAPPONI G., CRISPINI L., SCAMBELLURI M. & VILLA
I.M. (2005) - 39 Ar/ 40 Ar dating of high-pressure rocks from the
Ligurian Alps: evidence for a continuous subductionexhumation
cycle. Earth Pl. Sci. Lett., 240, 668-680.
FEDERICO L., CRISPINI L., SCAMBELLURI M. & CAPPONI G. (2007)
- Ophiolite mélange zone records exhumation in a fossil
subduction channel. Geology, 35, 499-502.

GELATI R. & GNACCOLINI M. (1998) - Sedimentary tectonics and
sedimentation in the Tertiary Piedmont Basin, north-western
Italy. Riv. Ital. Paleontol. Stratigr., 104, 193-214.
HOOGERDUIJN STRATING E.H. (1994) - Extensional faulting in an
intraoceanic subduction complex – working hypothesis for the
Palaeogene of the Alps-Apennine system. Tectonophysics,
238, 255-273.
RUBATTO D. & SCAMBELLURI M. (2003) - U-Pb dating of
magmatic zircon and metamorphic baddeleyte in the Ligurian
eclogites (Voltri Massif, Western Alps). Contrib. Mineral.
Petrol., 146, 341-355.
VANOSSI M., CORTESOGNO L., GALBIATI B., MESSIGA B.,
PICCARDO G. & VANNUCCI R. (1984) - Geologia delle Alpi
Liguri: dati, problemi, ipotesi. Mem. Soc. Geol. It., 28, 5-75.
VIGNAROLI G., FACCENNA C. & ROSSETTI F. (2009) -
Retrogressive fabric development during exhumation of the
Voltri Massif (Ligurian Alps, Italy): arguments for an
extensional origin and implications for the Alps-Apennine
linkage. Int. J. Earth Sci., 98, 1077-1093.
363
SESSIONE 10

SESSIONE 10
Key words: Abano Terme, fissure ridge, Schio-Vicenza fault,
travertine.
THE EUGANEAN GEOTHERMAL FIELD
The Euganean Geothermal Field (EGF) develops along the
northwest-trending Schio-Vicenza fault system (SVFS), a
structure that marks the western side of the Friuli and Veneto
plain, which is the foreland of three surrounding chains:
Dinarides, Alps and Apennine.
Fig. 1 – Historical picture of the thermal well on the Montirone Hill.
The EGF is located close to the northeast margin of the
Euganean Hills (PICCOLI et alii, 1976), where the existence of a
extensional relay zone between segments of the SVFS has been
proposed (ZAMPIERI et alii, 2009). Given the Neogene to
Quaternary sinistral strike-slip kinematics, superimposed on preexisting
normal faults, this structure is responsible for rock
fracturing and permeability increase, enhancing the quick
uprising of thermal waters. In this area about 100 mining claims
and more than 400 wells have been drilled. Thermal waters
_________________________
(*) Dipartimento di Geoscienze – Università degli studi di Padova,
dario.zampieri@unipd.it
Lavoro eseguito nell’ambito del progetto ex 60% Università di Padova
“Modello idrogeologico e geologico strutturale dell'area termale euganea"
(resp. P. Fabbri) e della tesi di dottorato (M. Pola) finanziata dalla
Fondazione CariPaRo.
The fissure ridge of Abano Terme (Padova)
DARIO ZAMPIERI (*), MARCO POLA (*) & PAOLO FABBRI (*)
364
(60°C < T< 86°C) are principally used for medicinal and tourism
purposes, with a subsidiary use as energy to heat hotels and
greenhouses. At present, about 250 wells are active and the total
average flow rate of thermal fluids is about 17 Mm 3 /year. Most
wells (depths from about 300 m to more than 1000 m) extend for
several hundred meters into bedrock, however well casing is
placed only in the Quaternary cover.
THE FISSURE RIDGE
Until the sixties, one of the main natural occurrences of the
outflow in the EGF was located in the town of Abano Terme,
marked by a 5 meter-high hill of travertine, called Montirone.
Thermal waters fed several pools located on the flat top and at
the base of the ridge (Fig. 1) and were also channelized to move a
mill-wheel (VANDELLI, 1761). Exploitation of the thermal waters
lowered the potentiometric level and dried up the hot springs. At
present the travertine hill is used as a public park. The hill is
affected by a network of fractures (Fig. 2a) mainly composed of
two sub-orthogonal fracture sets (NW-SE and NNE-SSW, Fig.
2b), which allow us to refer to the travertine deposit as a fissure
ridge. These structures have been studied in tectonically active
regions of Turkey (Anatolia), Greece (Euboea island), the USA
(California) and Italy (Tuscany), showing typical features and
providing significant information about stress orientation during
travertine deposition (e.g. HANCOCK et alii, 1999; TEMIZ et alii,
2009; BROGI et alii, 2009).
The trend of the two fracture sets parallels the trend of the
main structural elements of the region. It suggests that the fissure
ridge is localized above an extensional fissure or in the hanging
wall of a transtensional fault cutting the bedrock lying about one
hundred meters beneath the alluvial cover.
The presence of the Montirone travertine deposit strongly
supports the existence of 1) a releasing structure in the subsurface
which controls the development of the EGF and, 2) ongoing
activity of the Schio-Vicenza fault.
REFERENCES
BROGI A. & CAPEZZUOLI E. (2009) - Travertine deposition and
faulting: the fault-related travertine ?ssure-ridge at Terme
S.Giovanni, Rapolano Terme (Italy). Int. J. Earth Sc., 98,
931–947.

HANCOCK P.L., CHALMERS R.M.L., ALTUNEL E. & ÇAKIR Z.
(1999) - Travitonics: using travertines in active fault studies.
J. Struct. Geol., 21, 903–916.
PICCOLI G. et alii (1976) - Il sistema idrotermale euganeo berico
e la geologia dei Colli Euganei. Mem. Ist. Geol. Miner. Univ.
Padova, 30, 266 pp.
TEMIZ U., GÖKTEN E. & EINKENBERG J. (2009) - U/Th dating of
fissure ridge travertines from the Kirsehir region (Central
Anatolia Turkey): structural relations and implications for
the Neotectonic development of the Anatolian block.
Geodinamica acta, 22(4), 201-213.
VANDELLI D. (1761) - De Thermis Agri Patavini. Tipografia
Conzatti, Padova, 234 pp.
ZAMPIERI D., FABBRI P. & POLA M. (2009) - Structural
constraints to the Euganean Geothermal Field (NE Italy).
Rend. online Soc. Geol. It., 5, 238-240.
a)
Fig. 2 – Fracture on the top of the Montirone fissure ridge (a). The rose diagram of the directions of the fractures (b) clearly shows two main trends oriented N
20 E and N 60 W, parallel to the main structural elements of the region.
365
Rose diagram of the fractures
of Montirone fissure ridge
N
b)
SESSIONE 10

SESSIONE 10
40 Ar/ 39 Ar dating of pseudotachylytes: direct evidence of Cretaceous
to Eocene compressions in the central Southern Alps
Key words: 40 Ar/ 39 Ar dating, Cretaceous orogeny, Orobic Thrust,
Porcile Thrusts, Pseudotachylytes.
INTRODUCTION AND GEOLOGICAL SETTING
The central Southern Alps (CSA), comprised between Lake
Como and the Adamello massif, belong to the S-verging retrobelt
of the Alps (LAUBSCHER, 1985), from which they are
separated by the E-W trending Tonale Line (SCHMID et alii,
1989). The structure of the CSA is typical of a thick-skinned foldand-thrust
belt (CARMINATI et alii, 1997) which involves both
basement and Permian to Cenozoic cover succession. Alpine
metamorphism was weak with respect to the Austroalpine units to
the north of the Tonale Line.
The pre-Alpine basement of the Southern Alps is thrusted
southward over the sedimentary successions along the Orobic
thrust and related faults which form a continuous fault-system
extending more than 80 km in length.
The Alpine structural evolution of the Southern Alps still
poses several unsolved problems especially on its oldest history
and its possible relationships with the Eoalpine tectonic events
affecting the Austroalpine domain. The occurrence of a pre-
Tertiary orogenic phase was already emphasized by several
authors on the base of indirect sedimentary evidence (DOGLIONI
&BOSELLINI, 1987; BERSEZIO &FORNACIARI, 1994) and K/Ar
dating of andesitic dykes cross-cutting thrust surfaces in the
Presolana area (ZANCHI et alii, 1990). The opportunity to date the
oldest thrust structures of the Southern Alps occurs in the western
Orobic region, where the occurrence of pseudotachylyte veins has
been described by previous authors (MEIER, 2003; CARMINATI &
SILETTO, 2005) along the Orobic and Porcile thrusts.
FOLD, CLEAVAGE AND FAULT ANALYSES ACROSS
THE OROBIC THRUST
In the Passo San Marco area the metamorphic basement
_________________________
(*) Dipartimento di Scienze Geologiche e Geotecnologie, Università degli
Studi di Milano Bicocca, stefano.zanchetta@unimib.it
STEFANO ZANCHETTA (*), PAOLO D’ADDA (*) & ANDREA ZANCHI (*)
366
displays a polyphase history with at least three ductile
deformation phases. D1 and D2 structures are considered to be of
Variscan age (CARMINATI &SILETTO, 2005). D1 structures are
preserved only as relic foliation and rootless folds within quartzrich
lithologies, whereas D2 fabric elements consist in isoclinal
folds associated to an axial plane foliation developed under upper
greenschist facies conditions (SPALLA et alii, 1999).
The D3 phase produced medium-tight folds not accompanied
by the development of an axial plane schistosity.
In the hangingwall of the Orobic thrust D3 fold axes trend
approximately N-S to NE-SW with dip angles of 25-30°.
Approaching the fault zone from the North, D3 folds
progressively rotate, becoming subparallel to the greenschist
facies mylonitic foliation that characterises the basement-derived
fault zone of the Orobic thrust. The described geometric features
of D3 folds suggest that the first ductile deformation stage of the
Orobic thrust postdates D3 folding.
Greenschist facies mylonites are preserved only locally due to
a pervasive overprint by subsequent brittle structure. The
mylonitic foliation dips N to NNE with dip angles close to 45°.
Dark-coloured cataclastic bands cross-cut mylonites at low
angles. Fault analyses of these bands revealed the occurrence of
dip-slip reverse fault with a preferential ENE-WSW strike and a
northward dip of 20°-60°, due to the occurrence of secondary R
shear planes.
Reverse faults are associated to pseudotachylyte veins. The
melt generation surfaces of pseudotachylytes show very similar
geometrical features with reverse faults, suggesting that the
genesis of pseudotachylytes is directly related to the main brittle
stages of thrust propagation.
The cover succession in the footwall of the Orobic thrust
shows medium to tight folds with a metre-scale wavelenght. In
fine-grained sandstones and siltstones an axial plane pressuresolution
cleavage locally occurs. Fold axial planes and cleavage
dip N to NW with dip angles of 40°-55°, resulting subparallel to
the Orobic thrust surface. This suggests that folding in the cover
is related to S-directed movements along the Orobic thrust.
40 Ar/ 39 Ar DATING OF PSEUDOTACHYLYTES
Pseudotachylytes discontinuously decorate fault planes and
typically display thickness from few to 20-25 mm, with rare
reservoir veins reaching 70-80 mm along the Porcile thrust. The

host rock usually displays cataclastic fabric and only in a few
cases pseudotachylytes cross-cut greenschist facies mylonites free
of brittle overprint. Systematic cross-cutting relationships
between different pseudotachylyte veins generations were never
observed in the field even if evidence of multiple events of
friction-induced melting were recognised at the micro-scale.
From pseudotachylyte samples micro-cores of 1-2 mm of
diametres were drilled and analysed by X-ray Micro-
Computerised-Tomography (microCT) combined with image
analyses. The microCT screening served to asses in 3D the
clast/matrix ratio of each micro-core in order to choose almost
clast-free sample for Ar-Ar dating.
Stepwise-heating experiments were performed in the 400-
1400°C T range, using 10 or 11 incremental steps.
All gas release pattern display similar features. The low T
steps have isotopic Ca/K values that differ from matrix values
determined by Electron Microprobe analyses. These devious
Ca/K values are likely correlated to the presence of secondary or
alteration mineral phases. The central, flat part of the spectrum,
occurring at intermediate T, corresponds to Ca/K values within
the chemical composition of pseudotachylyte matrix determined
with the microprobe. The intermediate T steps are therefore
interpreted to represent gas release from matrix and so were used
for crystallisation age calculations. High T steps invariably give
the oldest ages with highest Ca/K values. These steps are related
to the breakdrown of inherited clasts, chiefly made of plagioclase.
Two age clusters of pseudotachylytes matrix were obtained
both along the Orobic and Porcile thrusts: a Late Cretaceous (80-
68 Ma) and latest Paleocene to middle Eocene (55-43 Ma).
These data strongly support the occurrence of a Cretaceous
compressive deformation if the central Southern Alps, till now
only suggested on the base of indirect evidence. This suggests
that the Alpine evolution of the Orobic Alps, prior to the
Adamello intrusion, was correlated to a long-lasting compressive
deformation, probably subdivided in two main stages.
Late Cretaceous is also a minimum age for the ductile/brittle
transition in the present-day exposed basement units. This implies
that ductile deformation, at least in the crustal levels now
exposed, took place only in the earliest growth phase of the CSA
orogenic wedge. The oldest pseudotachylyte ages are tentatively
correlated to the Cretaceous orogenic phase (SCHMID et alii, 2004
with literature) documented in the Austroalpine domain north of
the Periadriatic Lineament.
The Middle Eocene re-activation of the Orobic and Porcile
thrusts predates the Adamello intrusion and the main activity
period of the Tonale segment of the Periadriatic Lineament.
The geodynamic significance of the pre-Adamello Eocene
deformation in the Orobic Alps is still unclear. Its relationships
with the Tertiary orogenic phase recorded in the N-verging sector
of the Alpine belt need further studies to be fully understood.
Our data provide evidence that the evolution of the central
Southern Alps was polyphase and more complex than previously
367
envisaged. In this context the understanding of the tectonic
evolution of the central Southern Alps gives also important
constraints for the reconstruction and interpretation of the whole
central sector of the Alpine belt.
REFERENCES
BERSEZIO R. & FORNACIARI M. (1994) – Syntectonic Upper
Cretaceous deep-water sequences of the Lombardy Basin
(Southern Alps, Northern Italy). Eclo. Geol. Helv., 87 (3),
833-862.
CARMINATI E., SILETTO G. & BATTAGLIA D. (1997) – Thrust
kinematics and internal deformation in basement involved
foreland fold and thrust belts: the Eastern Orobic Alps case
(Central Southern Alps, Northern Italy). Tectonics, 16, 259-
271.
CARMINATI E. & SILETTO G.B. (2005) – The Central Souther
Alps (N Italy) paleoseismic zone: a comparison between field
observations and predictions of fault mechanics.
Tectonophysics, 401, 179-197.
DOGLIONI C. & BOSELLINI A. (1987) – Eoalpine and Mesoalpine
tectonic in the Southern Alps. Geol. Rundsch., 76, 735-754.
LAUBSCHER H.B. (1985) – Large scale, thin-skinned thrusting in
the Southern Alps: kinematic models. Geol. Soc. Am. Bull.,
76, 710-718.
MEIER A. (2003) – The Periadriatic Fault System in Valtellina
(N-Italy) and the evolution of the Southwestern Segment of
the Eastern Alps. PhD Thesis, Diss. Eth. No. 15008, Zurich.
SCHMID S.M., AEBLI H.R., HELLER F. & ZINGG A. (1989) – The
role of the Periadriatic Line in the tectonic evolution of the
Alps. In: M.P.Coward, D. Dietrich & R.G. Park, (Eds.),
Alpine tectonics. Spec. Publ. Geol. Soc. London, 45, 153-
171.
SCHMID S.M., FÜGENSCHUH B., KISSINGL E. & SCHUSTER R.
(2004) – Tectonic map and overall architecture of the Alpine
orogen. Eclo. Geol. Helv., 97, 93-117.
SPALLA M.I., CARMINATI E., CERIANI S., OLIVA A. & BATTAGLIA
D. (1999) – Influence of deformation partitioning and
metamorphic re-equilibration on P-T path reconstruction in
the pre-Alpine basement of Central Southern Alps (Northern
Italy). J. Metamorphic Geol., 17, 319-336.
ZANCHI A., CHIESA S. & GILLOT P.Y. (1990) – Tectonic evolution
of the Southern Alps in the Orobic chain: structural and
geochronological indications for pre-Tertiary compressive
tectonic. Mem. Soc. Geol. It., 44, 77-82.
SESSIONE 10

SESSIONE 10
368

SESSIONE 11
Geotermia e risorse geotermiche
CONVENERS
Alessandro Sbrana (Università di Pisa)
Paolo Fulignati (Università di Pisa)
369
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SESSIONE 11
Geochemical surveillance of reactive gas from geothermal area of
Pozzuoli Solfatara (Naples, Italy): chronological evolution and local
ground displacement
Keywords: Bradysism, Campania, Pozzuoli.
Since 2000, the Geoscience and Earth Resources Institute
researchers are working on the area of Phlegrean Fields with
systematic sampling on fluids emission from Pozzuoli Solfatara,
specifically fumaroles named Bocca Grande and Soffionissimo
(and Forum Vulcani till 1984). This scientific activity is a follow
on of similar work carried out on the same area from 1982 to
1997, with particular attention to gas monitoring (CO2, H2, CH4,
H2S, N2, Ar, He, Rn).
Our results evidence that reactive gases H2, CH4, H2S
show a specific trend that can be well represented on a triangular
diagram.
The 2001-2005 compositional trend point out to a
refocusing towards values measured during the 1983/85 period,
which was characterized by accentuate bradisism phenomena.
More, according to our observation, the period from 1989-
1997 shows similar path of reactive fumarolic gas evolution.
Compared observation in different periods of triangular
diagrams H2, CH4, H2S with the graphic about ground level
variation till 2003, shows a correspondence between the
evolution of relative gas concentrations and the trend of
bradisism.
More specifically, on the base of our data set, we can define
a trend characterized from a relative increase of H2S, a decrease
of H2 and prevalently CH4 during the phase of negative
bradisism.
Following this preliminary observations, the correspondence
between temporal evolution of gas chemical composition and new
bradisism phenomena, could enlighten the contribution of
geochemical monitoring on the study of the phenomena related to
soil subsidence in the Phlegrean field area.
_________________________________________________
(*) Istituto di Geoscienze e Georisorse, CNR Pisa, caprai@igg.cnr.it,
scarsi@igg.cnr.it
ANTONIO CAPRAI (*) & PAOLO SCARSI (*)
370

Medium enthalpy geothermal fluids in the Argentera Massif:
geochemical investigations for further
geothermal exploration studies.
Key words: Geochemistry, geothermal fluids, geothermometers,
medium enthalpy, South-Western Alps.
INTRODUCTION
At the beginning of 20th century Italy was the first nation in
the world exploiting geothermal resources and produce electricity
in Lardarello (Tuscany) and nowadays it is the fifth nation for
electricity production. Only a few geothermal exploration
projects were, however, carried outside of Tuscany. The southern
part of Piedmont and in particular the Italian side of the
Argentera Massif shows favorable conditions for exploitation of
thermal waters at Bagni di Vinadio and Terme di Valdieri. The
main objectives are to decipher the origin of the fluids from its
chemical and isotopic compositions, in relation to natural fluid
pathways inferred from geological and geophysical prospection
to detect the deep structures and more shallow investigations.
GEOLOGICAL SETTING
The two study areas are located in the Argentera Massif, the
southernmost of the external crystalline massifs of the Alps. The
massif can be divided into two main complexes: The Malinvern
Argentera Complex, mainly constituted by migmatitic gneisses,
and the Tinée Complex, mainly formed by anatectic gneisses. In
particular the studied thermal springs are entirely located within
the Malinvern Argentera Complex. The structural setting of the
Argentera Massif is the result brittle reactivation of pre-Alpine
and early-Alpine ductile shear zones. A main NW-SE shear zone,
the Valletta Shear Zone, crosscuts the massif dividing the two
complexes and branches towards North in the Bersezio Fault. In
the central part of the massif, the Valletta Shear Zone connects to
the Fremamorta Shear Zone, a E-W oriented milonitic corridor
with a reverse sense of shear (BAIETTO, 2006, PERELLO et alii
2001).
_________________________
(*) Dipartimento di Scienze della Terra - Università di Torino,
cesare.comina@unito.it, luca.guglielmetti@unito.it,
giuseppe.mandrone@unit.it
CESARE COMINA (*), LUCA GUGLIELMETTI (*) & GIUSEPPE MANDRONE (*)
371
At Bagni di Vinadio, thermal springs discharge at 1320 m
a.s.l. through intensely fractured aplitic dykes located at the
margins of the Bersezio Fault. The Terme di Valdieri springs
discharge at 1425 m a.s.l. in one of the most elevated sector of
the Argentera Massif. In particular the springs emerge through
the damaged zone of the Lorusa Fault a 7 km-long NW-SE strike
slip fault that cuts through migmatitic gneisses.
GEOCHEMISTRY
The geochemistry of the waters of the two thermal sites was
already studied in the past (FANCELLI &NUTI, 1978). During two
campaigns, waters samples of both thermal and fresh water
sources were collected to add more information and data.
Conductivity, pH, Temperature were measured in the field and
then compared to the measured values at the lab. All the samples
were analyzed by means of ion chromatography for the major
ions, by means of Inductive Coupled Plasma spectrometry (ICP)
for trace elements, heavy metals and Si, and d 2 H, d 18 O, Tritium
isotopes were also analyzed. These analyses showed many
differences between the thermal waters at Bagni di Vinadio and
at Terme di Valdieri. At Bagni di Vinadio temperature ranges
between 28°and 72°C and shows a direct relationship with the
TDS that ranges between 400 and 2700 mg/l. Both the Vinadio
and Valdieri waters have pH values of 7-9 or even higher and the
alkalinity ranges between 0.2 to 1 meq/l at Vinadio and between
0.3 to 0.9 meq/l at Valdieri. At Terme di Valdieri Temperature
ranges between 32°C and 65°C, but the TDS is constant at 300
mg/l. The Piper diagram shows both the different chemical
composition between thermal waters at the two study sites and
the chemical differences between thermal and cold waters at
Vinadio whereas at Valdieri this does not occur. A Schoeller
diagram shows the general higher mineralization of the thermal
waters, the high Cl - content and the lower SO4 - concentration at
Vinadio compared to that at Valdieri. The main cation is Na + for
both waters at Vinadio and Valdieri but Cl - is the major anion for
Vinadio as SO4 2- is for Valdieri. It is evident the differentiation
between the thermal waters at Vinadio and at Valdieri: in fact
Vinadio hot waters create a distinct group itself showing a higher
concentration of chloride while those at Valdieri, richer in
bicarbonate, are much closer to the cold water that have almost
the same composition both at Vinadio and Valdieri.
The content in stable isotopes d 2 H and d 18 O were evaluated
SESSIONE 11

SESSIONE 11
from selected water samples. The sampled waters plot close to
World Meteoric Water Line and the Mediterranean Sea Meteoric
Line indicating that the thermal fluids are meteoric waters and in
particular show the influence with Mediterranean precipitations.
Both thermal springs and cold waters fall into the range between
-10 and -13 (‰ vs. SMOW) for the isotope d 18 O and within -80
and -100 (‰ vs. SMOW) for the d 2 H isotope. Thermal waters do
not exhibit positive d 18 O-shift, typical of high-temperature
geothermal systems with long water residence time at depths.
Isotopic analysis show that the waters coming from the two
locations are close to world meteoric water line and show the
influence with Mediterranean precipitations. Water infiltration
elevations can also be inferred from these isotopic data: 1700-
2000 m for both Bagni di Vinadio and Terme di Valdieri.
Tritium analysis show very low values (0.6

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Ultrasonic test in geothermal heat exchangers (BHE) to monitor grout
integrity against migration of contaminants into ground water system.
CESARE COMINA (*), LUCA GUGLIELMETTI (*) & GIUSEPPE MANDRONE (*)
Key words: Aquifers, borehole exchangers, cementation,
Geothermic, ultrasonic monitoring.
Non-electric uses of geothermal energy in Italy are associated
with the spa business, greenhouses and fish farming and space
heating, including district heating (CARELLA &SOMMARUGA,
2000). An ideal heat source has a high and stable temperature
during the heating season, is abundantly available, is not
corrosive or polluted, has favourable thermophysical properties,
and its utilisation requires low investment and operational costs.
In most cases the availability of the heat source is the key factor
determining its use: ground water and rocks are the main heat
sources in most of the Northern Italian regions.
Ground water is available with stable temperatures (4-10°C)
in many regions. Open or closed systems are used to tap into this
heat source. In open systems the ground water is pumped up,
cooled and then reinjected in a separate well or returned to
surface water. Closed systems can either be direct expansion
systems, with the working fluid evaporating in underground heat
exchanger pipes, or brine loop systems. A major disadvantage of
ground water heat pumps is the cost of installing the heat source.
Additionally, local regulations may impose severe constraints
regarding interference with the water table and the possibility of
soil pollution. Rocks (geothermal heat) can be used in regions
with no or negligible occurrence of ground water. Typical bore
hole depth ranges from 100 to 200 metres. This type of heat
pump is always connected to a brine system with welded plastic
pipes extracting heat from the rock.
Vertical ground loop heat exchangers typically consist of
high-density-polyethylene (HDPE) pipe U-tubes inserted in deep
boreholes. The boreholes have typical diameters of 76 mm to 127
mm and the pipe diameters in the range from 19 mm 38 mm. The
pipes forming the U-tube are accordingly closely spaced in the
borehole. A grout mixture is typically pumped into the borehole
to fill the gap between the U-tube and the borehole walls. The
purpose of the grout is to improve the heat transfer between the
soil and plastic pipes by providing a better contact surface
between them, and also to provide a seal around the U-tube to
guard against migration of contaminants into the ground water
_________________________
(*) Dip. Scienze della Terra - Università di Torino, cesare.comina@unito.it,
luca.guglielmetti@unito.it, giuseppe.mandrone@unit.it
375
system.
Geothermal heat pumps uses are not common in Italy,
contrary to Central and Northern Europe examples. As for all
new techniques, there is a general apprehension mainly due to
two questions: 1) Is it working? 2) Is it a possible source of
pollution for water tables?
Thermal response tests can answer question n.1. They can
integrate the underground thermal properties along the entire
length of a BHE, including groundwater and backfilling material,
providing a so-called “effective” thermal conductivity as defined
under strict heat conduction assumptions. Laboratory
measurements alone may lead to different values since they
cannot correctly account for groundwater flow and water-filled
cracks and pores (SIGNORELLI et alii, 2007)
Question n. 2 is still a problem. Actually, the only assurance
that the PVC pipes are completely insulated from the ground (and
from the aquifers) is given by the blowing up of the backfilling
material, pumped up from the bottom of the drilling.
The problem of the integrity of the backfill and its
functionality in respect to hydraulically insulate of BHE from the
ground is not so different from other situations in civil
engineering. For example, non-destructive test methods have
become the standard in quality assurance of concrete piles
particularly in respect to shaft foundations. Several methods are
available to perform this tests but ultrasonic logging techniques
play the major role (RAUSCHE, 2004; LIKINS et alii, 2007). The
purpose of these tests is to assess the homogeneity and integrity
of concrete between one or more access tubes. Testing
specifications requires medium diameter, water filled, access
tubes installed full-length in the shaft.
Test equipment includes an ultrasonic transmitter, a matched
receiver and a data acquisition system. In Cross Hole logging the
transmitter and receiver are inserted into the bottom of two tubes,
raising them simultaneously while the transmitter continuously
emits and the receiver acquires the ultrasonic signals. A related
technique is the Single Hole logging method which requires only
a single access tube. Testing is done by lowering the transmitter
and receiver on top of each other and then scanning the pile as
the 2 are retrieved. In both methods the records of signal travel
time (and relative strength) yield an assessment of the concrete
quality and continuity. In the Single Hole method problems arise
due to the sensors vicinity since travel times can be strongly
affected by water and concrete-tube interface.
SESSIONE 11

SESSIONE 11
Since in BHE access water filled tubes are already available
these techniques can be potentially used to evaluate the quality
and integrity of cementation in the exchanger. Several problems
must be however taken into consideration. First usually small
diameter tubes are used so that the insertion of the ultrasonic
sonde is not possible. Secondly the tubes are not perfectly vertical
one to each other and can be quite tortuous so that a good
calibration of data is not always possible.
The potentiality of ultrasonic tests in the verification of a
good cementation quality in BHE has been therefore attempted
on an experimental pile. The pile is about 4 m high and is
generally constituted by a 1:1 mix of concrete and bentonite.
Some defects, layers of coarse sand mixed with expanded clay,
have been moreover placed in the pile at different heights. Two
access tubes (3,8 cm in diam.) have been inserted in the pile and
have been filled with water for the execution of both Cross Hole
and Single Hole logs by means of a commercially available
monitoring system (CHUM - www.piletest.com). After the
execution of the tests, a window was opened in the pile in order
to verify experimental data.
Cross hole test results are reported in fig. 1 and compared
with a picture of the experimental pile. A visual inspection of the
test signals (“nested” in a diagram) can guide in the location of
the integrity zones. Defect identification is clear both in the first
arrival travel time curve then in the relative velocity curve. In
particular the cemented zones are highlighted for velocities
higher then 2500 m/s. Since wave transmission is strictly related
to the presence of water in the tubes in the upper part of the pile
no signal has been acquired for the last concrete layer.
Also single hole tests were performed with different distance
between receivers. In this testing disposition the first arrival
travel time curve was however not able to clearly identify defects.
This can be due to direct waves travelling in the water between
the two sensors or by the fact that the refracted waves (tube
waves) from the PVC tube prevails in respect to the real stiffness
differences in the confining concrete. However some more
analysis of the signals seems, even with less clear evidence than
in the previous testing setup, to reveal the possibility to identify
the position of the defects in cementation.
In conclusion, preliminary test presented underline the
potentiality of the ultrasonic tests in cementation defect
identification for BHE monitoring. Technical problems (mainly
tube diameter and signal coupling in single hole tests) have
however to be solved for an application of the technique to real
case histories. At the same time more sophisticated signal
interpretation techniques could lead to a clearer identification of
defects. Anyway, this technique open a new vision on the field of
environmental certification, permitting to highlight situation in
which borehole heat exchangers can be a possible source of
pollution or, simply, can put in connection different aquifers due
to lack or poor cementation of the space between pipes and
ground.
376
Fig. 1 – Cross Hole test defect identification in comparison to experimental pile:
grey zone means good cementation.
REFERENCES
CARELLA R. & SOMMARUGA C. (2000) - Geothermal space And
agribusiness heating in Italy. Proc. World Geothermal
Congress, Kyushu - Tohoku, Japan, 28/5 - 10/6, 117-122.
LIKINS G. E., RAUSCHE F., WEBSTER K. & KLESNEY A., (2007) -
Defect Analysis for CSL Testing. Geotechnical Special
Publication No. 158 - Contemporary Issues in Deep
Foundations; Proceedings from Geo-Denver 2007 New Peaks
in Geotechnics: Denver, CO. (CD-ROM).
RAUSCHE F. (2004) - Non-Destructive Evaluation Of Deep
Foundations. Proceedings of the Fifth International
Conference on Case Histories in Geotechnical Engineering:
New York, NY. (CD-ROM).
SIGNORELLI S., BASSETTI S., PAHUD D. & KOHL T (2007) -
Numerical evaluation of thermal response tests. Geothermics
36, 141–166.

The Campi Flegrei Deep Drilling Project: from volcanic risk
mitigation to geothermal research
Key words: Campi Flegrei, risk mitigation, geothermal research.
Campi Flegrei caldera is a good example of the most
explosive volcanism on the Earth, a potential source of global
catastrophes. Alike several similar volcanic areas (Yellowstone
and Long Valley, USA; Santorini, Greece; Iwo Jima, Japan, etc.)
its volcanic activity is dominated by physical mechanisms
involving the strict interaction between shallow magma sources
and geothermal systems. Furthermore, just like similar areas, it
should be characterised by very large shallow magma chambers,
filled by residual magma left after the ignimbritic, caldera
forming eruptions. However, neither the physical mechanisms of
magma-water interaction, nor the evidence for such large magma
chamber, are actually clear enough to be used for detailed
volcanological interpretation and eruption forecast.
Campi Flegrei caldera, with respect to many similar area, has
the advantage that the most interesting structural details and main
volcanic features appear located at shallower depth, making it a
natural candidate for a deep drilling project aimed to understand
the volcanic structure of calderas.
The CFDDP project aims to understand, for the first time in a
direct way by deep drilling, the location and rehology of large
residual magma chambers and the mechanisms of interaction
between magma and aquifer systems to generate eruptions and
unrests.
Furthermore, the direct, detailed study of the whole
geothermal system will allow to extract crucial information about
the geothermal potential and about the most fruitful strategies for
geothermal energy exploitation in such a densely urbanised area.
Just like the Icelandic Deep Drilling Project, in addition, Campi
Flegrei deep hole will reach temperatures overcoming 500°C, in a
rock sustem were supercritical fluids are expected. Supercritical
fluids exploitation can be considered the most powerful
geothermal energy of the future, in hot volcanic areas.
CFDDP is then also aimed to raise new interest for
geothermal energy exploitation, which, mainly in Italy, can
become the real clean and sustainable alternative to fossile fuels.
_________________________________________________
(*) Istituto Nazionale di Geofisica e Vulcanologia, sezione di Napoli
Osservatorio Vesuviano
giuseppe.denatale@ov.ingv.it, claudia.troise@ov.ingv.it
GIUSEPPE DE NATALE (*) & CLAUDIA TROISE (*)
377
SESSIONE 11

SESSIONE 11
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SESSIONE 11

SESSIONE 11
Keywords: Geothermal district heating, Paris basin, sustainable
management.
The Paris Basin geothermal district heating (GDH) scheme
stands as the second world largest of its kind, after the city of
Reykjavik, with a total installed capacity and yearly heat supplies
(heating and sanitary hot water – SHW) amounting to 220 MWt
and 1100 GWht respectively, serving ca. 150000 equivalent
dwellings (each ca 200 m 3 in volume) from 34 well doublets.
The first attempt to exploit the hot waters hosted in the
Dogger carbonate formation (mid Jurassic) dates back to year
1962, at Carrieres-sur-Seine west of Paris. The well, despite a
high productivity, was abandoned as a result of a highly saline
brine, incompatible with the disposal of the waste water in the
natural medium (a surface stream). This led a private operator to
commission, in 1969, the first field implementation of the
geothermal doublet concept of heat mining, combining a
production well and an injection well pumping the heat depleted
brine into the source reservoir.
The doublet (two deviated, 7" cased, wells) produced in self
flowing mode was put online in 1971, on the henceforth Melun
l'Almont emblematic site, South of Paris, to supply heat to a
nearby social dwelling compound. It enabled, incidentally, to
design new, titane alloyed, plate heat exchangers, able to cope
with a hostile fluid environment, a corrosive, slightly acid (pH =
6), saline (30 g/l eq. NaCl) and hot (74°C) brine. The system
since then has been operating satisfactorily, the doublet moving
in the meantime towards a triplet array including two injector and
one new, innovative, anti corrosion production well combining
steel casings and freely suspended, non cemented, fiberglass
liners. Noteworthy is that this pioneer achievement was
completed irrespective of any energy price crisis nor public
subsidising whatsoever. Regarded at the time as a technological,
fairly exotic, curiosity the concept has been extended later to the
whole Paris Basin GDH systems.
The sharp energy prices rises in the aftermath of the 1970s oil
shocks led the French authorities to promote, among other
renewable energy sources, low grade geothermal heat as base
_________________________________________________
(*) GPC IP - PARIS NORD 2, m.antics@geoproduction.fr
Sustainable management of the Dogger
geothermal Reservoir - Paris Basin
PIERRE UNGEMACH (*) & MIKLOS ANTICS (*)
380
load to district heating grids and other space heating systems.
This commitment has been concluded by the development, in
the Paris Basin alone, of 54 GDH doublets of which 34 still
serviced to date, indeed a satisfactory score given it addressed a
new energy development route and a highly competitive energy
market. This success story undoubtedly benefited from the
convergence of three main driving stimuli (i) evidence of a
dependable geothermal reservoir (Dogger limestones) of regional
extent, reliably assessed thanks to former hydrocarbon
exploration and development campaigns (over 3000 wells drilled
and 5000 km processed seismic lines); (ii) a strong, voluntarist,
commitment of the State in favour of alternative energy sources
and accompanying incentives (mining risk coverage, mutual
insurance(sinking)-fund mitigating exploitation hazards, financial
support to district heating grids and focused R,D&D
programmes), and, last but not least, (iii) the presence above the
geothermal resource of large social dwelling units,eligible to
district heating, numerous throughout the Paris suburbs.
In spite of this strong backing, geothermal development did
not avoid contagion from infantile diseases inherent to the
implementation of new technologies as evidenced by several
symptoms, chiefly.
- structural : lack of expertise from operators (mainly of the
public sector) in managing industrial installations and energy
processes implying a strong mining impact ;
- technical : (i) loose mastering in operating heating grids,
under a retrofit rationale combining several base load and backup/relief
energy sources and fuels, (ii) repeated failures of
submersible pump sets, and (iii) above all, devastating corrosion
of well casing, well heads and equipments caused by a
thermochemically hostile fluid ;
- administrative and managerial : imprecise definition of
duties and obligations of involved parties (operators, engineering
bureaus, heating companies, consults…) and of relevant
exploitation/service contracts, inefficient marketing and
negotiations of heat sales and subscription contracts ;
- economic and financial : severe competition from
conventional fossil fuels (heavy fuel oil and natural gas, the
leading competitor) penalising sales and revenues, persistent
depleted energy prices further to the second oil shock, adding to a
debt nearing 85 % of total investment (CAPEX) costs in a capital
intensive (5 to 8 M , now approaching 15 to 18 M ), low equity,
high interest rates (12 to 16 % in the late 1980's) context. This

clearly placed most geothermal operations in a typically third
world position.
With time and experience, structural and technical problems
could be overcome via systematic and standardised fluid and
equipment monitoring and logging inspection protocols,
innovative well workover and chemical inhibition procedures
aimed at restoring well; performance and preventing
corrosion/scaling damage, the latter supported by the State
through pertinent R&D programme and funding.
Simultaneously (early to mid 1990's) administrative, State
inspired, measures enabled to reduce the debt charge,
renegotiated by a spreading out of debt annuity repayments,
interest rate cuts and grace period extensions. Tax deductions
were applied to geothermal operators, regarded therefore as
energy producers, the most significant one addressing the VAT
rate set at 5,5 % instead of the former 19.4 %. Simultaneously,
improved technical administrative and financial management of
GDH grids could be noticed among most geothermal players.
Hence, the revival of a technology, once endangered to a
point its abandonment had been seriously contemplated, could be
achieved at the expense through of the shut in/cementing of 22
doublets i.e. ca one third of the initial load and a subsequent loss
in heat supplies as displayed in the recorded and projected figures
listed below.
Target Achived Forecast
(1985) 1990 2008 2012 2020
Operating doublets 54 43 34 37 45
Total installed
capacity (MWt)
360 260 220 250 350
Produced heat
(GWht/yr)
2.000 1.455 1200 1300 1.600
Unit capacity
(MWt)
6.5 6.0 6.5 6.7 7.5
Unit yield
(MWht/yr)
36000 33800 35000 35000 35000
Artificial lift wells 48 36 27 30 40
Self-flowing wells 6 7 7 7 5
Since the late 1990's/early 2000's GDH in the Paris suburbia
accessed to adult age and technology and know matured to a
stage present heat extraction is mastered, heat marketing safely
managed and sustainable development issues challenged. It has
also gained wider social acceptance, as a result of growing clean
air concerns and reduction of GDH emissions, an awareness
favourably echoed by the media.
Having recalled these milestones and premises the present
paper will highlight the major technical accomplishments, namely
(i) new well completion designs associating steel casing
and fiber glass lining, a material response to corrosion
shortcomings,
381
(ii) abatement of thermochemical, corrosion/scaling,
damage via custom designed inhibitor formulations and
continuous, coiled tubing type, downhole chemical injection
lines,
(iii) specific damaged well cleaning (sliding nozzle jetter)
tools and procedures,
(iv) soft acidizing stimulation techniques,
(v) tracer injection protocols, replacing costly packer leaf
off tests, as a means for checking well integrity,
(vi) waste disposal management via a mobile processing
(degassing, solids removal, fluid cooling) line, substituted to the
previous refuse pit practice, best suited to well workovers located
in sensitive, densely populated, urban environments,
(vii) implementation of representative multilayered
geothermal reservoirs and stacked, sandwiched equivalent
structures and of simulation tools modelling close to actual heat
and mass transfer processes,
(viii) design of multi-well, doublet/triplet/doublet, arrays
extending, on the same site, system life from the casual 25 year
thermal life span to 75 year reservoir longevities. meeting the
requirements of key sustainable reservoir management issues,
(ix) Dogger Data Base. Its architecture (joint BRGM-
CFG-GPC IP design) has been conceived (and is actually
practiced) as a dynamic interactive reservoir management tool,
(x) last but not least, design and implementation of
geothermal district heating & cooling grids and combined
shallow aquifer heat and cold storage/deep aquifer heatingpreheating.
SESSIONE 11

SESSIONE 11
382

SESSIONE 12
Processi e meccanismi di esumazione delle catene
montuose
CONVENERS
Chiara Montomoli (Università di Pisa)
Eduardo Garzanti (Università di Milano - Bicocca)
383
SESSIONE 12

SESSIONE 12
An example of two stages exhumation of a thrust and fold belt
from the thermochronology of Western Carpathians
Key words: Carpathians, erosion, exhumation,
thermochronology.
The Tertiary-Quaternary evolution of the Carpathian orogen
is controlled by different geodynamic processes such as SW- to
W-dipping subduction, slab retreat, and back-arc extension.
Therefore, the response of the chain at shallow crustal levels was
marked by different episodes of thrusting and extension that gave
rise to the construction and following disruption of the orogenic
wedge. Rocks were then moved to the surface through erosional
or tectonic exhumation processes according to the prevailing
tectonic regime. Hence, thermochronological data could provide
key information to unravel timing of the geodynamic evolution.
In this study we use apatite fission-track (AFT) and (U-Th)/He
(AHe) analysis across the Western Outer Carpathians where
thrusting is commonly interpreted to have ceased at about 11 Ma
but being progressively younger towards the east (TOKARSKI.,
1978). This eastward trend is followed by formation of
“intramontane basins” (ROYDEN, 1988) and by the development
of extensional features (MAZZOLI et alii, 2010)
The overall distribution of AFT ages shows that exhumation
of the western Outer Carpathians occurred between 7.0 and 26.3
Ma. Although clear trends are not visible (due also to the limited
amount of data in some areas), it appears that younger ages are
confined to the eastern region, with no differences between
Magura, Dukla and Silesian tectonic units.
AHe ages span between 6.16 and 20.56 Ma: in the eastern
sector AHe data are comparable to AFT ones, dating back to the
Late Miocene, whereas in the western and central sector they are
referred to Early to Middle Miocene, being 2 to 15 Ma older than
AFT ones.
Exhumation of the chain, as inferred from
thermochronological analysis integrated with structural data
_________________________
(*) Department of Geosciences, University of Padova,
benedetta.andreucci@studenti.unipd.it
(**) Polish Geological Institute, Cracow (Poland)
(°) Department of Earth Sciences, University of Naples
(°°) Institute of Geophysics, Polish Academy of Science, Warsaw (Poland),
BENEDETTA ANDREUCCI (*), LESZEK JANKOWSKI (**), STEFANO MAZZOLI (°),
RAFAL SZANIAWSKI (°°) &
MASSIMILIANO ZATTIN (*)
384
(MAZZOLI et alii, 2010) appears therefore characterized by two
distinct periods, separated by a period of quiescence. Exhumation
of the inner (DANISIK et alii, 2010) and easternmost part of
Western Carpathians occurred in the Late Miocene, whereas the
central and western region yield an Early Miocene signal.
Since the thermochronological ages referred to the central and
western sectors are coeval with thrusting and scarcely
homogeneous, and since they show a variable, but generally high,
time gap between AFT and AHe, the first exhumation episode
appears to be concurrent with thrusting and dominated by
erosional processes.
The ages from the inner and eastern sector are instead
younger and highly homogeneous, with a small span between
AFT and AHe ages, and they post-date thrusting. This points out
a relatively fast exhumation process, that occurred after
termination of accretion-related shortening. This second
exhumation phase appears to be driven by tectonic processes, as
pointed out by the presence of normal faulting and detachment
faults well inside the Outer Carpathians (MAZZOLI et alii, 2010),
and it matches well with the timing of the Late Sarmatian-Early
Pannonian extensional phase.
We suggest that recent (

NEMCOK M., POSPISIL L., LEXA J. & DONELICK R.A. (1998) -
Tertiary subduction and slab break-off model of the
Carpathian-Pannonian region. Tectonophysics, 295, 307–
340.
ROYDEN L.H. (1988) - Late Cenozoic tectonics of the Pannonian
basin system, The Pannonian Basin. In: L.H. Royden and F.
Horváth (Eds.) - Am. Assoc. Petr. Geol. Mem., 45, 27–48.
TOKARSKI A.K. (1978) - On Quaternary fault and jointing in
Nowy Sacz Basin, Outer Western Carpathians, Ann. Soc.
Geol. Pol., 48, 509–516.
385
SESSIONE 12

SESSIONE 12
Key words: Mantle, geodynamics, thermal uplift.
Thermobarometry of spinel peridotites collected in northern
Victoria Land in Cenozoic basalts of the Mt Melbourne Volcanic
Province, reveals warming of local lithospheric mantle, marked
by a shift of geothermal gradient from 0.5°C/km to ~3°C/km
during the development of Cenozoic magmatism related to the
opening of the Ross Sea rift system.
We suggest that a significant uplift fraction of the rift shoulder
on the West Antarctic margin is due to the change in olivine
molar volume induced by mantle heating.
The heat source is provided by enhancement of
asthenospheric convection induced by an “edge effect” in the
mantle circulation, following the opening phase of the Ross Sea.
Besides explaining the asymmetric uplift of the rift shoulder
corresponding to the Transantarctic Mountains, this mechanism
satisfactorily accounts for the time scale (~10 Ma) and most of
total uplift (~3000 m) of the western border of the Ross Sea in
northern Victoria Land. P-T history recorded by spinel peridotites
of northern Victoria Land indicates that the lithospheric mantle of
the area suffered a local heating that shifted the thermal gradient
from values typical of a dynamic rift (0.5°C/km) to a much higher
value (~3°C/km) due to the onset of an edge-driven convection
determined by the lithospheric step between the East Antarctic
craton and the thinned crust of the Ross Sea.
In this model the change of thermal gradient drives the
increase of molar volume of upper mantle phases inducing a
regional uplift.
This scheme may be conveniently applied in a variety of
geodynamic contests different from the classical application to
the evaluation of the increase of see floor depth with the distance
from the ridge and may explain the local uplift in regions where a
plume (Afar, West Eifel, Massif Central), a slab window
(Patagonia) or an edge effect (South Australia) switch the
regional gradient to an higher value.
_________________________
Cenozoic thermal evolution of lithospheric mantle
in northern Victoria Land (Antarctica):
the Uplift of the Transantarctic Mountains
(*) Dipartimento di Scienze della Terra, Università degli Studi di Pisa,
armienti@dst.unipi.it
PIETRO ARMIENTI (*) & CRISTINA PERINELLI (*)
386

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388

Lithological discrimination in collisional belt through Remote
Sensing: a case study (Buraburi granite; Western Nepal, Himalayas)
Key words: ASTER, exhumation, granite, Himalaya, PCA,
Remote Sensing.
INTRODUCTION
A new granitoid body (Buraburi Granite-BG) was discovered,
mapped and sampled in Dolpo region (western Nepal,
Himalayas) starting from remote sensing analysis on ASTER
satellite data. We started from fragmented bibliographic
observations about the presence of leucogranite rocks with very
uncertain boundaries. So far, these rocks have been considered as
the southern portion of the bigger Mugu granite (FUCHS, 1973-
74).
The aim of the study was to define the most suitable
methodologies for ASTER data preprocessing and analysis in
order to enhance peraluminous granitoid rocks in extreme terrain,
both vegetated and roughly profiled and to provide a geological
map of the main body and county rocks.
The work-flow started from image raw data pre-processing
and continued by comparing satellite, field and laboratory data.
Results from Density-sliced and false color composite images of
Band Ratio, Relative Absorption Deep and Principal Component
Analysis (PCA) allowed us to generate a geological map that
highlights the BG shape and the surrounding tectonic units. This
provides evidence that BG is an isolated body not connected with
the larger Mugu granite as previously believed.
The integration of Remote Sensing analysis and field
observations, point out both the intrusive nature of the contact
between BG and Tibetan Sedimentary Sequence (TSS) and the
presence in the BG basal part of a well developed foliation
parallel to the regional one. This suggest a relation between the
South Tibetan Detatchment System (STDS) activity and granite
emplacement.
These findings have also substantial geological implications
_________________________
(*) Dipartimento di Geoscienze - Università degli Studi di Padova,
luca.bertoldi@unipd.it
(**) Dipartimento di Scienze della Terra – Università di Pisa,
carosi@dst.unipi.it
Research financed by CARIPARO and PRIN (national coordinator: Prof. E.
Garzanti)
LUCA BERTOLDI (*), MATTEO MASSIRONI (*), DARIO VISONÀ (*),
RODOLFO CAROSI (**) & CHIARA MONTOMOLI (**)
389
for the time-extent and even existence of the assumed extrusion
and/or channel flow mechanisms which would have driven the
exhumation of the Higher Himalayan Crystalline HHC in this
area.
METODOLOGY
In order to fully map the Early Miocene leucogranite BG,
located along the contact between Higher Himalayan Crystalline
HHC and TSS and to analyze its relationships with the hostrocks,
we performed a Remote Sensing analysis on ASTER data.
ASTER is a multispectral sensor on board of the Earth
Observation System (EOS) Terra satellite launched in 1999.
ASTER provides three bands in the visible to near infrared
(VNIR) at a resolution of 15m/pixel, six bands in the short-wave
infrared (SWIR) at 30m/pixel and five bands in the thermal
infrared (TIR) at 90m/pixel (ABRAMS et alii, 2002).
In this paper, we briefly discuss the Principal Component
Analysis of the six SWIR bands, with which was obtained the
best lithological discrimination. Results point out the possibility
that the lower TSS (e.g. North Col Formation), was intruded by
granite dykes and slightly metamorphosed in greenscist facies;
green and yellow pixels (high PC4) indicate mainly Calcite
presence, that is related to two or more formations belonging to
the TSS (e.g. Dhaulagiri Limestone), purple pixels highlight the
presence of high-grade metamorphic rocks (HHC).
CONCLUSIONS
The processing of ASTER data for lithological mapping and
discrimination on areas with high relief energy, abundantly
covered by vegetation, snow-ice, water bodies and clouds, led to
satisfactory results. Using masking and band operation/statistic
(PCA) techniques gazed at highlight leucogranites outcrops, we
were able to map the boundary of a 110 Km 2 granitoid body and
the surrounding host rocks (Fig. 1) (BERTOLDI et alii, 2009).
Despite some authors (SEARLE &GODIN, 2003; LAW et alii,
2006) concluded that Oligo-Miocene leucogranites are restricted
to the footwall of the brittle portion of the South Tibetan
Detachment System (STDS), the contact shape, as observed both
in the ASTER image and in the field (CAROSI et alii, 2009)
SESSIONE 12

SESSIONE 12
Fig. 1 – Left: RGB false color composite of 6,4,2 PCA bands regarding the 6th ASTER SWIR band. Image interpretation and field controls allow the following
conclusion: red pixels (high PC6) are referred to Muscovite presences related to granites litologies (e.g. Buraburi Granite); blue and cyan pixels (high PC3)
indicate Chlorite and Calcite presence, related to the lower TSS (e.g. North Col Formation), intruded by granite dykes and slightly metamorphosed in greenscist
facies; green and yellow pixels (high PC4) indicate mainly Calcite presence, that is related to two or more formations belonging to the TSS (e.g. Dhaulagiri
Limestone), purple pixels highlight the presence of high-grade rocks (HHC). Right: geological maps after Remote Sensing analysis integrated with ground
study.
between the BG and the TSS, evidences intrusive relations. This
suggests a complex tectonic evolution and kinematic relationships
between pluton emplacement and STDS activity. In particular, we
corroborated the relation between leucogranite emplacement and
the final stage of detachment fault systems, in a continental
collision setting. First results point out that BG emplaced mainly
post- STDS activity (CAROSI et alii, 2009).
REFERENCES
ABRAMS M., HOOK S. & RAMACHANDRAN B L. (2002) - ASTER
User Handbook, v2: Advanced Spaceborne Thermal Emission
and Reflection Radiometer. Jet Propulsion Lab., 135 pp.
BERTOLDI L.,MASSIRONI M., VISONÀ D., CAROSI R., MONTOMOLI
C. & FRASSI C. (2009) - How the Buraburi pluton (Dolpo
region-Western Nepal) was discovered through remote
sensing analysis and ground truth. Abstract: The 5th
International Symposium on Tibetan Plateau/The 24 th
Himalaya-Karakorum-Tibet Workshop, 11-14 August, 2009,
Beijing, China.
390
CAROSI R., MONTOMOLI C., RUBATTO D., BERTOLDI L., FRASSI
C., VISONÀ D. & PERTUSATI P.C. (2009) - Along strike
variation of exhumation mechanism of the Higher Himalayan
Crystallines: Insight from Western Nepal. Abstract: The 5th
International Symposium on Tibetan Plateau/The 24 th
Himalaya-Karakorum-Tibet Workshop, 11-14 August, 2009,
Beijing, China.
FUCHS G. (1973-74) – On the geology of the Karnali and Dolpo
Regions,West Nepal. On Mitteilungen der Geologischen
Gesellschaft in Wien, 66-67.
LAW R.D., SEARLE M.P. & GODIN L. (2006) - Channel flow,
ductile extrusion and exhumation in continental collision
zones.. Geol. Soc. SP., London, 268, 620 pp.
SEARLE M.P. & GODIN L. (2003) - The South Tibetan detachment
and the Manaslu leucogranite: A structural reinterpretation
and restoration of the Annapurna-Manaslu Himalaya, Nepal.
J. Geol., 111, 505-523.

From normal to strike-slip faults during exhumation processes: the
case of the eastern Elba Island (inner Northern Apennines)
Key words: Elba Island, exhumation, inner Northern Apennines,
strike-slip tectonics.
In the post-collisional extensional tectonic framework, the
exhumation of deepest tectonic units is commonly related to the
activity of extensional detachment faults affecting the previously
overthickened continental crust.
From the Early-Middle Miocene, the inner Northern
Apennines have been affecting by extensional tectonics. One of
the best exposure outcrop of a regional extensional detachment
fault (i.e., the Zuccale fault) is largely exposed in the Elba Island
(Tuscan Archipelago). Geometry and kinematics of the Zuccale
Fault were investigated by many authors in the last decades.
The Zuccale Fault is associated with the exhumation of the
western Elba sub-volcanic magmatic system and of the Monte
Capanne granodiorite. Sub-volcanic rocks and granodiorite
emplaced in a time-span ranging from about 8-6.7Ma. A younger
magmatic body is located in eastern Elba, and referred to as the
Porto Azzurro monzogranite, dated at 5.4Ma. Both the western
and eastern magmatic complexes were dissected by the Zuccale
normal fault. Thus, its activity is constrained at least during Late
Messinian. The horizontal displacement determined by the
Zuccale normal fault is estimated in about 6km. The fault activity
produced the superimposition of the Ligurian Units over the
Tuscan metamorphic “basement” represented by the Verrucano
Group (Trias) and the Palaeozoic rocks.
In the eastern side of the Elba Island two sets of strike-slip
faults cross-cut the Zuccale normal fault: the first set, N120°
oriented on average, is characterized by a left-lateral movement
with a minor normal component; Riedel structures, striae and
slickensides are the most common kinematic indicators. A
widespread tourmaline mineralization was associated with these
structures. The last set of strike-slip faults displays a right-lateral
movement and its trend is almost N170°. Iron-hydroxides veins
characterize the fault zones.
The two strike-slip faulting events were active after the Late
Messinian. Fault rocks and fabrics suggest that these developed at
shallower structural levels with respect to the Zuccale Fault
_________________________
(*) Dipartimento di Scienze della Terra, Università di Siena,
brogiandrea@unisi.it
(**) Dipartimento di Geofisica e Geologia, Università di Bari,
d.liotta@geo.uniba.it
ANDREA BROGI (*) & DOMENICO LIOTTA (**)
391
level. This implies changes in the local stress field at the
boundary Late Messinian - Early Pliocene.
We discuss two different interpretations: a) the exhumation
process determined a significant decrease of the vertical load, and
therefore, the switch of the s 1 orientation; b) the study area was
affected by a dominant transcurrent shear zone, related to transfer
zones in the framework of the Pliocene extensional tectonics
which affected the inner Northern Apennines.
In southern Tuscany, available data indicate that transcurrent
tectonics is localized in shear zones where magmatism, volcanism
and geothermal fluid flow is enhanced. These shear zones are
presently explained as transfer zones in the framework of the
Pliocene-Present extensional tectonics. In this context, we
interpret the Elba strike-slip faults as features of the Pliocene
tectonic evolution of the Northern Tyrrhenian Basin.
SESSIONE 12

SESSIONE 12
Mg-carpholite bearing quartz veins and HP-LT mineralogical
assemblages in the exhumed siliciclastic units of the Monticiano-
Roccastrada Ridge (inner Northern Apennines)
Key words: Exhumation, HP-LT metamorphism, inner Northern
Apennines, poliphased tectonics, southern Tuscany.
In this presentation we report new data on the tectonometamorphic
evolution of the siliciclastic succession (Triassic
Verrucano Group) exposed in the northern part of the
Monticiano-Roccastrada Ridge (southern Tuscany), exhumed
during the Middle-Late Miocene extensional tectonics which
affected the inner Northern Apennines.
The siliciclastic succession consists of Early-Middle Triassic
quartz metaconglomerate, metasandstone, metasiltite and phyllite
affected by contractional structures mainly ascribed to two
deformation events (D1 and D2) related to the Northern
Apennines Tertiary collisional event.
During the first deformation event (D1), reverse faults and
isoclinal folds (F1) developed. F1 folds consist of mainly N–S
and/or NE–SW striking meso- to map-scale structures. An axial
planar tectonic foliation (S1), consisting of a pervasive
schistosity, mainly developed in the fine grained lithotypes. The
successive deformation event (D2) was typified by mesoscopic to
map-scale asymmetric folds (F2) and an associated, locally
pervasive, crenulation-cleavage (S2). F2 fold axes are mainly
NNE–SSW-oriented, frequently exhibit recumbent attitude and
overturned shorter limbs. S2 is very pervasive in the metapelites
but results discontinuous in the metasandstones and
metaconglomerates.
Mg-carpholite bearing quartz veins, centimeter to decimeter in
thickness, growth during the D1 deformation event and
contemporaneously with the development of the S1 composite
tectonic foliation. Such evidences, coupled with the dynamic
crystallization of muscovite + pyrophillite + chlorite + chloritoid
+ quartz mineralogical assemblage on the S1 tectonic foliation,
support for HP-LT metamorphic condition (P ~ 1Gpa, T=350-
400°C) which took place during the D1 deformation event.
Cookeite, pyrophyllite, kaolinite, sudoite may replace
carpholite and they represent a retrograde assemblage probably
formed during the D2 deformation event under lower P condition
_________________________
(*) Dipartimento di Scienze della Terra, Università di Siena,
brogiandrea@unisi.it, giorgettig@unisi.it
ANDREA BROGI (*), GIOVANNA GIORGETTI (*) & RENZO REGOLI (*)
392
and still relatively high temperature.
A comparable tectono-metamorphic setting has been described,
by many authors, for the same succession exposed in the Monte
Argentario, Monte Leoni, and Tuscan Archipelago (Giglio and
Gorgona Islands).
In this view, the new data reported in this presentation indicate
that HP-LT metamorphism characterize also the northern part of
the Monticiano-Roccastrada Ridge, in the Monticiano area. This
supports for a widespread HP-LT metamorphism affecting the
whole inner part of the Northern Apennines during the
development of the orogenic built, mainly ascribed to the D1
deformation event. The D2 deformation event developed in a
shallower structural level during the uplift of the Northern
Apennines. The HP-LT metamorphic units are presently exposed
in the Tuscan Archipelago and southern Tuscany due to their
exhumation mainly produced by the activity of low-angle normal
faults.

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The South Tibetan Detachment on the Northern slope of Mt. Cho
Oyu (Southern Tibet, China)
RODOLFO CAROSI (*), CHIARA MONTOMOLI (*) & FABRIZIO BARTOLI (**)
Key words: Greater Himalayan Sequence, Himalayas, Lesser
Himalaya, leucogranites, Main Central Thrust, Mt. Cho
Oyu, North Col Formation, South Tibetan Detachment
System, Tibetan Sedimentary Sequence.
The Higher Himalayas close to the Nepal-Tibet boundary
attracted the attention of the researchers since the eighties being
the place where the South Tibetan Detachment System crops
out (CABY et alii, 1983; BURG et alii 1984; BURCHFIEL et alii
1992; CAROSI et alii 1998; SEARLE, 1999; SEARLE et alii
2003). The South Tibetan Detachment System (STDS) is a
system of normal sense shear zone and normal faults with a topto–the
NE sense of displacement putting into contact the
Fig. 2 – Cho Oyu north face (Tibetan side) from the Cho You advanced
base camp. The STD (top-to-the North sense of shear: white arrow) is located
to the top of the Cho Oyu summit: above there is the North Col Formation or
Everest Series and below there are the high-grade schists and gneisses of the
Rongbuk Formation (dark rocks) intruded by la network of leucogranite
dykes and sills (Photo by F. Bartoli).
bottom of the nearly unmetamorphosed Tibetan Sedimentary
Sequence (TSS) with the underlying high-grade gneiss and
granites of the Greater Himalayan Sequence.
CAROSI et alii (1998) recognized in the Mt. Everest area the
occurrence of more complex architecture of the STDS being
constituted by two main “faults”:
_________________________
(*) Dipartimento di Scienze della Terra, Pisa, e-mail: carosi@dst.unipi.it;
montomoli@dst.unipi.it
(**) Corso di Laurea in scienze Geologiche, Università di Pisa,
fabriziobartoli@hotmail.it
395
an upper brittle fault getting into contact the fossiliferous
Ordovician limestone of the TSS with the underlying Everest
Schists or North Col Formation (Qomolangma detachment;
BURCHFIEL et alii 1992; SEARLE et alii 1999);
a lower ductile shear zone, with a thickness > 1km, getting
into contact the overlying Everest schists or North Col
Formation with the high-grade sillimanite and biotite-bearing
gneiss of the upper part of the Greater Himalayan Sequence
(Lhotse Detachment; SEARLE et alii 1999, 2003).
The contemporaneous activity of the MCT and STDS
between 23 and 17 Ma (GODIN et alii 2006, with references)
allowed to propose some mechanisms of exhumation of the
Higher Himalayan Crystallines or Greater Himalayan Sequence
(GHS) such as extrusion and channel flow. Large volume of
granites were intruded in its upper portion, below the South
Tibetan Detachment (BURCHFIEL et alii 1992; SEARLE, 1999;
BEAUMONT et alii 2001; GRUJIC, 2006; GODIN et alii, 2006
with references).
The STD cross cuts the summits of some of the eight
thousands mountains such as the Mt. Everest and the Mt. Cho
Oyu so that a detailed map of the faults is difficult (SAKAI et
alii, 2005).
In a tentative of climbing the summit of the Mt. Cho Oyu
during the spring 2010 F. Bartoli reached the uppermost
portion of the Cho Oyu and collected some rock samples below
the STD.
The STD dips gently to the North and cross-cuts the summit
of the Mt. Cho Oyu (8200 m) at an altitude of nearly 7900-
8000 m (Fig. 1) and the summit of Mt. Gyachung Kang (7922
m). The lower STD crops out well above 6500 m so that the
higher part of the summit of Mt. Cho Oyu is made by few
hundred meters of low-grade metamorphics of the North Col
Formation. The metamorphic rocks below the lower STD are
sillimanite- and biotite-bearing schists of the Rongbuk
formation intruded by a network of Higher Himalayan
leucogranites dykes and sills. They vary from deformed, with
an attitude nearly parallel to the foliation in the gneiss to
poorly-deformed up to undeformed cross-cutting the foliation at
an high-angle. They are well-observable on the south face of
Cho-Oyu and Gyachung Kang as well as on the northern slope
of the Gyachung Kang in southern Tibet.
Direct observation in the field and rock samples as well as
the use of close up photographs from the Camp 1 (6400 m) and
Camp 2 (7200 m) allowed to better map the STD on the
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northern slope of Mt. Cho Oyu.
REFERENCES
BEAUMONT C., JAMIESON R.A., NGUYEN M.H. & LEE B. (2001)
- Himalayan tectonics explained by extrusion of a lowviscosity
crustal channel coupled to focused surface
denudation. Nature, 414, 738–742.
BURCHFIEL B.C., CHEN Z., HODEGES K, LIU S., ROYDEN L.H.,
CHANGRONG D. & XU L. (1992) - The South Tibetan
Detachment System, Himalayan Orogen: extension K Y.. V.
contemporaneous with and parallel to shortening in a
collisional mountain belt. Geol. Soc. Am. SP., 269, 41.
BURG J.P., BRUNEL M., GAPAIS D., CHEN G.M. & LIU G.H.
(1984) - Deformation of leucogranites of the crystalline
main central thrust sheet in southern Tibet (China). J.
Struct. Geol., 6, 535-542.
CABY R., PECHER A. & LE FORT P. (1983) - Le grand
chevauchement central himalayen: nouvelles données sur le
métamorphisme inverse à la base de la Dalle du Tibet. Rev.
Géol. Dyn. Géog., 24, 89-100.
CAROSI R., LOMBARDO B., MOLLI G., MUSUMECI G. &
PERTUSATI P.C. (1998) - The South Tibetan Detachment
System in the Rongbuk valley, Everest region. Deformation
features and geological implications. J. Asian Earth Sci.,
16, 299-311.
GODIN L., GRUIJC D., LAW R.D. & SEARLE M.P. (2006) -
Channel flow, ductile extrusion and exhumation in
continental collision zones: an introduction. Geol. Soc. SP.,
268, 1-23.
GRUIJC D. (2006) - Channel flow and continental collision
tectonics: an overview. In:R.D. Law, M.P. Searle and L.
Godin (Eds.) - Channel flow, Extrusion, and Exhumation in
Continental Collision Zones. Geol. Soc. SP., 268, 25-37.
SAKAI H., SAWADA M., TAKIGAMI Y., ORIHASHI Y., DANHARA
T., IWANO H., KUWAHARA Y., DONG QI, CAI H. & LI J.
(2005) - Geology of the summit limestone of Mount
Qomolangma (Everest) and cooling history of the Yellow
Band under the Qomolangma detachment.Isl. Arc,14, 297-
310.
SEARLE M.P. (1999) - Extensional and compressional faults in
the Everest-Lhotse Massif, Khumbu Himalaya, Nepal. J.
Geol. Soc. London, 156, 227-240.
SEARLE M.P. & GODIN L. (2003) - The south tibetan
detachment system and the manaslu leucogranite: a
structural reinterpretation and restoration of the
Annapurna-Manaslu Himalaya, Nepal. J. Geol., 111, 505-
524.
396

Geological field trip in the Kaligandaki Valley (Central Nepal) by
the Italian Group of Himalayan Geology
RODOLFO CAROSI (*), CHIARA MONTOMOLI (*), SANTA MAN RAI (**),
ANGELO BORSANI (*) & SALVATORE IACCARINO (*)
Key words: Collisional belts, Himalayas, Greater Himalayan
Sequence, Italian Group of Himalayan Geology, Lesser
Himalaya, Main Central Thrust, South Tibetan Detachment
System, Tibetan Sedimentary Sequence.
INTRODUCTION
The Himalayan belt has been regarded as the classical
example of collisional orogen caused by a continent-continent
collision between India and Asia since ~55 Ma. It is characterised
by the impressive continuity over hundreds of kilometres of
tectonic features such as thrusts (e.g. Main Central Thrust: MCT)
and normal faults (e.s. South Tibetan Detachment; STD), as well
as large volumes of high-metamorphic grade rocks and granite
exposed at the surface (Fig. 1).
The Himalayan belt constitutes an invaluable field laboratory
Fig. 1 – Geological sketch map of Himalayas (from S. Guillot website), with
location of study area
to unravel the tectonic and metamorphic evolution of crystalline
units and the mechanisms of exhumation of deep-seated rocks in
orogens.
The contemporaneous activity of the MCT and STD between
23 and 17 Ma (GODIN et alii, 2006 with references) allowed to
propose some mechanisms of exhumation of the Greater
_________________________
(*) Dipartimento di Scienze della Terra, carosi@dst.unipi.it;
montomoli@dst.unipi.it;
(**) Department of Geology, Tri-Chandra Campus, Tribhuvan University,
Kathmandu, Nepal, santamanrai@yahoo.com
397
Himalayan Sequence (GHS) such as extrusion and channel flow.
Large volume of granites were intruded in its upper portion,
below the South Tibetan Detachment (BURCHFIELD et alii, 1992;
SEARLE, 1999; BEAUMONT et alii, 2001; GRUJIC, 2006; GODIN et
alii, 2006 with references).
The nearly E-W trending structures of the belt have been cut
by N-S grabens such as the Thakkola, Dingyè, Yadong grabens
(Fig. 2) starting from Middle Miocene and pointing to an E-W
extension.
Fig. 2 – Pliocene sediments of the Thakkola graben in the Mustang region.
The Kaligandaki valley is regarded as the deepest canyon in
the world, limited to the East by the eight thousands of
Annapurna group ad to the West by the Mt. Dhaulagiri (> 8000
m). This peculiar features allow to directly observe a very thick
crustal section of the belt from the Cretaceous sediments in the
upper portion of the Tibetan Sedimentary Sequence, up to the
Pre-Cambrian Nawakot complex of the Lesser Himalaya to the
south, cross cutting all the crystalline rocks of the Greater
Himalayan Sequence.
The Italian Group of Himalayan Geology is an informal group
of researchers, mainly from the Universities of Pisa, Padua, Milan
and Turin, actively working in the Himalayas since long time in
different scientific areas of Earth Sciences.
Many scientific expeditions have been realized in the last
twenty years allowing to gain the knowledge of most of the
interesting areas of the Himalayan belt from West to East and
Tibet.
During April-May 2010 we have organized a two-weeks
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Fig. 3 – Fold interference between F1 south verging folds (F1 anticline in the
Fang nappe) and F2 north verging folds (Nilgiri antiform and synform) in the
Kaligandaki valley. AD: Annapurna Detachment (South Tibetan
Detachment), Cs: Cambrian–Ordovician Sanctuary Formation; Ca:
Cambrian–Ordovician (Annapurna Formation); O: Ordovician; S: Silurian
(from L. Godin website).
geological field trip in the Kaligandaki valley open to students,
PhD students and other researchers wishing to have a direct
knowledge of the most famous continent-continent collisional
belt. The field leaders (R. Carosi and C. Montomoli) gained the
invaluable help of Prof. Santa Man Rai from the Department of
Geology, Tribhuvan University, Tri-Chandra Campus,
Kathmandu, co-author of a Geological guidebook for Himalayan
trekkers (UPRETI &YOSHIDA, 2005).
A number of 28 people attended successfully the field trip in
the Kaligandaki. When arrived in Kathmandu a day was devoted
to some talks at the Department of Geology with the aim to
introduce to the geology of the Himalayas: R. Carosi introduced
the general features of the belt, C. Montomoli showed the
geological feaures of the main tectonic discontinuities along the
belt, D.Visonà pointed out the role of leucogranites in the belt
and, finally, S. M. Rai introduced to the beautiful geology of the
Kaligandaki.
SUMMARY KALIGANDAKI TRANSECT
Following the geological guidebook by Upreti & Yoshida
(2005) we reached Jomsom from Pokhara by flight and we started
the geological trekking arriving in Kagbeni and Muktinath
villages observing the sedimentary and structural features of the
formations of the Tibetan Sedimentary Sequence from Jurassic to
Early Cretaceous. Coming back from Muktinath to Jomsom and
then to Marpha we observed the sequence from Jurassic to
Middle Paleozoic. From Marpha to Kalopani we reached the
bottom of the sequence observing the more deformed and
metamorphosed Cambrian-Ordovician sequence. All the Tibetan
Sedimentary Sequence has been affected by large-scale NE
398
verging folds, well-observable at large scale on the west face of
Nilgiri (Fig. 3). Few km before Kalopani village we entered in
the high-grade metamorphic rocks and granites of the Greater
Himalayan Sequence crossing the South Tibetan Detachment.
The section shows a complete view of the three units constituting
the GHS up to the beautiful kyanite-bearing gneiss with mylonitic
fabric approaching the MCT zone.
At Kalopani a contractional ductile shear zone in the unit 3
has been observed (VANNAY &HODGES, 1996) and discussed
with the occurrence of other shear zones within the GHS in
Western Nepal (CAROSI et alii, 2007, 2010).
It was possible to discuss in the field the problem of the
definition and localization of the MCT (mainly near Dana
village) by different authors following the shear fabric down to
Mahabar village defining the MCT zone (see Searle et alii, 2008
with references therein). After that we entered in the Kuncha
Formation of the Lesser Himalaya.
REFERENCES
CAROSI, R., MONTOMOLI C. & VISONÀ D. (2007) - A structural
transect in the Lower Dolpo: insights on the tectonic
evolution of Western Nepal. J. Asian Earth Sci., 29, 407-423.
CAROSI R., MONTOMOLI C., RUBATTO D. & VISONÀ D. (2010) -
Late Oligocene high-temperature shear zones in the core of
the Higher Himalayan Crystallines (Lower Dolpo, Western
Nepal). Tectonics, doi:10.1029/2008TC002400, in press
GODIN L. (2003) - Structural Evolution of the Tethyan
Sedimentary Sequence in the Annapurna area, central Nepal
Himalaya. J. Asian Earth Sci., 22, 307-328.
SEARLE M. P., LAW R. D., GODIN L., LARSON K., STREULE J. M.,
COTTLE J.M & JESSUP M. J. (2008) - Defining the Himalayan
Main Central Thrust in Nepal. J. Geol Soc. London, 165,
523-534.
UPRETI B.N. & YOSHIDA M. (2005) – Geology and Natural
harzards along the Kaligandaki Valley, Nepal. Guidebook for
Himalayan Trekkers, series n. 1. Dept. of Geol., Tri-Chandra
Campus, Tribhuvan University, Kathmandu, 165 pp.
VANNAY, J.C. & HODGES K. (1996) - Tectonometamorphic
evolution of the Himalayan metamorphic core between the
Annapurna and Dhaulagiri, central Nepal. J. Metamorph.
Geol., 14, 635-656.

South Tibtetan Detachment activity constrained at 13-14 Ma by
syntectonic leucogranite emplacement in Laya region, Western
Bhutan
RODOLFO CAROSI (*), CHIARA MONTOMOLI (*), DANIELA RUBATTO (**) & DARIO VISONÀ (°)
Key words: Channel flow, collisional belts, exhumation,
extrusion, Himalayas, leucogranite.
The upper portion of the Greater Himalayan Sequence is
widely intruded by leucogranites: they are both large-size granitic
plutons and smaller size melts whose emplacement was
controlled by tectonic structures. The volume of granites changes
along the strike of the belt reaching the higher values in the
eastern part of the Himalayas (LEECH, 2008).
Recent investigations in Western Bhutan led to recognize two
different generations of Higher Himalayan leucogranites
Fig. 1 – Geological sketch map of the Bhutan Himalayas, with location of
study area. 1: Tibetan Sedimentary Sequence; 2: Checka Formation; 3: Higher
structural level of the Greater Himalayan Sequence; 4: Lower structural level
of the Greater Himalayan Sequence; 5: Lesser Himalya; 6: Siwalik; 7: Higher
Himalayan leucogranites; 8: Quaternary covers.
emplaced in the Greater Himalayan Sequence and characterized
by different age and tectonic setting.
Leucogranites at 24-17 Ma have been intruded in the Greater
Himalayan Sequence and in the Checka Formation (GRUJIC et
alii, 2002; KELLET et alii, 2010). They are biotite or two mica
granite ± tourmaline ± cordierite ± sillimanite ± andalusite ±
kyanite ± garnet and tourmaline granite ± andalusite ± sillimanite
± garnet.
_________________________
(*) Dipartimento di Scienze della Terra, Università di Pisa,
carosi@dst.unipi.it; montomoli@dst.unipi.it
(**) Research School of Earth Sciences, The Australian National
University Canberra, Australia, Daniela.Rubatto@anu.edu.au
(°) Dipartimento di Mineralogia e Petrologia, Università di Padova,
dario.visona@unipd.it
399
A relatively younger generation of leucogranites have been
intruded in the core of the Greater Himalayan Sequence (Gasa-
Koina-Laya) at 20-17 Ma. Their emplacement and cooling are
not related to the South Tibetan Detachment System but they are
closely related to the development normal-sense shear zones with
a top to –the SE sense of shear (CAROSI et alii, 2006). The
normal-sense shear zones accommodate the lengthening of the
inner part of Greater Himalayan Sequence in response to the pure
Fig. 2 – Leucogranite dyke intruded at 13.9 ± Ma in sillimanite bearing
gneiss in the uppermost part of the Greater Himalayan Sequence, northwest of
Laya village.
shear component of the flow as indicated by kinematic analysis
(CAROSI et alii, 2006). More recent leucogranites have been
found northeast of Laya emplaced in high-angle fractures, with a
width of few meters. They are fine grained two mica sillimanite
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bearing leucogranites deformed under solid state conditions.
Kinematic indicators in mylonitic leucogranites indicate a topdown-to-the-North
sense of shear. U-Th-Pb dating on monazites
from a mylonitic leucogranite gives a relatively young
crystallization age (13.9 ± 0.6 Ma). High-angle fractures, filled
by leucogranite, strike nearly E-W and steeply dip to the North.
They belong to a system of fractures affecting the uppermost
portion of the Greater Himalayan Sequence, just below the South
Tibetan Detachment System. Associated low-angle conjugate
brittle-ductile shear zones point to and extensional setting for
their origin with a sub-vertical sigma 1.
They are interpreted as shear zones linked to the brittle
evolution of the South Tibetan Detachment System, continuing to
exhume hot-rocks producing younger melts migrating within the
Greater Himalayan Sequence and emplacing in the opening
spaces produced by the high-angle fractures.
The study system of fractures cannot be related to E-W
extension (e.g. to the Yadong Cross Structure) cross-cutting the
ductile and the brittle shear zones and faults of the South Tibetan
Detachment System few My later (e.g. 11.6 Ma in the Ama
Drime range; COTTLE et alii, 2009).
The tectonic setting of the study fractures suggests that the
activity of the South Tibetan Detachment System, starting at
nearly 24 Ma, continued up to ~ 13-14 Ma. These results are in
agreement with the age of 11 Ma constrained for the inner portion
of the South Tibetan Detachment in the Bhutan Himalayas, north
of the study area (KELLET et alii, 2010).
High-angle fractures (striking nearly E-W and dipping 80° to
the north) filled by mylonitic leucogranites as well as the South
Tibetan Detachment are gently folded by a later system of largescale
gentle antiforms and synforms.
Restoring the projected South Tibetan Detachment to its prelate
folding position the attitude of the high-angle fractures fit
well with an antithetic system of fractures related to a brittle
evolution of the South Tibetan Detachment.
Two main consequences arise:
- antithetic Riedel shear fractures occurred at ~ 13-14 Ma,
related to the late and brittle activity of the South Tibetan
Detachment;
- large-scale gentle folds affecting all the tectonic units as well
as the South Tibetan Detachment (CAROSI et alii, 1999) occurred
after the brittle activation of the South Tibetan Detachment, i.e.
later than ~ 13-14 Ma.
REFERENCES
CAROSI R., LOMBARDO B., MUSUMECI G. & PERTUSATI P.C.
(1999) - Geology of the Higher Himalayan Crystallines in
Khumbu Himal (Eastern Nepal). J. Asian Earth Sci., 17, 785-
803.
400
CAROSI R., MONTOMOLI C. & VISONÀ D. (2006) - Normal sense
shear zones in the core of higher Himalayan Crystallines
(Bhutan Himalaya): evidence for extrusion?. Geol. Soc.
London, SP., 268, 425-444.
COTTLE J.M., JESSUP M.J., NEWELLD.L., HORSTWOOD M.S.A.,
NOBLE S.R., PARRISH R.R., WATERS D.J. & SEARLE M.P.
(2009) - Geochronology of granulitized eclogite from the
Ama Drime Massif: Implications for the tectonic evolution of
the South Tibetan Himalaya. Tectonics, 28, DOI:
10.1029/2008TC002256.
GRUJIC D., HOLLISTER L. & PARRISH R.R. (2002) - Himalayan
metamorphic sequence as an orogenic channel: insight
from Bhutan. Earth Planet. Sc. Lett., 198, 177–191.
KELLET D., GRUJIC D. & ERDMANN S. (2010) - Miocene
structural reorganization of the South Tibetan detachment,
eastern Himalaya: Implications for continental collision.
Lithosphere, 1, 259-281.
LEECH M.L. (2008) - Does the Karakoram fault interrupt midcrustal
channel flow in the western Himalaya?. Earth
Planet. Sc. Lett., 276, 314-322.

Occurrence of a large leucogranite body intruding the Tibetan
Sedimentary Sequence in Western Nepal during Early Miocene:
insights on the exhumation mechanisms of the Himalayan belt
RODOLFO CAROSI (*), CHIARA MONTOMOLI (*), DANIELA RUBATTO (**), LUCA BERTOLDI(**),
CHIARAFRASSI (*), DARIO VISONÀ (**) & PIERO CARLO PERTUSATI (*)
Key words: Channel flow, collisional belts, Exhumation,
extrusion, Himalayas, leucogranite.
INTRODUCTION
The Himalayan belt, which has been developing during India-
Asia collision since ~55 Ma, is regarded as a classic collisional
orogen. It is characterised by the impressive continuity over
hundreds of kilometres of tectonic features such as thrusts and
normal faults, as well as large volumes of high-metamorphic
grade rocks and granite exposed at the surface. This constitutes
an invaluable field laboratory to unravel the tectonic and
metamorphic evolution of crystalline units and the mechanisms of
exhumation of deep-seated rocks in orogens.
The mechanisms of exhumation of the Higher Himalayan
Crystallines or Greater Himalayan Sequence (GHS) by channel
flow and extrusion has been well established in the eastern sector
of the Himalayan belt (from central Nepal to Bhutan) where the
Fig. 1 – Geological sketch map of Himalayas, with location of study area.
_________________________
(*) Dipartimento di Scienze della Terra, Università di Pisa,
carosi@dst.unipi.it; montomoli@dst.unipi.it; frassi@dst.unipi.it;
(**) Research School of Earth Sciences, The Australian National
University Canberra, Australia, Daniela.Rubatto@anu.edu.au
(***) Dipartimento di Mineralogia e Petrologia, Universitò di Padova,
dario.visona@unipd.it, luca.bertoldi@unipd.it
401
thickness of the GHS is nearly 20-30 km and large volume of
granites were intruded in its upper portion, below the South
Tibetan Detachment System (BURCHFIELD et alii, 1992; SEARLE,
1999; BEAUMONT et alii, 2001; GRUJIC, 2006; GODIN et alii,
2006 with references).
WESTERN NEPAL
Moving westward, in Dolpo and Mugu Karnali regions
(Western Nepal) granites are scarcer (LEECH, 2008) and the
thickness of the GHS dramatically decreases down to a minimum
of 2-3 km in the Annapurna area (GODIN et alii, 2006) and 1-3
km in lower Dolpo (CAROSI et alii, 2002; 2007).
A high-temperature shear zone (Toijem shear zone) has been
recently documented in the core of the GHS in lower Dolpo. Its
activity has been constrained at circa 26 Ma (CAROSI et alii,
2010). The Toijem shear zone is responsible for the exhumation
of the hanging wall rocks before the well known period of
extrusion or channel flow of the GHS by the contemporaneous
activity of the Main Central Thrust to the bottom and South
Tibetan Detachment System to the top of GHS (23-17 Ma; see
age review in GODIN et alii, 2006).
Field work in 2008 and 2009 in Dolpo and Mugu-Karnali
areas (Jumla district) allowed to recognize a large granitic body
(nearly 110 kmq) intruding both the uppermost portion of the
GHS and the lower portion of the Tibetan Sedimentary Sequence.
This granite and the Manaslu pluton (whose interpretation in still
debated) represent the very few reported cases of Higher
Himalayan leucogranites intruding the TSS.
U-Pb-Th ages from zircons and monazites extracted from the
main granitic body and dykes intruded both in the GHS and in the
TSS point to an emplacement age at nearly 22-23 Ma. because of
the granite structural position, its the age constrains the
movement of the STDS (or at least of the lower ductile shear
zone) to before 23 Ma in western Nepal. These new data rise
doubts about the contemporaneous activity of the South Tibetan
Detachment System and Main Central Thrust, or at least strongly
limits the length of their contemporaneous activity. As a
consequence, the mechanisms of exhumation of the GHS, such as
extrusion and channel flow, need to be reconsidered for the study
area.
Additional observations, point to a more complex exhumation
history of GHS: (1) The limited thickness of the GHS (one order
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SESSIONE 12
Fig. 2 – Intrusion of the Bura Buri granite and related dykes in the Tibetan
Sedimentary Sequence (TSS). Sisne Himal (Jumla district, Western Nepal).
of magnitude below the 20-30 km requested for an active channel
flow; Godin et al., 2006); (2) the exhumation of the upper portion
by contractional shear zones of the GHS before the MCT-STDS
activity (CAROSI et alii, 2010); and (3) the contractional coupling
and (at least part of) extensional decoupling of TSS and GHS
before 22-23 Ma.
REFERENCES
BEAUMONT C., JAMIESON R.A., NGUYEN M.H. & LEE B. (2001) -
Himalayan tectonics explained by extrusion of a low-viscosity
crustal channel coupled to focused surface denudation.
Nature, 414, 738–742.
BURCHFIEL B. C., CHEN Z., HODEGES K, LIU S., ROYDEN L. H.,
CHANGRONG D. & XU, L. (1992) - The South Tibetan
Detachment System, Himalayan Orogen: extension K Y.. V.
contemporaneous with and parallel to shortening in a
collisional mountain belt. Geol. Soc. Am. SP., 269, 41.
CAROSI R., MONTOMOLI C. & VISONÀ D. (2007) - A structural
transect in the Lower Dolpo: insights on the tectonic
evolution of Western Nepal. J. Asian Earth Sci., 29, 407-423.
CAROSI R., MONTOMOLI C., RUBATTO D. & VISONÀ D. (2010) -
Late Oligocene high-temperature shear zones in the core of
the Higher Himalayan Crystallines (Lower Dolpo, Western
Nepal). Tectonics, doi:10.1029/2008TC002400, in press
CAROSI R., MONTOMOLI C. & VISONÀ D. (2002) - Is there any
detachment in the Lower Dolpo (western Nepal)?. C.R.
Geoscience, 334, 933-940.
GODIN L., GRUIJC D., LAW R.D. & SEARLE M.P. (2006) -
Channel flow, ductile extrusion and exhumation in
402
continental collision zones: an introduction. Geol. Soc. SP.,
268, 1-23.
GRUIJC D. (2006) - Channel flow and continental collision
tectonics: an overview. In: R.D. Law, M.P. Searle & L. Godin
(Eds.) - Channel flow, Extrusion, and Exhumation in
Continental Collision Zones. Geol. Soc. SP., 268, 25-37.
LEECH M.L. (2008) - Does the Karakoram fault interrupt midcrustal
channel flow in the western Himalaya?. Earth
Planet. Sc. Lett., 276, 314-322.
SEARLE M.P. (1999) - Extensional and compressional faults in
the Everest-Lhotse Massif, Khumbu Himalaya, Nepal. J.
Geol. Soc. London, 156, 227-240.

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Tectonics of the southern Alpi Apuane (northern Apennines):
evidence for large scale low-angle normal faulting during Tertiary
extension
Key words: Alpi Apuane, normal faulting, Tertiary.
INTRODUCTION
The Alpi Apuane area is the main tectonic window in the
nappe structure of the Northern Apennines; in the central part of
the tectonic window greenschist facies metamorphic rocks
outcrops below non-metamorphic rocks of the upper tectonic
units. The tectonic window show a NW-SE elongated shape (Fig.
1) and high-angle normal faults are well documented at the
northeast border (Garfagnana valley) and southwest border
(Versilia plain) and interpreted as the bordering faults responsible
for the uplift of the metamorphic core. Investigations in the south
part of the Alpi Apuane reveal that despite high-angle normal
faults are not widespread here, extension was severe during
Tertiary and was achieved through large-scale normal faulting.
Faults are NE-dipping and with top-NE transport direction. Later
uplift of the central part of the Alpi Apuane rotate the main of
this faults and now only a main tectonic contact, sub-horizontal or
SW-dipping it is recognizable in the field.
GEOLOGICAL SETTING
In the Alpi Apuane the deepest structural level of the
Northern Apennine nappe stack is exposed. From top to the
bottom are exposed (Fig. 1): (a) non-metamorphic tectonic units
derived from oceanic domain (Ligurian and Sub-ligurian tectonic
units); (b) a non metamorphic tectonic unit (“Falda Toscana”)
derived from the Adria continental margin and (c) a metamorphic
unit (“Autoctono” Auctt) derived from a more external portion of
the Adria continental margin. All the tectonic units were stacked
during the Tertiary tectonic evolution of the northern Apennines.
_________________________
(*) Centro di GeoTecnologie e Dipartimento di Scienze dellla Terra,
Università degli Studi di Siena, San Giovanni Valdarno (AR)
conti@unisi.it
PAOLO CONTI (*), GIOVANNI MASSA (*) & LUIGI CARMIGNANI (*)
405
The evolution of this sector of the Adria margin encompasses:
1. A stage of shortening (D1 deformation), underthrusting
associated with a peak metamorphism of about 350-450 °C
and 0.5-0.6 GPa. During this stage polyphasic deformation
occur with isoclinal folding and main foliation development.
Locally syn-contractional exhumation may occur;
2. some stages of extension (D2 deformation) that led to final
exhumation and uplift, with development of recumbent to
upright folding, low-angle normal faulting and finally high
angle brittle faulting. Stratigraphic and geochoronological
constraints point for about 20 Ma for the shortening stage
and an age of 10-13 Ma for the onset of extension.
Fig. 1 – Tectonic sketch map of the Northern Apennines surrounding the
Alpi Apuane tectonic window. Location of fig. 2 is indicated.
SESSIONE 12

SESSIONE 12
TECTONIC OF THE SOUTHERN ALPI APUANE
In the southern portion of the Alpi Apuane Metamorphic
Complex (Stazzema area, Fig. 2) D1 isoclinal folding linked with
underthrusting and nappe emplacement is overprinted by later
isoclinal NE-facing folds and contemporaneous shear
deformation.
Shear deformation occurs along tectonic contacts: (a) bearing
undeformed ore bodies among boudins along the mylonitic
foliation; (b) developing strong shape preferred orientation of
calcite grains parallel to the mylonitic foliation when crosscut
marble formations: calcite grains are not affected by any later
static recrystallization; (c) refold earlier foliation and tectonic
contacts; (d) are NE-dipping and show a top-NE sense of sear.
Based on these observation we infer for this deformation and
related isoclinal folding a development during uplift, in a regional
extensional context.
Fig. 2 – Tectonic map of the southern Alpi Apuane. See fig. 1 for map
location.
During extension in the southern Alpi Apuane the whole
Falda Toscana unit is affected by low angle normal faults that: (a)
led to remarkable tectonic elision, with younger rocks (Macigno,
Maiolica, etc.) directly juxtaposed with older formations (Calcare
cavernoso, etc.); (b) cause cataclastic deformation in the Calcare
cavernoso fm.; (c) led to thick cataclastic rocks with clasts of
rethian and jurassic limestones.
One of the main low angle normal faults runs from NE of
Viareggio (Fig. 2) to N of Fornovolasco. This normal fault cuts
increasing older rocks in the hanging-wall (Falda Toscana
tectonic unit) towards NE, we infer for this fault a “top-NE”
tectonic transport direction. This fault between Sant’Anna and
406
Fornovolasco is later refolded by upright folds with gently SE
dipping fold axis and now the fault plane dips toward SE. In its
southern portion (Camaiore area) the fault dips toward S.
Evidence of refolding and overprinting by later high-angle
normal faults (N of Fornovolasco) points for this low angle
normal fault a development at midcrustal levels.
The occurrence of a km-scale low-angle normal fault in this
area could explain the evidence of strong internal deformation in
rocks of the whole southern Alpi Apuane Metamorphic Complex
(mylonite development, isoclinal folding) all linked with
extension and NE-transport direction.

P-T evolution of Punta Orvili metabasite, NE Sardinia, Italy: some
constraints from pseudosection modelling
Key words: Eclogite facies, metabasite, metamorphic
re-equilibration, pseudosection, - P T path, Variscan Sardinia .
INTRODUCTION
The Punta Orvili metabasite crops out as a lens of ca. 10 m in
diameter, in the northern side of the Posada Valley in the
Hercynian Metamorphic Complex with Dominant Amphibolite
Assemblages of the variscan chain of Sardinia (CARMIGNANI et
alii, 2001). The metabasite lens is hosted in a sequence of
mylonitic gneiss with calc-silicate nodules. The regional foliation
in the host rocks is the S2 schistosity striking N 80° and dipping
30°-50° towards SE. Locally the S2 is transposed by centimetric,
sinistral strike-slip green-schist shear zones striking N 30° and
dipping 60° towards SE (CRUCIANI et alii, 2006). The mylonitic
gneiss is characterized by millimetric to centimetric quartzfeldspathic
aggregates enveloped by the S2 foliated phyllosilicaterich
matrix. The age of the Punta Orvili metabasite protolith is
unknown. Other metabasite from the Migmatite Complex yield a
Upper-Ordovician protolith age (GIACOMINI et alii, 2005;
PALMERI et alii, 2004).
A detailed petrological study of the Punta Orvili metabasite
has been performed by integrating quantitative pseudosection
modelling and reaction balancing, with the aim of: (i) reconstruct
the metamorphic evolution and P-T path of a still poorly
investigated Sardinian metabasite; (ii) compare the P-T evolution
of the Punta Orvili metabasite with that of the other eclogites
from northern Sardinia.
PETROGRAPHY
The Punta Orvili metabasite consists of amphibole, garnet,
clinopyroxene, biotite and plagioclase. Ilmenite, Fe-oxide,
_________________________
GABRIELE CRUCIANI (*), MARCELLO FRANCESCHELLI (**) & CHIARA GROPPO (°)
(*) Dipartimento di Scienze della Terra, Università di Cagliari,
gcrucian@unica.it
(**) Dipartimento di Scienze della Terra, Università di Cagliari,
francmar@unica.it
(°) Dipartimento di Scienze Mineralogiche e Petrologiche, Università di
Torino, chiara.groppo@unito.it
407
titanite, apatite, rutile, quartz, epidote, K-feldspar and chlorite
have also been observed in minor amounts. The metabasite
preserves clinopyroxene + plagioclase symplectites and coronitic
microstructures around garnet which reveal a complex
metamorphic history from the eclogite facies down to granuliteand
amphibolite facies.
Garnet occurs as medium-grained, strongly fractured grains
with composition Alm50-55 Sps1-3 Prp15-25 Grs18-30 (abbreviations
according to FETTES &DESMONS, 2007). It shows an irregular
zoning with a decrease in Ca, counterbalanced by an increase in
Fe and Mg content from core to rim (core: XMg=0.25-0.27; rim:
XMg=0.30-0.32). Mn content is constant, or irregularly variable
with a very slight enrichment in the outermost rim.
Clinopyroxene has been observed into two textural
occurrences: Cpx1 and Cpx2.. Medium- to coarse-grained Cpx1 in
the matrix is a diopside (XMg ∼ 0.80) characterized by an increase
in Na toward the rim (up to 0.17 a.p.f.u.). Cpx2 occurs in the
symplectite developed at the expenses of Cpx1. It is also a
diopside (XMg ∼ 0.80) with Na ∼ 0.06 a.p.f.u..
Amphibole was observed in four types of occurrences: Am1,
Am2, Am3 and Am4. Am1 was observed in the matrix as unzoned
grains with actinolite or Mg-hornblende composition, or as zoned
grains with actinolite core (less commonly Mg-hornblende)
surrounded by mostly Mg-hornblende rim. It is also included in
garnet. Am2 occurs as a thin layer at the contact between Am1 and
the coronitic shell around garnet; it is pargasite to tschermakite.
Am3 occurs in the garnet corona and ranges in composition
between Mg-hornblende, tschermakite, and pargasite. Am4
observed in veins is actinolite with XMg between 0.5 and 0.6.
Plagioclase was only observed in symplectites and coronitic
microdomains (Pl1, Pl2, respectively). Pl1 lamellae in the
symplectite is Ab60-70. Pl2 from the coronae is more calcic with
compositions mostly in the range Ab48-53. Albite lamellae have
been also locally found in the symplectite.
Biotite is Ti- (∼0.6 a.p.f.u.) and Ba-rich (∼0.2 a.p.f.u.) with
XMg ratio ∼ 0.6.
DISCUSSION AND CONCLUSIONS
The Punta Orvili metabasite preserves microstructural
evidences of: (i) a pre-symplectite prograde stage (M1) revealed
by the occurrence of amphibole inclusions in garnet, by Na-rich
diopside (Cpx1), and by compositional zoning in garnet,
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clinopyroxene and amphibole; (ii) a symplectite stage (M2)
documented by the occurrence of Cpx2+ Pl1 symplectite growing
on the margin of Cpx1; (iii) a corona stage (M3) documented by
the formation of micrometric-thick Pl2 ± Amp3 ± Ilm coronas
around garnet; (iv) a late stage (M4), documented by the growth
of epidote and albite, by the replacement of biotite and
clinopyroxene by chlorite, and by the formation of veins and
fractures filled by actinolitic amphibole, titanite and K-feldspar.
The M1 pre-symplectite stage has been modelled by
pseudosections calculated in the NCKFMASTH model system
following the approach of CONNOLLY (1990) at aH2O=1 (for aH2O
= 0.5 field boundaries are shifted towards lower temperatures of
about 50°C). Mg and Ca zoning in garnet and Na zoning in
clinopyroxene document a progressive increase in temperature
and pressure during garnet and clinopyroxene growth from 610 <
T < 630°C, 1.7 < P

Metamorphic evolution of gabbro and acidic volcanics from Nurra,
northwestern Sardinia
Key words: Amphibole, low -grade metamorphism, metagabbro,
metarhyolite, potassic white mica, Sardinia.
The metamorphic basement of south and central Nurra
belongs to the internal nappe Zone of the Variscan chain of
Sardinia (CARMIGNANI et alii, 2001). This basement consists of a
volcano-sedimentary sequence mainly made up of phyllite,
metasandstone metagreywacke, metaconglomerate, felsic and
intermediate metavolcanics, oolitic ironstone, metagabbro lenses
and rare marble. Based on the mineral assemblage of pelitic and
psammitic rocks four metamorphic zones with increasing
metamorphic grade towards the northwest have been
distinguished in the Nurra basement: i) chlorite zone; ii) biotite
zone, iii) garnet + albite zone, iv) garnet + oligoclase zone
(FRANCESCHELLI et alii, 1990).
Metavolcanics of the Canaglia Unit (metarhyolite to
metadacite) occur as, mostly N-S oriented, lenticular bodies from
0.5 to 2 km in length. Metavolcanics are withish to greyish, finegrained,
strongly foliated rocks containing flattened augens of
quartz and feldspar in a phyllosilicate rich matrix.
The studied metagabbro crops out as a body of ~ 1 km × 0.6
km in size at Monte Rugginosu, Central Nurra. The Monte
Rugginosu metagabbro is a brownish to greenish massive to
moderately schistose rock, characterized by plagioclase and
amphibole crystals up to 10 and 4 mm in size, respectively. A
decrease in the size of plagioclase and in the amount of mafic
minerals has been observed towards the north. Igneous minerals
in the Nurra metagabbro are plagioclase and rare clinopyroxene
pre-dating the S1 schistosity. Ilmenite, up to 0.3 mm in size, is
also thought to be of igneous origin. Metamorphic minerals are
mainly amphibole, biotite, chlorite, epidote, stilpnomelane,
titanite, apatite, quartz, and K-feldspar in variable modal
amounts.
Albite (Ab97-99) is by far the most abundant mineral, locally
reaching ~50% of the rock volume.
_________________________
GABRIELE CRUCIANI (*), MARCELLO FRANCESCHELLI (**) & HANS-JOACHIM MASSONNE (°)
(*) Dipartimento di Scienze della Terra, Università di Cagliari,
gcrucian@unica.it
(**) Dipartimento di Scienze della Terra, Università di Cagliari,
francmar@unica.it
(°) Institut für Mineralogie und Kristallchemie, Universität Stuttgart,
h-j.massonne@imi.u-stuttgart.de
409
Clinopyroxene, observed only in a few samples as isolated
grains up to 0.5 mm in size, is diopside to hedenbergite (XMg:
0.62-0.64, Na: 0.01-0.03 a.p.f.u., Ti: 0.03-0.05 a.p.f.u.).
Chlorite is by far the most abundant metamorphic mineral,
forming the fine grained intergranular matrix within albite
crystals. XMg in chlorite is 0.37-0.43, whereas Al/(Al+Fe+Mg) is
~0.35. Chlorites with variable Mg/Fe ratio have been observed in
some samples. High K2O content in chlorite (up to 3-4 wt.%)
reveals that at least part of the metagabbro chlorite derives from
biotite replacement.
Stilpnomelane (XMg: 0.18-0.25, K2O ∼ 1.0-1.5 wt.) is radially
arranged at the albite/chlorite interface, or found as small single
elongated crystals associated with biotite and chlorite in the rock
matrix.
Amphibole occurs as small elongated or medium- to coarsegrained
crystals of prevailing actinolite composition. All
amphiboles show a wide compositional variation, often observed
as a strong patchy zoning. Patches, usually of hornblende
composition, are Al-, Na-rich, and Mg-poor (7-10 wt.% Al2O3;
1.3-1.6 wt.% Na2O; 7-8 wt.% MgO), as compared to the
composition of actinolitic amphibole (2-6 wt.% Al2O3; 0.2-0.9
wt.% Na2O; 8-12 wt.% MgO). XMg is 0.41-0.67 in matrix
amphibole and 0.39-0.44 in amphibole patches. XCa is between
0.92-0.98 and similar in amphibole matrix and in the patches.
Biotite (XMg: 0.36-0.44) has been observed as two textural
varieties: i) single euhedral crystals associated to chlorite and
epidote in the matrix, ii) anhedral biotite growing on amphibole.
Epidote occurs as euhedral to subhedral grains with a very
strong variability in size and composition. Subhedral grains often
grew on albite suggesting a Ca-richer composition of the previous
igneous plagioclase. Euhedral grains of epidote, usually less than
0.3 mm, are often associated to chlorite and biotite in the rock
matrix. Compositional variations are related to a patchy zoning,
with Fe-richer zones (XFe: 0.25-0.27) and Fe-poorer ones (XFe:
0.19-0.21) within the same epidote grain.
Ilmenite, showing a considerable amount of Mn (3.8 wt.%
MnO; Mn ~ 0.08 a.p.f.u.), is always surrounded by a thick,
regular rounded shell of titanite up to 0.2 mm in width.
Apatite was observed as coarse-grained rounded crystals, or
as elongated crystals up to 0.3-0.4 mm in length. K-feldspar has
been found in some metagabbro samples as sporadic anhedral
micrometric patches associated to albite and amphibole, or as
millimetric anhedral grains. In both cases no detectable Na is
present in K-feldspar.
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The metavolcanics are characterized by the close alternation
of fine-grained phyllosilicate-rich and quartzofeldspathic layers
in which flattened, partially recrystallized, fractured and/or
variably deformed quartz, albite, or more rarely K-feldspar
porphyroclasts are frequently found. Albite and K-feldspar
approach the composition of pure phases (no considerable K2O
and Na2O content, respectively). Quartzofeldspathic layers
consist of fine-grained quartz with subordinate clusters of fine
grained albite. Chlorite and potassic white mica, oriented
according to the regional S2 schistosity, form the phyllosilicate
layers. Si contents in white mica are between 3.2-3.3 a.p.f.u.,
whereas XMg of chlorite is mostly within 0.5-0.6. Fresh biotite
was not found in the analysed samples, as all former biotite was
partially transformed to chlorite discernable by K2O contents
between 2 and 4 wt.%. K-free chlorites, however, were also
detected.
The metamorphic evolution of the Nurra metagabbro and the
acidic metavolcanics has been investigated by the construction of
P-T pseudosections for fixed bulk-rock composition in the
NCKFMASH+Ti+Mn model system within the P-T frame 1-11
kbar, 150-450°C. These pseudosections were calculated using the
computer software package PERPLE_X (CONNOLLY, 2005) and
the internally consistent thermodynamic data set and the equation
of state for H2O by HOLLAND &POWELL (1998, revised 2004).
Solid-solution models used are those of HOLLAND &POWELL
(1998) for garnet, biotite (Bt), phengite (Ph), chlorite (Chl) and
epidote (Ep). Additional solid-solution models were taken from
FUHRMAN &LINDSLEY (1988), MASSONNE &WILLNER (2008),
LIU et alii (2009), for plagioclase (Pl), alkalifeldspar, paragonite,
pumpellyite, stilpnomelane, amphibole (Amp) and Na-rich
clinopyroxene. The bulk-rock compositions used in the
calculations were obtained by (i) averaging eight calcite-free
samples from the metagabbro, (ii) consideration of diverse
metarhyolite compositions, and (iii) addition of H2O to
accomplish H2O saturation at most of the considered P-T
conditions, (iv) consideration of some iron to be ferric (addition
of some O2).
The P-T path of the metagabbro is clockwise with the
prograde segment overprinted by later metamorphic reequilibration.
Pressure peak, constrained by the absence of garnet
in the studied samples, occurred at pressures ≤ 5-6kbar and T ~
400°C, in the multivariant field Amp+Bt+Chl+Ep+Ph+Pl +
titanite (Ttn) + quartz (Qtz). A slight increase in temperature up
to 420-430°C accompanied by a decrease in pressure to ~ 2.5
kbar led to the metamorphic peak corresponding to the
multivariant assemblage Amp+Bt+Chl+Ep+Pl+Ttn+Qtz +
magnetite in which phengite is not any more stable. The last
segment of the P-T path is characterized by a nearly isobaric
cooling marked by a decrease in temperature to 250-300°C
leading to the formation of stilpnomelane. This last stage is also
confirmed by the P-T conditions recorded in the metavolcanics in
which XMg of chlorite and Si content of potassic white mica
410
indicate P-T conditions of 200-250°C at 2.5 kbar. The peak
pressure conditions derived from the metagabbro are also
compatible with the observed Si contents of potassic white mica
in the metavolcanics.
REFERENCES
CARMIGNANI L., OGGIANO G., BARCA S., CONTI P., SALVADORI I.,
ELTRUDIS A., FUNEDDA A. & PASCI S. (2001) - Geologia
della Sardegna. Note illustrative della Carta Geologica della
Sardegna a scala 1:200000. Mem. Descr. Carta Geol. It., 60,
283 pp.
CONNOLLY J.A.D. (2005) - Computation of phase equilibria by
linear programming: a tool for geodynamic modeling and its
application to subduction zone decarbonation. Earth Planet.
Sc. Lett., 236, 524-541.
FRANCESCHELLI M., PANNUTI F. & PUXEDDU M. (1990) - Texture
development and PT time path of psammitic schist from the
Hercynian chain of NW Sardinia (Italy). Eur. J. Mineral., 2,
385-398.
FUHRMAN M.L. & LINDSLEY D.H. (1988) - Ternary-feldspar
modeling and thermometry. Am. Mineral., 73, 201-215.
HOLLAND T.J.B. & POWELL R. (1998) - An internally consistent
thermodynamic data set for phases of petrologic interest. J.
Metamorph. Geol., 16, 309-343.
LIU Y., LIU H., MASSONNE H.-J. & THEYE T. (2009) - Evidence
for oceanic subduction at the NE Gondwana margin during
Permian and Triassic times. Terra Nova, 21, 195-202.
MASSONNE H.-J. & WILLNER A.P. (2008) - Phase relations and
dehydration behaviour of psammopelite and mid-ocean ridge
basalt at very-low-grade to low-grade metamorphic
conditions. Eur. J. Mineral., 20, 867-879.

U-Pb chronological constraints for the late- and post-orogenic
episodes in the Ligurian Variscides
GIORGIO DALLAGIOVANNA (*), LAURA GAGGERO (**), MATTEO MAINO (*), SILVIO SENO (*) & MASSIMO TIEPOLO (°)
Key words: Basement, Permo-Carboniferous,Variscan high T/P
metamorphism.
GEOLOGICAL BACKGROUND
In spite of the polyphase Alpine evolution, the Ligurian Alps
preserve different thick post-Variscan successions (forming the
so-called tegument) partially detached from their lower Paleozoic
basement. The present-day tectonic units, particularly the
Briançonnais ones, display an internal continuity and their
consistency allowed inferring stratigraphic successions, and even
more, their paleogeographic setting (VANOSSI et alii, 1986). Such
Late Paleozoic successions, bounded by a lower and an upper
unconformity, were built by volcanic and sedimentary products
with highly variable relative thickness and facies due to an
irregular palaeomorphology caused by the development of graben
and half-graben structures. Within the volcanic successions,
CABELLA et alii (1988) and CORTESOGNO et alii (1993)
recognized two main magmatic series: an early bimodal calcalkaline
igneous activity, followed by K-alkaline products.
SHRIMP U–Pb dates of small calc-alkaline intrusive bodies
indicate an intrusion age between 300 and 294 Ma (GAGGERO et
alii, 2004). The main calc-alkaline volcanism occurred between
285.6±2.6 Ma and 272.7±2.2 Ma (LA ICP MS dating;
DALLAGIOVANNA et alii, 2009). The alkaline magmatic episode is
represented by K-rich rhyolitic ignimbrites which provided ages
as old as 258.5 ± 2.8 Ma.
THE PARADOX OF THE “BARBASSIRIA” BASEMENT
In the Ligurian Alps, the Lower Permian volcano-sedimentary
succession of the Mallare Unit (Internal Briançonnais) rests on a
gneissic basement re-equilibrated under pre-Alpine amphibolite
facies metamorphic overprint, named Barbassiria Orthogneiss. In
spite of the presence of this metamorphism, its effusive protolith
has been dated at the Latest Permian-Earliest Triassic (~250 Ma)
_________________________
(*) Dipartimento di Scienze della Terra – Università degli Studi di Pavia
(**) Dipartimento per lo Studio del Territorio e delle sue Risorse –
Università degli Studi di Genova, gaggero@dipteris.unige.it
(°) C.N.R. - Istituto di Geoscienze e Georisorse (IGG), Unità di Pavia
411
by means of a Rb-Sr isochron on muscovite separates (DEL MORO
et alii, 1981). The Barbassiria Orthogneiss are rhyolites with Kfeldspar
porphyroclasts (5-15 mm) and lenticular quartz
aggregates, likely from pristine phenoclasts. The orthogneisses
are interbedded with quartz – mica schists, locally as rich as 90%
in volume in quartz, likely originated from in situ arenitization of
the igneous rock. Locally, minor metarhyolitic dikes cut across.
Relic pre-Alpine metamorphic textures are absent in the dikes,
rare in the orthogneisses, relatively frequent in the
metasediments, and characterized by biotite + muscovite and
quartz-feldspatic layers. The Alpine deformation strongly
affected the Barbassiria basement and its cover
(DALLAGIOVANNA et alii, 1997). The Alpine blueschist
metamorphic overprint is pervasive and expressed as a composite
S1+S2 fabric. Despite localized mechanical fractionation of Kfeldspar
and quartz, che bulk rock composition is homogeneous,
metaluminous (A/CNK between 1.2 and 1.5) and close to a
minumum melt liquid. The Ta/Yb correlation points to a syncollisional
setting, whereas a late-orogenic character is suggested
by the parameters R1-R2. Above the Barbassiria Orthogneiss, the
base of the Lower Permian succession is represented by the C.
Lisetto Metarhyolites, aged 285.6 ± 2.6 Ma (DALLAGIOVANNA et
alii, 2009). This age clearly contrasts with the remarkably
younger Rb/Sr dating of the Barbassiria Orthogneiss (~250 Ma).
Some questions thus arise in order to match the emplacement age
of the rhyolitic protolith, the timing of amphibolite facies
metamorphism and possible further magmatic episodes. In order
to solve these discrepancy and contribute to describe the lateorogenic,
tectono-magmatic evolution of the Ligurian Variscides,
we performed U-Pb dating by LA ICP MS on the main body of
the Barbassiria Orthogneiss and on metarhyolitic dikes cutting
across.
U-PB DATING
The in situ U-Pb geochronology and trace element
abundances were determined with excimer laser ablation (ELA)-
ICP-MS. The U-Pb analysis was carried out on zircons separated
from one sample from the orthogneiss and one from a
metarhyolic dike cutting across the main body of the Barbassiria
basament. The U-Pb analysis performed on the magmatic textural
domain from orthogneiss revealed two main populations with
ages of 300±5 Ma and 265±4 Ma respectively. The U-Pb analysis
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from the metarhyolitic dike shows a single age population of
259±3 Ma.
DISCUSSION AND CONCLUDING REMARKS
The spots on oscillatory zoning in zircon grains from the main
volcanic body yielded an age as old as 300±5 Ma, that can be
assessed as the emplacement age of the rhyolite. The Barbassiria
Orthogneiss however show a pre-Alpine metamorphic overprint
characterized by the assemblage muscovite + K-feldspar + quartz
+ plagioclase (CORTESOGNO et alii, 1995). The age of the
Barbassiria metamorphism could correspond to the age of the
low-grade Variscan amphibolite-greenschist facies
metamorphism dated in the Ligurian Briançonnais basement at
310–300 Ma, and associated with the final stages of exhumation
(GIACOMINI et alii, 2007). Thus, a very short time gap results
between the shallow emplacement of the rhyolite and the
amphibolite facies metamorphism. Taking into account the
resolution and meaning of the different isotopic systematics, after
emplacement rhyolites were brought from surface at a minimum
depth of 6-7 km in about 5 Ma, or alternatively, the metamorphic
overprint was likely syn-kinematic to the shallow level
emplacement. The dikes cutting the Barbassiria Metarhyolite at
259±3 Ma belong to the diffuse K-rhyolitic volcanism that built
the Lithozone D, already dated at 258.5±2.8 Ma
(DALLAGIOVANNA et alii, 2009).
Some consequences derive from these new data.
1) The definition of a Carboniferous basement, assessed by
radiometric dating, after the younging of the continental
sediments overlying or intercalated in Lower Permian
acidic and intermediate volcanites
2) The Barbassiria Orthogneiss were emplaced at shallow
level/subintrusive, with intercalated sediments. The
muscovite-bearing assemblage is a pre-Alpine relic of an
amphibolite facies (syn-kinematic?) overprint.
3) A short time interval is deduced between emplacement
and overprint (about 5 Ma); a rough estimate indicates
that an average speed rate for underplating the rhyolites
to 6-7 km and taking them back to the surface require ca
0.3 cm / y. This rate could be even lower if associated
with a high T/P likely during the exhumation.
REFERENCES
CABELLA R. CORTESOGNO L. DALLAGIOVANNA G. VANNUCCI R.
& VANOSSI M. (1988) - Vulcanismo, sedimentazione e
tettonica nel Brianzonese ligure esterno durante il Permo-
Carbonifero. Atti Tic. Sc. Terra, 31, 269-326.
CORTESOGNO L., DALLAGIOVANNA G., GAGGERO L. & VANOSSI
M. (1993) - Elements of the Palaeozoic history of the
412
Ligurian Alps. In: J.F. von Raumer & F. Neubauer (Eds.) -
Pre-Mesozoic Geology in the Alps. Springer, Berlin, 257–
277.
CORTESOGNO L., DALLAGIOVANNA, G.,GAGGERO L., SENO S. &
VANOSSI M. (1995) – Nuovi dati sul basamento e sul
tegumento carbonifero dell’Unità di Mallare (Brianzonese
intermedio-interno, Alpi Liguri). Atti Tic. Sc. Terra, S.s., 3,
65-82.
DEL MORO A. PARDINI G. MESSIGA B. & POGGIO M. (1981) -
Dati petrologici e radiometrici preliminari sui massicci
cristallini della Liguria occidentale. Rend. Soc. Ital. Miner.
Petrol., 38(1), 73-87.
DALLAGIOVANNA G., GAGGERO L., MAINO M., SENO S. &
TIEPOLO M. (2009) – U Pb zircon ages for post-Variscan
volcanism in the Ligurian Alps (Northern Italy). J. Geol. Soc.,
166, 101-114.
DALLAGIOVANNA G., SENO S. & VANOSSI M. (1997) - An example
of the Alpine structural evolution of the Penninic zone in the
Ligurian Alps: tectonics of the Barbassiria area. Eclogae
Geol. Helv., 90, 337–344.
GAGGERO L., CORTESOGNO L. & BERTRAND J.M. (2004) - The
pre-Namurian basement of the Ligurian Alps: a review of the
lithostratigraphy, pre-Alpine metamorphic evolution, and
regional comparison. Period. Mineral., 73, 85–96.
GIACOMINI F., BRAGA R., TIEPOLO M. & TRIBUZIO R. (2007) -
New constraints on the origin and age of Variscan eclogitic
rocks (Ligurian Alps, Italy). Contrib. Mineral. Petr., 153 (1),
29-53.
VANOSSI M., CORTESOGNO L., GALBIATI B., MESSIGA B.,
PICCARDO G.B. & VANNUCCI R. (1986) - Geologia delle Alpi
Liguri: dati, problemi, ipotesi. Mem. Soc. Geol. It., 28, 5–75.

Quartz microstructural and petrofabrics constraints in the Lesser
Himalayan Crystalline (Lower Dolpo, Western Nepal)
Key words: Deformation temperatures, Nepal, Qtz
microstructures and petrofabrics.
INTRODUCTION
The continental collision at ca. 50-55 Ma between the passive
margin of Indian plate and the Andean-type margin of Asian
block (Lhasa block) produced the Himalayan mountain belt. Its
high topographic level and the excellent exposure of high-grade
metamorphic rocks make it a natural laboratory where study the
mechanisms and the processes responsible of the exhumation of
deep-seated crustal rocks. Classically three main tectonometamorphic
units can be described (Fig. 1). From lower
structural levels in the south to upper structural levels in the
north, there are: (1) the Lesser Himalayan (LH), made by
Precambrian to Eocene sedimentary sequences that recorded an
increase in the metamorphic grade up to greenschists
metamorphic facies (Grt+Bt zone) in the north; (2) the Higher
Himalaya Crystalline (HHC), made mainly by high-grade rocks,
migmatites and leucogranites affected by Grt+Bt up to Sill+Ky
mineral assemblage and (3) the Tibetan Sedimentary Sequence
(TSS), made by upper Paleozoic to Eocene sediments deformed
under very low-grade metamorphic conditions. The HHC is
bounded by two regional scale low-angle shear zones active
contemporaneously between 23 and 17 Ma (HODGES, 2000 and
references therein): the Main Central Thrust (MCT) at the
bottom, and the South Tibetan Detachment system at the top.
Despite detailed studies have been published to constraint the
kinematic and tectono-metamorphic evolution of the MCT
(SEARLE et alii, 2008 with references therein) on the central and
eastern sector of the Himalayan belt, very few data are available
for the Dolpo region (western Nepal; CAROSI et alii, 2007).
_________________________
CHIARA FRASSI (*), RODOLFO CAROSI (*), CHIARA MONTOMOLI (*), PIERO CARLO PERTUSATI (*),
LUCA BERTOLDI (**) & DARIO VISONA' (**)
(*) Dipartimento di Scienze della Terra, Università di Pisa, e-mail:
frassi@dst.unipi.it
(**) Dipartimento di Geoscienze, Università di Padova
Lavoro eseguito bell’ambito del progetto COFIN-MiUR 2007 con il
contributo finanziario dell’Università.di Pisa
413
Fig. 1 – Location of the study area
In the study section, located in the central sector of lower
Dolpo region, the LH is represented mainly by a sequence of 10
to 60 cm thick layers of white quartzites and micaschists affected
by upper greenschist metamorphic facies, whereas the HHC is
represented by gneisses and migmatitic gneisses with a dominant
sillimanite + biotite metamorphic assemblage. The MCT zone is
few meters thick and poorly exposed. A leucogranitic body
crosscutting the main foliation in the HHC and in the TSS,
constraining the upper limit of STDS c. 24-25Ma (Buraburi
granite: CAROSI et alii, 2009).
Both in the LH and HHC the main foliation shows a general
NW-SE strike and dips 30-45° toward NE whereas the mineral
lineation, marked by streaking of biotite and muscovite and by
quartz aggregates, trends NNE-SSW and plunges ca. 40° toward
NE (Fig. 2).
QUARTZ MICROSTRUCTURAL AND PETROFABRICS
CONSTRAINTS
To document the deformation regime responsable of the
shearing along the MCT zone, we collected oriented sample of
quartzites and quartz-rich micaschists and gneisses in the LH
along a transect oriented sub-orthogonal to the MCT zone. More
in detail we carried out microstructural, metamorphic and quartz
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petrofabrics analyses in order to constrain (1) the deformation
temperature and (2) the finite strain geometry (i.e. magnitude,
path and shape of finite ellipsoid) recorded at different structural
levels below the MCT.
Quartz microstructures revealed that the recrystallization
occurred mainly by GBM (Fig. 2B) under deformation
temperatures higher the 550°C. Moving toward the MCT we
document an increase in the size of both recrystallized quartz
grains and biotite and muscovite porphyroblasts. In the samples
collected closer to the MCT, we observe ameboid boundaries
between quartz and feldspar indicating that deformation occurred
at temperatures higher that 600-650°C.
However, at c. 1 km far from the MCT, we document the
Fig. 2A- Grain boundary migration represents the dominant
recrystallization mechanism. 2B- Example of quartz c-axis fabrics
obtained for a quartzite collected c. 1300 m far from the MCT.
A.
B.
414
presence of an important process of subgrain rotation
recrystallization overprinted on the GBM fabrics. This event
produced a strong bimodal grain size distribution under
temperatures of 400-500°C. As a consequence, we suggest the
presence of a secondary tectonic lineament inside the LH active
at shallower structural levels after the MCT shearing that is not
directly observable in the field.
Quartz c-axis fabrics revealed asymmetric Type-I cross girdle
pointing to a top-to-the SW sense of shear. Moving toward the
MCT (1) deformation temperatures obtained using Qtz c-axis
opening angles increase, in agreement with those obtained by
quartz microstructures and by the mineral assemblage and (2) the
asymmetry of Qtz fabrics skeleton becomes stronger, implying an
increase in the simple shear component of deformation.
REFERENCES
CAROSI R., MONTOMOLI C. & VISONÀ D. (2007) - A structural
transect in the Lower Dolpo: Insights on the tectonic
evolution of Western Nepal. J. Asian Earth Sci., 29, 407-423.
CAROSI R., MONTOMOLI C., RUBATTO D., BERTOLDI L., FRASSI
C., VISONÀ D. & PERTUSATI P.C. (2009) - Along strike
variations of exhumation mechanisms of the Higher
Himalayan Crystallines: insights from western Nepal. 24TH
Himalaya-Karakorum-Tibet Workshop, Beijing. August 2009.
HODGES K. (2000) - Tectonics of Himalaya and southern Tibet
from two perspectives. Geol. Soc. Am. Bull., 11(2), 324–350.
SEARLE M., LAW R.D., GODIN L., LARSON K., STREULE M.,
COTTLE J. & JESSUP M. (2008) - Defiing the Main Central
thrust in Nepal. J. Geol. Soc., 165, 523-534.

Key words: Internal Crystalline Massifs, Piedmont Zone,
tectono-metamorphic evolution, Western Alps.
GEOLOGICAL AND STRUCTURAL FRAMEWORK
Detailed geological mapping combined with micro-structural
and petrological investigation allowed to clarify the structural and
metamorphic relations between the Internal Crystalline Massifs
(ICM) and the Piedmont Zone (PZ) and between the Lower and
Upper PZ in the Western Italian Alps.
The three study areas (Gressoney, Orco and Susa sections)
take into consideration the same structural level across the axial
portion of the metamorphic belt, i.e. a geological section across
the Internal Crystalline Massifs vs Piedmont Zone boundary.
Two Tectonic Elements were detected on the basis of their
tectono-metamorphic evolution. The Lower Tectonic Element
(LTE) consists of the ICM and the Lower PZ (Zermatt-Saas type
Units) both showing well preserved eclogite facies relics. Instead,
the Upper Tectonic Element (UTE) consists of the Upper PZ
(Combin type Units) and of the Gneiss Minuti Complex of the
Sesia-Lanzo Zone, both lacking evidence of eclogite facies relics.
These two tectonic elements are separated by thick shear zones
developed under greenschist facies conditions known as
Gressoney Shear Zone (REDDY et alii, 1999), Orco Shear Zone
(GASCO et alii, 2009) and Susa Shear Zone.
Despite the three areas are far away from each other,
however, the structural data can be compared if strictly linked to
the metamorphic evolution. The only structural elements which
show a different orientation are the S1 foliations because of the
different position of the three study areas around the ICM.
In the LTE the D1 event is characterized by development of
isoclinal folds trending E-W to NE-SW and of a composite S1
foliation developed under middle-P greenschist to epidote-albite
amphibolite facies always associated with top to W sense of
shear; generally fold axes are parallel to stretching lineations.
_________________________
Structural and metamorphic evolution across the Internal
Crystalline Massifs vs Piedmont Zone boundary (Western Alps)
(*) Università degli Studi di Torino, Dipartimento di Scienze della Terra,
ivano.gasco@unito.it; marco.gattiglio@unito.it
(**) Università degli Studi di Torino, Dipartimento di Scienze
Mineralogiche e Petrologiche, alessandro.borghi@unito.it
This work was financially supported by Ministero dell’Università e della
Ricerca Scientifica e Tecnologica (M.U.R.S.T.).
GASCO IVANO (*), BORGHI ALESSANDRO (**) & GATTIGLIO MARCO (*)
1
415
Meso- and microscopic relics of pre-S1 foliations developed
under eclogite facies metamorphism are widespread. The tectonic
contact between the ICM and the Zermatt-Saas type Units is
deformed by meso-scale D1 folds developed after eclogite facies
peak pressure conditions.
Instead, in the UTE, the S1 foliation developed under
greenschist facies conditions and the associated lineations strike
NW-SE in Gressoney Valley and E-W in the Orco and Susa
Valley.
In all the study areas the LTE is separated from the UTE by a
greenschist facies shear zone which is always later than the
development of the regional foliation S1 and developed during
top to SE sense of shear in the Orco Valley and Gressoney Valley
while it is marked by top to the W sense of shear in the Susa
Valley. This different orientation in the sense of shear is related
to the position of these shear zones relatively to the investigated
side of the Internal Crystalline Massifs.
D2 is always associated to the development of greenschist
facies shear zones separating the UTE from the LTE. In the Orco
and Gressoney Valleys this event developed isoclinal folds while
no corresponding folding stage was observed in the Susa Valley.
The following evolution is the same in all the three study
areas.
The D3 deformation phase is characterized by open to close
folds which rarely developed a new axial plane foliation in micarich
rocks. Their asymmetry shows top to SE sense of shear.
The D4 deformation phase shows NW-SE directed fold axes
with a fold asymmetry suggesting top to SW sense of shear in
Gressoney and Susa Valley while The in the Orco section D4
developed only macro-scale folds with high angle axial surfaces
dipping both SW and NE indicative of the presence of large scale
box folds.
INTERNAL CRYSTALLINE MASSIFS PT PATH
The petrographic analisys and pseudosection modelling of
two chemical systems (metabasites and metapelites) allowed
reconstructing a portion of the PT path followed by the ICM
during the Alpine orogenesis. In particular, well preserved
eclogite facies rocks (M1 and M2 assemblages) were investigated
to reconstruct the HP history of the ICM while re-equilibrated
rocks allowed to infer the PT conditions attained during the
development of the regional foliation (M3 to M4 assemblages).
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The M1 and M3 tectono-metamorphic stages are related to the
development of the pre-S1 and S1 foliations, respectively. The M2
assemblage is not ubiquitously developed and represents the first
decompressional stage after M1 and is never related to the
development of a new structural surface. It mainly consists of
pseudomorphs or of a static growth of minerals after the pre-S1
foliation. Finally, the M4 assemblage grew as rim over the M3
minerals (i.e. hornblende rimming actinolite, ilmenite rimming
rutile, oligoclase rimming albite) or overgrew the S1 regional
foliation (albite porphyroblasts overgrowing the S1 foliation
already defined by albite) and therefore can be considered as the
final stage of the M3 stage.
The comparison of the different PT path reconstructed for the
Fig. 1 – PT path reconstructed for the three study areas.
ICM (Fig. 1) enhances three interesting observations:
- firstly, the PT conditions for the development of the eclogite
facies pre-D1/M1 stage are different for all the ICM, especially
that of the northern Dora Maira Massif but all have equilibrated
along a 6-7 °C/km geothermal gradient typical for a subduction
zone The different peak pressure only depends from the depth
from which the tectonic slices were detached from the subducting
slab;
- secondly, the regional foliation D1/M1 developed under a 15-
25 °C/km geothermal gradient almost at the same P conditions (6-
9 kbar) while the T shows a wide range between 460 and 610 °C
mainly depending on the extent of the late re-heating stage;
- finally, Monte Rosa and Gran Paradiso Massif were affected
by a late thermal overprint of ca 50-60 °C while Dora-Maira
Massif underwent post eclogitic decompressional heating.
DISCUSSIONS AND CONCLUSIONS
Pseudosection modelling of the Alpine metamorphic assemblages
allowed reconstructing the Alpine PT path for the ICM. The
416
southern Monte Rosa and eastern Gran Paradiso reached higher
pressure during the pre-D1/M1 eclogite facies tectonometamorphic
stage around 24-27 kbar and 550-600°C while the
northern Dora-Maira was subducted to 20-21 kbar at 500-520 °C.
The exhumation paths are different too and are characterized by
cooling in the MR and GP while the DM registered a
decompressional heating. This first exhumation stage was
followed by the development of the regional foliation (D1/M3-M4
tectono metamorphic stage) at 6-9 kbar and 460-610 °C and the
MR and GP underwent a re-heating event of about 50-60 °C. On
the contrary, the northern DM did not register a late T increase
probably because it was already rather hot after the
decompressional heating. Therefore, the ICM show a different
HP evolution along a 6-7 °C/km subduction gradient while the reequilibration
event (D1/M3-M4 stage) is similar and took place in
the middle to lower crust (25-35 km) along an hotter geothermal
gradient (15-25 °C/km). The fact that all the ICM equilibrated at
HP along a similar subduction gradient is indicative that they
reached different depth in the subduction channel and then
returned towards the bottom of the crust and were re-equilibrated
at similar depth. The tectono metamorphic relationships between
the ICM and the Lower PZ indicate that tectonic coupling took
place during exhumation of the ICM after the pre-D1/M1-M2
tectono-metamorphic stage and before the development of the S1
regional foliation (D1/M3-M4 stage). PT conditions for tectonic
coupling are constrained by the lower stability of eclogite facies
assemblages (< 12-13 kbar according to BOUSQUET et alii, 1997)
and the development of the S1 regional foliation which therefore
took place between 9 and 13 kbar. After this event the ICM and
Lower PZ underwent the same tectono-metamorphic evolution.
The tectonic contact between the eclogite-bearing LTE and the
eclogite-free UTE developed after the S1 regional foliation at P <
6-8 kbar at middle crustal level (< 25 km) during extensional
tectonics in the upper portion of the orogenic wedge. The
reconstruction of the tectono-metamorphic evolution of three
different geological sections across the same structural levels
allowed showing that they shared a similar Alpine history since
the first exhumation stages after the eclogite facies
metamorphism.
REFERENCES
BOUSQUET R., GOFFÉ B., HENRY P., LE PICHON X. & CHOPIN C.
(1997) - Kinematic, thermal and petrological model of the
Central Alps: Lepontine metamorphism in the upper crust and
eclogitisation in the lower crust. Tectonophysics, 273, 105-127.
GASCO I., GATTIGLIO M. & BORGHI A. (2009) - Structural
evolution of different tectonic units across the Austroalpine-
Penninic boundary in the middle Orco Valley (Western Italian
Alps). J. Struct. Geol., 31, 301-314.
REDDY S.M., WHELEER J. & CLIFF R.A. (1999) - The geometry
and timing of orogenic extension: an example from the Western
Italian Alps. J. Metamorph. Geol., 17, 573-589.

_________________________
Crustal anatexis in the Higher Himalayan Crystallines of Eastern
Nepal: constraints on the P-T evolution of the Barun Gneiss
CHIARA GROPPO (*), FRANCO ROLFO (*) , RODOLFO CAROSI (**), CHIARA FRASSI (**), CHIARA MONTOMOLI (**),
PIERO PERTUSATI (**) & DARIO VISONÀ (°)
Key words: Barun Gneiss, channel flow model, Crustal anatexis,
Himalaya, P-T pseudosections, P-T evolution.
INTRODUCTION
Partial melting of deep continental crust may occur during
either prograde heating or decompression. Although the effect of
temperature on crustal melting has been widely investigated (e.g.
VIELZEUF &HOLLOWAY, 1988; PATIÑO DOUCE &JOHNSTON,
1991), only few experimental studies addressed the question of
the influence of pressure on crustal melting (e.g. AUZENNEAU et
alii, 2006). In spite of these limited number of studies,
decompression melting is a very common process, as testified by
the near-isothermal decompression paths of many regional-scale
migmatite terranes, that show evidence for progressive melting
from high-medium P (Ky stability field) to lower P (Sil field).
In the Higher Himalayan Crystallines of eastern Himalaya, the
structurally lowermost Barun Gneiss (and their laterally
equivalents Kangchenjunga Gneiss and Darjeeling Gneiss; see
GOSCOMBE et alii, 2006 for a review) is an east–west-trending, 6-
7 km thick, sequence of Grt-Kfs-Ky-Sil granulitic and migmatitic
metasediments, laterally continuous for at least 200 km along the
Himalayan chain, from eastern Nepal to Sikkim and Buthan.
Preliminary studies (POGNANTE &BENNA, 1993) suggest that
Barun Gneiss experienced partial melting during nearly
isothermal decompression from the Ky to the Sil stability field:
however, their P-T evolution is still poorly constrained. Recent
studies on the Namche Barwa Syntaxis (NBS) at the easternmost
margin of the Himalayan chain, ca. 1000 km east of the Barun
Gneiss type locality, have shown the existence of very similar
Grt-Kfs-Ky-Sil rocks.
The aims of this study are: (i) to reconstruct, using the most
(*) Dipartimento di Scienze Mineralogiche e Petrologiche, Università di
Torino, chiara.groppo@unito.it, franco.rolfo@unito.it
(**) Dipartimento di Scienze della Terra, Università di Pisa,
carosi@dst.unipi.it,
pertusati@dst.unipi.it
frassi@dst.unipi.it, montomoli@dst.unipi.it,
(°) Dipartimento di Geoscienze, Università di Padova, dario.visonà@unipd.it
417
recent petrological approaches, the P-T evolution of a still poorly
investigated high-grade Himalayan tectonometamorphic unit; (ii)
to recognise possible similarities between two different sectors of
the Himalayan chain (i.e. eastern Nepal and NBS), and eventually
demonstrate the existence of a HP-HT belt with similar
characteristics through the whole eastern sector of the Himalayas;
(iii) to discuss the resulting P-T evolution of the Barun Gneiss in
the framework of the “channel flow” model (BEAUMONT et alii,
2001) predicting the tectonic evolution of Himalaya.
PETROGRAPHY
The studied rocks outcrop along the Arun-Barun transect
toward the Nepalese Makalu base camp, in the sector between
Kauma to the south and Yangle Kharkha to the north across the
Shipton La and Tu La Pokhri. Two samples have been
petrologically investigated in detail. Samples #07-16 and #07-35
come from lower and upper structural levels respectively, and
mainly differ for the relative proportion of garnet and kyanite.
At the outcrop scale, Barun Gneisses typically consist of mmto
cm-thick leucocratic quartzo-feldspathic domains alternating
with millimetric dark biotite + plagioclase + sillimanite layers
which define a more or less continuous planar foliation (Fig. 1).
Two additional phases are always present in the Barun Gneisses:
(i) a pink-red garnet, occurring as millimetric to centimetric
porphyroblasts enveloped by the Bt+Pl+Sil foliation or occurring
within the leucocratic domains, and (ii) kyanite, that always
occurs as a relict phase corroded by Pl ± Bt. Barun Gneisses are
locally crosscut by decimetric-thick granitic dykes. Boudins of
calc-silicate fels (diopside + plagioclase + quartz ± garnet ±
scapolite) are locally included in the Barun Gneisses and are
enveloped by the regional foliation.
Several microstructures representing the evidence of meltproducing
or melt-consuming reactions have been recognised,
such as: (i) plagioclase and K-feldspar films around quartz
inclusions in garnet, with garnet showing equilibrium crystalline
faces toward these films: they are interpreted as pseudomorphs of
liquid-filled pores (e.g. HOLNESS &SAWYER, 2008) and suggest
that garnet grew during partial melting; (ii) garnet porphyroblasts
are locally crowded of very small polymineralic inclusions (up to
20 μm in diameter) with a negative-crystal shape, resembling the
“nanogranites” as defined by CESARE et alii (2009); (iii) kyanite
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is rimmed and corroded by a Pl ± Bt corona, suggesting that it
reacted with melt; (iv) Bt + Pl symplectites develop at the garnet
rim and are consistent with the final stages of back-reactions
involving melt crystallization.
Fig. 1 –Representative microstructures of the studied samples as seen under
optical microscope (Plane Polarized Light)
RESULTS
The P-T evolution of two Barun Gneiss samples has been
reconstructed using the petrologic approach of P-T
pseudosections. Calculations have been performed in the
NCKFMASTH system and the effects of possible episodes of
melt loss during the rocks evolution have been considered. Peak
and retrograde P-T conditions have been constrained combining
the observed modal proportions of phases and mineral
compositions, with modelled isomodes and compositional
isopleths. Results of the thermodynamic modelling suggest that
the studied Barun Gneisses experienced a similar clockwise P-T
evolution characterized by: (i) heating during decompression up
to peak-T conditions of 800°C at P=10 kbar (#07-16) and P=8
kbar (#07-35); (ii) a nearly isothermal decompression down to
7.5 kbar (#07-16) and 6.5 kbar (#07-35), when melt completely
crystallized; (iii) some melt loss occurred during the rocks
evolution, as testified by the preservation of the peak assemblage.
The P-T evolution reconstructed for the Barun Gneisses
shows similarities and differences with that proposed for the HP
anatectic metapelites of the NBS, suggesting that both represent
continental crust that experienced anatexis at different depths. As
418
concerning the Barun Gneiss in the framework of the HHC, our
metamorphic and petrologic data match well with the
expectations of the “channel flow” model (BEAUMONT et alii,
2001), including: (i) the clockwise shape of the P-T paths; (ii)
the estimated P at peak-T (our data: 10 to 8 kbar at 800°C;
model: 13 to 7 kbar at 800°C); (iii) the decreasing P structurally
upward, which defines a “normal” metamorphic sequence, in
contrast to the inverted metamorphic sequence occurring in the
lowermost MCTZ; (iv) the nearly-isothermal exhumation,
reflecting the progressive exhumation of rocks that have been
entrained in the deep, high-T region of the channel, where they
experience gradually declining P at nearly constant T.
REFERENCES
AUZENNEAU E., VIELZEUF D. & SCHMIDT M.W. (2006) –
Experimental evidence of decompression melting during
exhumation of subducted continental crust. Contrib. Mineral.
Petr., 152, 125-148.
BEAUMONT C.R.A., JAMIESON M.H., NGUYEN M.H. & LEE B.
(2001) – Himalayan tectonics explained by extrusion of a
low-viscosity channel coupled to focused surface denudation.
Nature, 414, 738-742.
CESARE B., FERRERO S., SALVIOLI-MARIANI E., PEDRON D. &
CAVALLO A. (2009) – “Nanogranite” and glassy inclusions:
the anatectic melt in migmatites and granulites. Geology, 37
(7), 627-630.
GOSCOMBE B., GRAY D. & HAND M. (2006) – Crustal
architecture of the Himalayan metamorphic front in eastern
Nepal. Gondwana Res., 10, 232-255.
HOLNESS M.B. & SAWYER E.W. (2008) – On the
pseudomorphing of melt-filled pores during the
crystallization of migmatites. J. Petrol., 49, 1343-1363.
PATIÑO DOUCE A.E. & JOHNSTON A.D. (1991) – Phase equilibria
and melt productivity in the pelitic system: implications for
the origin of perallumionus granitoids and aluminous
granulites. Contrib. Mineral. Petr., 107, 202-218.
POGNANTE U. & BENNA P. (1993) – Metamorphic zonation,
migmatization, and leucogranites along the Everest transect
(Eastern Nepal and Tibet): record of an exhumation history.
In: P.J. TRELOAR & M.P. SEARLE (Eds.) - Himalayan
Tectonics. Geol. Soc. London, SP., 74, 323–340.
VIELZEUF D. & HOLLOWAY J.R. (1988) – Experimental
determination of the fluid-absent melting relations in the
pelitic system. Contrib. Mineral. Petr., 98, 257-276.

Geometry, kinematics, and non coaxiality of the flow in the Tibetan
Sedimentary Sequence during the activity of the South Tibetan
Detachment System (southern Tibet, China): insight into the
exhumation of the Himalayan belt
CHIARA MONTOMOLI (*), RODOLFO CAROSI (*), ALESSIO CARULLI (*), ERWIN APPEL (**), ISTVÀN DUNKL (°),
BERNARD LEISS (°), RACHIDA EL BAY (**) & DING LIN (°°)
Key words: Deformation temperatures, finite strain analyses,
Himalaya, non-coaxial deformation, South Tibetan
Detachment System, Tibetan Sedimentary Sequence.
INTRODUCTION
The South Tibetan Detachment System (STDS) is one of the
main tectonic discontinuity of the Himalayan belt well known
since the eighties (BURG et alii, 1983; BURCHFIEL et alii, 1992).
It is characterized by a lower top-to-the NE low-angle ductile
shear zone and by an upper low-angle brittle fault with the same
sense of movement (CAROSI et alii, 1998; SEARLE &GODIN,
2003; JESSUP et alii, 2006, 2008). The STDS puts in contact the
high-grade metamorphic rocks belonging to the Higher
Himalayan Crystallines (HHC) with the upper very-low grade to
non metamorphic rocks of the overlying Tibetan Sedimentary
Sequence (TSS).
Fig. 1 – STDS cropping out in the study area; on the left grey rocks are sillbt
schists of the Greater Himalayan Sequence, yellowish rocks on the right
are Ordovician limestone of the Tibetan Sedimentary Sequence.
_________________________
(*) Dipartimento di Scienze della Terra, Università di Pisa,
montomoli@dst.unipi.it
(**) University of Tübingen, Germany
(°) University of Göttingen, Germany
(°°) Institute of Tibetan Plateau Research, CAS, Beijng, China
419
During this work we mainly focused on the study of the
geometry, kinematic and deformation temperatures of the
hanging-wall rocks of the STDS represented by the Paleozoic
portion of the TSS.
We sampled a 1,5 km thick section of the TSS made up by
Paleozoic sequence cropping out above the STDS in Dinggye-
Saìer area (South Tibet).
The Ordovician limestone, at the bottom of the unit, is
characterized by a ductile heterogeneous deformation during
which calcmylonites developed. Centimetric to decimetric highstrain
zones, post-dating D1 distinct isoclinal folds, are associated
to a mylonitic foliation striking parallel to the STDS and dipping
few degrees to the North. Kinematic indicators indicate a top-tothe
NE sense of shear.
Microfabric analysis of calcite on marbles and calc-mylonites
show shape and lattice preferred orientations as well as grain size
reduction within layers of cm-thickness
Moving upward in the sequence, primary sedimentary
structures are still well recognizable and there is a quite sharp
transition to very-low grade deformation mechanisms where
pressure solution is predominant.
A strain increase has been detected along the section moving
from top to bottom. Finite strain analyses have been performed in
marbles along the section and the estimated axial ratios of the
principal XZ sections of the strain ellipsoid vary from 2.1 to 1.5
moving from bottom to top
Deformation temperatures have been constrained at 350°C by
the calcite-dolomite geothermometer for Ordovician
calcmylonites at the bottom of the TSS. In addition the detailed
study of syntectonic twinning in calcite crystals (BURKHARD,
1992) pointed out a decreasing deformation temperature of about
150°C moving from the bottom to the top of the study section.
Peak metamorphic temperatures, of at least 325°C, for
samples coming from the bottom of the sequence are supported
also by the dominance of magnetic remanence unblocking at the
Curie temperature of pyrrhotite.
To estimate the component of pure and simple shear acting
simultaneously during deformation the study vorticity kinematic
number has been performed.
Vorticity kinematic numbers (Wk) have been derived from
lattice preferred orientations (LPOs) of calcite, which were
determined by means of an X-ray goniometer on suitable
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samples. Wk highlighted an equal contribution of pure and simple
shear components during deformation.
CONCLUSIONS
The estimated deformation temperatures point out an apparent
very high thermal gradient for the study section of about
100°C/km.
Fig. 2 – Mylonitic foliation in the Ordovician limestones (lower part of TSS).
Two main facts can be responsible: 1) heating effect linked to
the exhuming hot (high-grade metamorphic) rock of the
underlying HHC coupling with the colder TSS rocks; 2) strong
vertical shortening due to a combination of pure and simple shear
components during deformation causing a strong telescoping of
the isograds both within the HHC (LARSON &GODIN, 2009) and
at the bottom of the TSS (CAROSI et alii, 2007; MONTOMOLI et
alii, 2009).
REFERENCES
BURCHFIEL B.C., CHEN Z., HODGES K.V., LIU Y., ROYDEN L.H.,
CHANGRONG D. & XU L. (1992) - The South Tibetan
Detachment System, Himalayan Orogen: extension
contemporaneous with and parallel to shortening in a
collisional mountain belt. Geol. S. Am. S., 269, 41.
BURKHARD M., (1992) - Calcite twins, their geometry,
appearance and significance as stress-strain markers and
indicators of tectonic regime: a review. J. Struct. Geol., 20, 1-
18.
CAROSI R., LOMBARDO B., MOLLI G., MUSUMECI G. & PERTUSATI
P.C. (1998) - The South Tibetan Detachment System in the
Rongbuk valley, Everest region. Deformation features and
geological implications. J. Asian Earth Sc., 16, 299-311.
420
CAROSI R., MONTOMOLI C. & VISONÀ D. (2007) - A structural
transect in the Lower Dolpo: Insights on the tectonic
evolution of Western Nepal. J. Asian Earth Sc., 29, 407-423
JESSUP M.J., LAW R.D., SEARLE M.P. &. HUBBARD M.S. (2006) -
Structural evolution and vorticity of flow during extrusion
and exhumation of the Greater Himalayan Slab, Mount
Everest Massif, Tibet/Nepal: implications for orogen-scale
flow partitioning. In: R.D. LAW, M.P. SEARLE & L.
GODIN, (Eds.) - Channel Flow, Ductile Extrusion and
Exhumation in Continental Collision Zones. Geol. Soc., SP.,
London, 268, 379–413.
JESSUP M.J., COTTLE J.M., SEARLE M.P., LAW R.D., NEWELL
D.L., TRACY R.J. & WATERS D.J. (2008) - P–T–t–D paths of
Everest Series schist, Nepal. J. Metamorph. Geol., 26, 717-
739.
LARSON K.P. & GODIN L. (2009)- Kinematics of the Greater
Himalayan sequence, Dhaulagiri Himal: implications for the
structural framework of central Nepal. J. Geol. Soc., 166, 25-
43.
MONTOMOLI C., CAROSI R., CARULLI A., APPEL E., DING L.,
DUNKL I., EL BAY R. & LEISS B. (2009) – Deformation,
kinematics and metamorphism of the South Tibetan
Detachment System in the Dinggye section (Southern Tibet).
24 TH Himalaya-Karakorum-Tibet Workshop, Pechino, 11-14
agosto 2009, 29-30.
SEARLE M.P. & GODIN L. (2003) - The south tibetan detachment
system and the manaslu leucogranite: a structural
reinterpretation and restoration of the Annapurna-Manaslu
Himalaya, Nepal, J. Geol., 111, 505-524.

Structural and metamorphic architecture of the Himalayas in the
Kangchenjunga area (far-Eastern Nepal)
Key words: Himalaya, Kangchenjunga transect, structural
architecture, tectono-metamorphic evolution.
INTRODUCTION
The eastern Himalayan collisional belt comprises few E-W
trending lithotectonic units which are, from south to north and
from lower to upper structural levels: the sub-Himalaya, the
Lesser Himalayan Sequence (LHS), the Main Central Thrust
Zone (MCTZ), the Higher Himalayan Crystallines (HHC) and the
Tibetan Sedimentary Series (see GOSCOMBE et alii, 2006 for a
review).
This contribution presents new data on the tectonometamorphic
architecture of the Himalayan thrust belt in fareastern
Nepal at the western flank of the Kangchenjunga massif,
the easternmost Himalayan eight-thousander. Structural and
petrographic studies, and related field mapping, were performed
in the Tamor-Ghunsa Khola and Simbua-Kabely Khola area,
following two traverses across the northern and north-eastern
flanks of the Taplejung tectonic Window (or Tamor Khola dome
in SCHELLING, 1992) where the LHS is exposed as a regional
antiformal structure beneath the MCTZ and the HHC.
Along the studied transects, the lithotectonic units show, at a
regional scale, layering and composite foliations variably dipping
from the N-NE to the W.
PETROGRAPHIC DATA
In the study area, the LHS mainly consists of metasediments
with widespread occurrence of fine-grained pale grey schists and
slates. The upper structural levels of the LHS are represented by
quartz-sericite and chlorite-sericite schists locally garnatiferous,
quartzites, and intercalated levels of augen gneisses (outcropping
_________________________
(*) CNR-Istituto di Geoscienze e Georisorse, UO Torino,
p.mosca@csg.to.cnr.it
(**) Dipartimento di Scienze Mineralogiche e Petrologiche, Università
degli Studi di Torino, chiara.groppo@unito.it, franco.rolfo@unito.it
PIETRO MOSCA (*), CHIARA GROPPO (**) & FRANCO ROLFO (*) (**)
421
north of Furumba village). These augen gneisses (Sisne Khola
augen gneiss in SCHELLING, 1992) are comparable in lithology
and structural position to the Ulleri gneiss in central Nepal (e.g.
LE FORT, 1975). Moving upwards, a few km-thick sequence of
metapelitic schists and gneisses has been observed. This sequence
is characterized by a typical inverted metamorphism, passing
from the structurally lower garnet ± kyanite ± staurolite twomicas
schists to the structurally upper two-micas, garnet and
kyanite-bearing migmatitic gneisses. This sequence has been
interpreted as the strongly condensed and thinned equivalent of
the MCTZ according to the scheme of GOSCOMBE et alii (2006).
Above the MCTZ, the HHC is exposed over more than 40 km
up to the Tibetan border. From a lithological and metamorphic
point of view the HHC may be divided in: (i) a lower portion,
mainly consisting of garnet-K-feldspar-kyanite-sillimanite
anatectic paragneisses (Jannu-Kangchenjunga Gneiss in
SCHELLING, 1992 and GOSCOMBE et alii 2006), with minor
intercalations of impure marbles and calc-silicate gneisses; (ii) a
middle portion, consisting of similar anatectic paragneisses but
characterized by the lack of kyanite and the abundant occurrence
of cordierite; (iii) an upper portion, characterized by the
occurrence of sillimanite-bearing anatectic orthogneisses with
widespread intrusions of tourmaline- and/or andalusite-bearing
leucogranites.
STRUCTURAL DATA
Meso- and micro-structural data emphasise the existence of a
several kilometres thick zone of high ductile to ductile-brittle
strain centred on the inverted metamorphic sequence of the
MCTZ, although an intense mylonitic deformation has also been
observed in the upper portion of the LHS and in the lower
portions of the HHC. Kinematic indicators show a consistent topto-south
sense of shear, related to the juxtaposition of the HHC
over the LHS. From the kinematic point of view, it is difficult to
clearly define the lower and upper boundaries of the MCTZ,
these being not marked by a single thrust or a set of adjacent
discrete thrusts. The boundaries are identified a zones of
pronounced increasing in deformation across the upper portions
of the LHS and the lower portions of the HHC. More in detail,
the structurally uppermost portion of the LHS consists of
phyllonites and mylonitic schists plus augen gneisses displaying a
SESSIONE 12

SESSIONE 12
mylonitic deformation with strong flattening and stretching of the
K-feldspar porphyroclasts. The lower portions of the HHC show
evidences of pervasive ductile shearing (folding and meso-scale
shear zones with top-to-south sense of movements). Moving
upwards, towards the middle portions of the HHC, ductile highstrain
is mainly concentrated in discrete, top-to-south metric to
decametric shear zones.
Finally, two later phases of folding, characterized by roughly
N-S and ENE-WSW trending axes, developed under low-grade
metamorphic conditions. These folds are likely to be associated
to the final exhumation stages and their geometrical interference
is inferred to control the present-day regional antiformal shape of
the LHS beneath the MCTZ and the HHC.
REFERENCES
GOSCOMBE B., GRAY D. & HAND M. (2006) – Crustal
architecture of the Himalayan metamorphic front in eastern
Nepal. Gondwana Res., 10, 232-255.
LE FORT P. (1975) - Himalaya: the collided range. Present
knowledge of the continental arc. Am. J. Sci., 275A, 1–44.
SCHELLING D. (1992) – The tectonostratigraphy and strcucture of
the eastern Nepal Himalaya. Tectonics., 11 (5), 925-943.
422

Geological map of Chomolungma, Cho-Oyu and Makalu area
(Nepal-Tibet)
PIERO CARLO PERTUSATI (*), BRUNO LOMBARDO (**), RODOLFO CAROSI (*), CHIARA FRASSI (*),
CHIARA GROPPO (°), DAVID IACOPINI (*), GIANCARLO MOLLI (*), CHIARA MONTOMOLI (*),
GIOVANNI MUSUMECI (*), FRANCO ROLFO (°) & DARIO VISONA’ (°°)
Key words: Cho-Oyu, Geological Map, Himalaya
Chomolungma, Makalu HHC South Tibetan Detachment.
The geology of Chomolungma (Mt. Everest) Cho-Oyu and
Makalu area (Nepal-Tibet) will be presented by exposition of a
geological map at the scale 1:100.000 in a preliminary version.
The area covered by the map comprises the Region of
Chomolungma extending from the Northern Nepal to the
Southern Tibet.
There some of the most important geological structures (Main
Central Thrust and South Tibetan Detachment) and tectonic Units
(Higher Himalayan Cristalline-HHC and Tibetan Sedimentary
Sequence-TSS) of the Himalayan chain have been investigated in
the years 1990-2010 by the Italian researchers. Legend, tectonic
scheme, geological cross sections complete the geological map.
_________________________
(*) Dipartimento di Scienze della Terra, Università di Pisa,
pertusati@dst.unipi.it ; carosi@dst.unipi.it
(**) IGG-CNR Torino
(°) Dipartimento di Scienze della Terra, Università di Torino
(°°) Dipartimento di Mineralogia e Petrologia, Università di Padova
423
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SESSIONE 12
Which are the driving factors to facilitate exhumation during active
subduction? Suggestions by numerical modelling.
Key words: Crustal exhumation, mantle wedge hydration,
numerical simulation, subduction zones.
INTRODUCTION
Studies on high-pressure (HP) and ultrahigh-pressure (UHP)
rocks exposed in orogenic belts linked to collisional margin show
that nappes of oceanic and continental deeply subducted crust can
be exhumed to shallow structural levels. In particular, during
ocean-continent-type subduction, the crustal material dragged
into subduction channel is composed chiefly by oceanic crust and
trench sediments, continental slices belonging to subducting plate
[microcontinent (RING & LAYER, 2003) or linked to early
continental collision (CHEMENDA et alii, 1995)] or crustal slices
tectonically eroded from the overriding plate (ablative
subduction) (TAO &O’CONNELL, 1992; MAROTTA &SPALLA,
2007). Several models have been developed, during last 20 years,
to analyse exhumation of subducted crustal material. They can be
resumed on five main mechanisms: a) crust-mantle delamination
(CHEMENDA et alii, 1995), b) slab break-off (ERNST et alii,
1997), c) slab retreat (RING &LAYER, 2003) and roll-back slab
(BRUN &FACCENNA, 2008) and d) decoupling of two main
ductile layers (YAMATO et alii, 2008), in which the exhumation is
mainly driven by negative buoyancy and/or faulting and e)
subduction-channel flow (GERYA &STOCKHERT, 2005) in which
the exhumation is driven by the upwelling flow developed a lowviscosity
mantle wedge. Only channel flow takes into account
recirculation of crustal slices dragged to high depth by ablation
within pre-collisional subduction zones.
To study the effects of subduction rate, slab dip and mantle
rheology changes on channel flow efficiency a parametric
analysis is proposed.
_________________________
MANUEL RODA (*), ANNA MARIA MAROTTA (*) & MARIA IOLE SPALLA (**)
(*) Dipartimento di Scienze della Terra “Ardito Desio”, Università di
Milano,
anna.maria.marotta@unimi.it
(**) Dipartimento di Scienze della Terra “Ardito Desio”, Università di
Milano
424
NUMERICAL MODELLING AND DISCUSSION
The contribution presents the results of a set of numerical
simulation with different subduction rates, slab dips and mantle
rheology represented by dry dunite and dry olivine flow laws.
Numerical model predictions are finally compared to some PT
paths obtained from ancient and actual subduction zones with
different slab dips and convergence velocities.
The numerical tool is a 2D thermodynamic code (SubMar,
MAROTTA et alii, 2006), in which the equations of continuity,
momentum and energy conservation are solved by finite element
method. The model represents a strongly coupled ocean-continent
convergent system, affected by slab dehydration and progressive
mantle wedge serpentinization. Erosion and sedimentation
processes are also accounted; shear heating is not taken into
account (MAROTTA &SPALLA, 2007; MEDA et alii, 2010). We
fixed a constant convergence velocity (varying from 1 to 10
cm/y) at the top of the oceanic plate and up to 80 km depth in the
trench zone, along different dip planes (30°, 45° and 60°), in
order to force the subduction.
The parametric analysis performed for ocean/continent
convergent systems points out that ablation is a highly efficient
process for dragging large masses of upper and lower continental
crust, belonging to the overriding plate, to deep levels. In
particular, ablative subduction is much more efficient for low slab
dip due to the stronger coupling between the oceanic and
continental plates. The subduction rate has also been observed to
have a moderate influence on ablative subduction efficiency.
In addition to slab dip, in 30° simulations, the similarity of
trends in hydration area and exhumation percentage with respect
to subduction rates suggests that the width of the hydration area is
correlated to the amount of exhumed material.
Maximum values of exhumation percentage are predicted for
intermediate subduction rates except in the 60° simulations,
where the peak values are predicted for the lowest velocities (1
cm/y).
The maximum values of Pmax are recorded by markers of 45°
subductions, and the lowest values are predicted by 60°
subduction markers. Just as for the exhumation percentage
values, the maximum Pmax is also generally predicted to occur for
medium subduction rates (3-5 cm/y) in low and intermediate dip

simulations (30° and 45°).
TPmax and Tmax values display a positive correlation with the
subduction angle and a low variation with subduction rate. In 30°
simulations thermal gradients along the mantle wedge are low and
TPmax and Tmax values are quite similar for similar subduction
rates. In contrast, in 60° dip, thermal gradients increase along the
mantle wedge, and strong thermal and mechanical erosion occur
at the base of the overriding plate.
The accrectionary prism is strongly affected by the subduction
rate and the subduction dip: increasing both parameters decreases
the width of the prism and is accompanied by an increase in
trench depth.
Variations in mantle rheology affect the slab geometry for low
and moderate subduction dips. Mantle viscosity has a positive
correlation with Pmax values due to the strong viscosity gradient
generated at the transition between hydrated and dry mantle.
Natural data and model predictions are in good agreement: the
thermal states simulated for ablative subduction with a hydrated
mantle wedge justify the natural PT estimates obtained on
continental crust units involved in ocean/continent subduction
systems. Similarly, the exhumation rates obtained from analysis
of PTt-paths are more compatible with natural ones than those
obtained from the upwelling flow vector which could justify only
a transient exhumation stage. In general, numerical simulations
and natural data show exhumation rates lower then subduction
rates. On the basis of these results, we propose that ablative
subduction of the overriding continental plate is a good precollisional
mechanism for the subduction and exhumation of
continental crust from the overriding plate. In contrast to
collisional processes such as slab retreat, rollback slab or
microcontinent collision, mantle wedge dynamics facilitates the
exhumation of ablated and deeply buried crustal fragments during
active subduction.
REFERENCES
BRUN J.-P. & FACCENNA C. (2008) - Exhumation of highpressure
rocks driven by slab rollback. Earth Planet. Sc. Lett.,
272,1–7.
CHEMENDA A. I., MATTAUER M., MALAVIEILLE J. & BOKUN A. N.
(1995) - A mechanism for syn-collisional rock exhumation
and associated normal faulting: Results from physical
modelling. Earth Planet. Sc. Lett., 132, 225–232.
ERNST W.G., MARUYAMA S. & WALLIS S. (1997) - Buoyancydriven,
rapid exhumation of ultrahigh-pressure
metamorphosed continental crust. Proc. Natl. Acad. Sci., 94
9532-9537.
425
GERYA T.V. & STOCKHERT B. (2005) - Two-dimensional
numerical modeling of tectonic and metamorphic histories at
active continental margins. Int. J. Earth Sci., 95(2), 250-274 .
MAROTTA A.M., SPLTA E. & RIZZETTO C. (2006) - Gravity
signature of crustal subduction inferred from numerical
modelling. Geophys. J. Int., 166, 923–938.
MAROTTA A.M. & SPALLA M.I. (2007) - Permian-Triassic high
thermal regime in the Alps: Result of late Variscan collapse
or continental rifting? validation by numerical modeling.
Tectonics, 26, doi:10.1029/2006TC002047.
MEDA M., MAROTTA A.M. & SPALLA M.I. (2010) - The role of
mantle hydration into the continental crust recycling in the
wedge region. Geol. Soc. SP., London, 332 (1), 149–172.
RING U. & LAYER P.W. (2003) - High-pressure metamorphism in
the Aegean, eastern Mediterranean: Underplating and
exhumation from the Late Cretaceous until the Miocene to
Recent above the retreating Hellenic subduction zone.
Tectonics, 22 (3), doi:10.1029/2001TC001350.
TAO W.C. & O’CONNELL R.J. (1992) - Ablative subduction: A
two-sided alternative to the conventional subduction model.
J. Geophys. Res., 97 (B6), 8877 – 8904.
YAMATO P., BUROV E., AGARD P., POURHIET L.L. & JOLIVET L.
(2008) - HP-UHP exhumation during slow continental
subduction: Self-consistent thermodynamically and
thermomechanically coupled model with application to the
Western Alps. Earth Plan. Sc. Lett., 271, 63–74.
SESSIONE 12

SESSIONE 12
Constrain by low-temperature thermochronometers in the evolution
of the Central Apennines
Key words: Central Apennines, low-temperature
thermochromoneters, Sangro-Volturno line.
INTRODUCTION
Orogenic belts are subjected to burial and uplift processes,
conditioned by transversal tectonic lines and thickness of the
involved stratigraphic succession (e.g., BEGIN & SPRATT,
2002). In order to constrain the burial/exhumation pattern in the
external orogenic belts, fundamental information are provided by
low-temperature thermochronometers, as apatite fission track, (U-
Th)/He analysis and vitrinite reflectance.
We discuss the role of the Sangro-Volturno transversal line,
which signs the separation between the Central and Southern
Apennine, combining fission track, vitrinite reflectance data
(RUSCIADELLI et alii, 2005) and (U-Th)/He analysis with the
geological and structural analysis from the Central and Southern
Apennines, across the Sangro-Volturno line.
GEOLOGICAL SETTING
The Apennines are a fold-and-thrust belt formed in the Late
Oligocene-Pleistocene and characterized by strong structural
elevation corresponding to maximum shortening (30 km) in the
Gran Sasso-Adriatic transect; shortening decrease southward till
less than 10 km, corresponding to the Frosolone-Gargano area of
the Southern Apennines (CALAMITA et alii, 2005, and references
therein).
The Central and Southern Apennines differ for the involved
paleogeographic domains, structural setting, geodynamic
evolution and paleomagnetic behaviour (e.g., CIARAPICA &
PASSERI, 2002; SATOLLI & CALAMITA, 2008). The Sangro-
Volturno transversal line (LOCARDI, 1982) signs the separation
between the Central and the Southern Apennines. The Plio-
Quaternary frontal thrusts are buried under the pre-Adriatic basin
discordant succession or under allochthonous units, north and
south of the Sangro-Volturno ramp, respectively.
_________________________
SARA SATOLLI (*), MAURO GABRIELE VIANDANTE (*) & FERNANDO CALAMITA (*)
(*) Dipartimento di Scienze, Università “G.d’Annunzio” of Chieti-Pescara,
s.satolli@unich.it
426
THERMOCHRONOLOGICAL DATA FROM THE
CENTRAL APENNINES
Apatite Fission Track, Vitrinite Reflectance and Fluid
Inclusion analyses indicate a continuous exhumation and uplift in
the Apennines from 14 Ma to the present. The inferred
exhumation and uplift range from 5-6 km in the inner zones of the
Northern Apennines (VENTURA et alii, 2001), to 3-4 Km in the
outer zone of the Northern (ZATTIN et alii, 2002), Central
(RUSCIADELLI et alii, 2005) and Southern Apennines (CORRADO
et alii, 2002).
Vitrinite and Fission tracks from the Central Apennines (Fig.
1) indicate two major exhumation events (RUSCIADELLI et alii,
2005), representing the buckling flexure of the Adria passive
margin into a foreland tectonic system and the beginning of the
exhumation phase of the outer zones of the central Apennines
during the Pliocene–Quaternary frontal thrust development.
Computed paleoburial is 3000-3500 m for the first recognized
event (35-15 Ma) and 2500-3000 m for the second event (5-1
Ma). Such conservative paleogradient imply a minor thickness to
be removed. However, also considering extreme
paleotemperatures and paleogradients (e.g., 35°C and 45°C/km,
respectively), a kilometric burial is requested.
Furthermore, (U-Th)/He data show a system closing age at ca.
2.5 Ma (50°C isotherm, representing the lower HePRZ limit) and
allowed us to constrain the timing of the turning points of the
Middle Pliocene exhumation event recognized in the analysed
area by RUSCIADELLI et alii (2005).
DISCUSSION AND CONCLUSION
AFTA, VR and (U-Th)/He data allowed us to define the role of
the Sangro-Volturno thrust ramp in the Neogene-Quaternary
Central Apennines evolution.
Maximum paleotemperature values documents a uniform low
level of maturation and, integrated with geological, structural and
paleomagnetic data from the literature, suggest the presence of
Ligurian allochthonous unit all over the Central and Southern
Apennines, eroded during the Middle Pliocene due to the
Pliocene-Quaternary frontal thrusts development (according to
RUSCIADELLI et alii, 2005). The Pliocene-Quaternary frontal

thrust record higher growth in the Central Apennines
(hangingwall of the Sangro-Volturno oblique thrust ramp) with
respect to the Southern Apennines, as indicated by maximal
values of exhumation, structural elevation and thickness of the
Pliocene foredeep siliciclastic deposits.
The first (U-Th)/He data from the Central Apennines confirm
the Middle Pliocene exhumation event detected by RUSCIADELLI
et alii (2005) and allowed us to constrain two segments with
different slope in the exhumation path. Considering a geothermal
paleogradient of 20°C/km, the first segment, between 3.5 Ma and
2.5 Ma, is characterized by a ca. 30°C cooling and corresponds to
1.5 mm/yr exhumation rate; the second segment, from 2.5 Ma to
present, is characterized by a ca. 50°C cooling and corresponds to
0.5 mm/yr exhumation rate.
Maximum exhumation in the hangingwall of the Sangro-
Volturno oblique thrust ramp brought the Apennine carbonate
units to crop out, where maximum amount of shortening in the
Central Apennines are documented. Instead, the frontal Plio-
Quaternary thrusts are buried by the Lagonegro-Molise
Fig. 1 – Simplified geological and structural map of the study area. White
circles represent AFTA and/or VR sample locations; grey circles represent (U-
Th)/He samples location.
427
allochthonous units in the Southern Apennines, in the footwall of
the Sangro-Volturno oblique ramp.
The reconstructed exhumation history agrees with a tectonic
style characterized by lithospheric significance of the Sangro-
Volturno oblique thrust ramp of the Pliocene-Quaternary frontal
thrusts, which caused the strong uplift of the Central Apennines.
REFERENCES
BÉGIN N.J. & SPRATT D.A. (2002) - Role of transverse faulting in
along-strike termination of Limestone Mountain Culmination,
Rocky Mountain thrust-and-fold belt, Alberta, Canada. J.
Struct. Geol., 24, 689-707.
CALAMITA F., ESESTIME P. & VIANDANTE M. G. (2005) - Tectonic
setting of the Central-Southern Apennines. Rend. Soc. Geol.
It., 1, 66-68.
CIARAPICA G. & PASSERI L. (2002) - The palaeogeographic
duplicity of the Apennines. Boll. Soc. Geol. It., Vol. Spec., 1,
67-75.
CORRADO S., INVERNIZZI C. & MAZZOLI S. (2002) - Tectonic
burial and exhumation in a foreland fold and thrust belt: the
Monte Alpi case history (Southern Apennines, Italy). Geodin.
Acta, 15, 159-177.
LOCARDI E. (1982) - Individuazione di strutture sismogenetiche
dall'esame dell'evoluzione vulcano-tettonica dell'Appennino e
del Tirreno. Mem. Soc. Geol. It., 24, 569-596.
RUSCIADELLI G., VIANDANTE M.G., CALAMITA F. & COOK A.C.
(2005) - Burial-exhumation history of the central Apennines
(Italy), from the foreland to the chain building:
thermochronological and geological data. Terra Nova, 17,
560-572.
SATOLLI S. & CALAMITA F. (2008) - Differences and similarities
between the central and the southern Apennines (Italy):
Examining the Gran Sasso versus the Matese-Frosolone
salients using paleomagnetic, geological, and structural data.
J. Geophys. Res., 113, doi:10.1029/2008JB005699.
VENTURA B., PINI G.A. & ZUFFA G.G. (2001) - Thermal History
and exhumation of the Northern Apennines (Italy): evidence
from combined apatite fission track and vitrinite reflectance
data from foreland basin sediment. Basin Res., 13, 435-448.
ZATTIN M., PICOTTI V. & ZUFFA G.G. (2002) - Fission-track
reconstruction of the front of the northern Apennine thrust
wedge and overlying Ligurian unit. Am. J. Sci, 302, 346-379.
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A detrital apatite fission-track study on the sedimentary successions
of the Valdelsa and Mugello basins, Northern Apennines, Italy
FRANCESCA TANGOCCI (*), MARIA LAURA BALESTRIERI (*) & MARCO BENVENUTI (**)
Key words: Detrital thermochronology, exhumation,
intermontane basins, lagtime .
The Valdelsa and Mugello basins are two of the Neogene to
Quaternary intermontane basins that developed on the western
flank of the Northern Apennine. These basins are elongated
parallel to the NW-SE Apenninic mountain trend and are
separated from each other by transverse morphotectonic
lineaments.
In the Valdelsa and Mugello basins, samples from the bedrock
and from the sedimentary succession were analysed and
compared to asses the role played by tectonics and climate in
shaping the succession and to reconstruct time and modality of
the exhumation of the bounding ridges.
The Valdelsa basin is a NW-SE trending depression filled
with more than 2000 m of Mio-Pliocene continental to shallow
marine deposits. It is located ca. 20 km south-west of Florence
and has a length of 60 km and width of 25 km. It is bounded to
SW by the Mid Tuscan Ridge and to the NE and SE by the M.
Albano- Monti del Chianti ridge. The latter separates the
Valdelsa basin from the sub-parallel Florence basin. The bedrock
of the Valdelsa basin consists of Ligurian Units (Jurassic-
Eocene) which were deformed during Cretaceous – Eocene
subduction-related orogenic phase. They tectonically rest onto the
Tuscan Units. The Tuscan Units are represented by the typical
turbidite successions, which filled the Apennine foredeep since
the late Oligocene (BENVENUTI et alii, 2007; DEL CONTE, 2007).
Eighteen samples were collected from 3 different stratigraphic
sections representative of the northern, central-southern and
southern portions of the Valdelsa basin and their source regions,
respectively. Eight samples were collected in the bedrock: four
samples from the Macigno Formation (Tuscan Units) and the
other from the sandstone and mudstone of the Ligurian units.
Only one sandstone sample from the Ligurian Units yielded some
apatites with a Central FT ages of 23.3±13.5 Ma. Samples from
_________________________
(*) Istituto di Geoscienze e Georisorse, CNR, balestrieri@igg.cnr.it
(**) Dipartimento di Scienze della Terra, Università di Firenze
This study is part of the EUROCORES Project: Coupled climatic/tectonic
forcing of European topography revealed through thermochronometry –
THERMOEUROPE of the European Science Foundation, and was funded
by the C.N.R.
428
the Macigno Fm yielded FT ages varying between 7.8±1.2 and
10.8±2.0 Ma. The grain-age distributions of Valdelsa Basin
sediment samples are generally characterized by two components,
one younger peak (P1) varying between 5.5±2.8 and 9.5±1.0 Ma
and one older peak (P2) varying from 15.0±8.0 and 41.0±10 Ma.
The average lagtime of the P1 component of the Valdelsa Basin
samples is ca. 4 Ma (RUIZ et alii, 2004). By dividing the
estimated depth of closure (Zc) of the used chronological system
by the lagtime, a mean exhumation rate of the source region can
estimated. In our case, we estimate a mean exhumation rate of
0.7-0.9 mm/yr.
By comparison with the bedrock ages we attribute the P1
population to the Macigno Fm and the P2 population to the
Ligurian Units. In the three stratigraphic sections, the trends of
the lagtime of P1 peak and of the variation in size of P2 peak
revealed that: i) the Macigno Fm was exposed in M. Albano –
Monti del Chianti ridge since at least the latest Messinian-early
Zanclean; ii) the basal portion of the southern succession likely
records a shift toward humid conditions (transgression Miocene-
Pliocene boundary); iii) the southern portion of the Monti del
Chianti ridge was actively rising from latest Messinian to middle
Zanclean, than it stopped while the northern portion started to
rise; iv) the M. Albano ridge started to rise and represented a
topographic barrier only after the early-middle Piacenzian; v) at
the top of the central-southern section a period of enhanced
erosion due to the coupling of strong tectonic activity and cold
climate conditions (2.6 Ma) is likely recorded.
The Mugello basin is a WNW-ESE trending depression filled
with 600 m of fluvio-lacustrine late Pliocene (?)–Pleistocene
deposits. It is located ca. 30 km north-east of Florence and has a
length of 25 km and width of 15 km. It is bounded to N-NE by
the Alpe di San Benedetto and to NW-SW by the Monti della
Calvana- Monte Giovi ridge. The basin is located near the main
Apennine watershed. The bedrock of the Mugello basin consists
of tectono-sedimentary units piled up in an imbricate mainly NEverging
and NW-SE-trending thrust-sheet system affecting the
Ligurian, Tuscan, and Romagna units. The uppermost Ligurian
units are locally completely eroded, forming in places small
klippen. The Tuscan and Romagna units are represented by the
foredeep sequences progressively accreted to the chain
(BENVENUTI, 1997; BENVENUTI, 2003). Seven samples come
from the bedrock: one from the Tuscan units and six from the
Romagna units.

The apatite FT bedrock age for the Tuscan Units is 18.0±1.4
Ma. From a vertical profile spanning ca. 500 m in the Romagna
Units, apatite FT ages vary between 2.6±0.8 and 4.1±1.2 Ma. The
AFT ages for the sediments vary between 4.2±0.6 to 9.6±2.1 Ma.
The grain-age distributions of Mugello Basin sediment samples
are characterized by four components, the younger peak (P1)
varying between 2.4±1.5 and 3.4±1.2 Ma, the P2 peak varying
between 6.4±1.7 and 8.3±2.5 Ma, the P3 peak ranging between
17.5±4 and 24.6±15 Ma and the P4 peak varying between
37.9±18 and 49.4±20 Ma (RUIZ et alii, 2004). The average
lagtime of the P1 component of the Mugello Basin samples is ca.
1.5 Ma from which we can estimate a mean exhumation rate of
2.0-2.4 mm/yr. By comparison with the bedrock ages here
obtained and those ones from the literature, we can attribute the
P1 population to the Romagna units, the P2 and P3 population to
the Tuscan units and the P4 population to the Ligurian Units.
Their appearance and disappearance in the stratigraphic sequence
going up-section are related to the activity and/or reactivation of
back-thrusts when the active front of the Northern Apennine
chain was at 50 km to ENE. Thus, our data represent a
confirmation that compressive tectonics controlled most of the
Mugello basin evolution. Extensional tectonics superposed onto
compressional structures from the middle Pleistocene until
Present.
REFERENCES
BENVENUTI M. (1997) – Physical stratigraphy of the fluviolacustrine
Mugello Basin (Plio-Pleistocene, northern
Apennines, Italy). Giorn. Geol., 59 (1-2), 91-111.
BENVENUTI M. (2003) – Facies analysis and tectonic
significance of lacustrine fan-deltaic successions in the
Pliocene-Pleistocene Mugello Basin, Central Italy. Sediment.
Geol., 157, 197-234.
BENVENUTI M. BERTINI A., CONTI C. & DOMINICI S. (2007) –
Integrated analyses of litho- and biofacies in a Pliocene
cyclothemic, alluvial to shallow marine succession (Tuscany,
Italy) . Geobios, 40, 143-158.
DEL CONTE S. (2007) – Dinamica deposizionale e fattori di
controllo dei sistemi fluvio-deltizi e marino-costieri: il Bacino
pliocenico della Valdelsa (Toscana Centrale, Italia).
Unpublished PhD thesis, Earth Sciences Dept, Florence
University, 140. pp.
RUIZ G.M.H., SEWARD D. & WINKLER W. (2004) – Detrital
thermochronology – a new perspective on hinterland
tectonics, an example from the Andean Amazon Basin,
Ecuador. Basin Res., 16, 413-430.
429
SESSIONE 12

SESSIONE 12
Key words: Geochronology, Himalaya, tectonics.
Many models attempt to reconstruct the geomorphological
history of an orogen by dating detrital minerals and by basing on
interpretive models proposed in the pioneer days of
geochronology. We propose instead to address the actualistic
processes that operate at present in a geologically and
petrologically well constrained framework, so as to discriminate
realistic argumentations from geofantasy.
The detritic minerals analyzed in this work derive from
present-day river sands from Sikkim. The rivers drain the
Kangchendzönga massif, whose highest elevation is 8.6 km.
Fission track dating on apatites and zircons indicate an erosion
rate of 1 mm/a during the whole Pleistocene.
Dioctahedral micas have ages between 10 and 15 Ma, as a
function of the lithological units cropping out upslope of the sand
samples. This corresponds, in the interpretive schemes sometimes
applied to Oligo-Miocene sediments, to a “lag time” of 10-15
Ma. The lag time is the age difference between the sediment and
the detrital minerals it contains. An unusually high lag time > 10
Ma is usually interpreted as slow erosion due to low relief. This
conclusion is paradoxical for Sikkim.
The solution of the paradox must be sought in the meaning of
geochronological data and in the processes that induce isotopic
rejuvenation. Dioctahedral mica (actually, the phengitemuscovite-margarite-paragonite
series) is formed in a variety of
petrological conditions and therefore represents a variety of
geological situations. As an example, phengite can normally be
assigned, by means of thermobarometric calculations performed
on the entire mineral assemblage of a rock, to a high pressure
(HP) event. The Rb-Sr and K-Ar systems in phengite usually
record the age of the HP event.
Often disequilibrium microtextures are observed, such as
patches of phengite replaced by muscovite (which formed in a
subsequent greenschist facies retrogression, GSFR). Only a
petrological study can reveal the internal disequilibrium of the
retrogressed HP paragenesis due to substitution reactions. During
GSFR, radiogenic isotopes 87 Sr and 40 Ar are lost independently of
_________________________
Himalayan detrital geochronology: tectonic modelling or
petrological equilibrium?
IGOR MARIAVILLA (*), GIOVANNI VEZZOLI (*), EDUARDO GARZANTI (*) & SILVIA BARDINI (*)
(*) Dipartimento di Scienze Geologiche e Geotecnologie, Università di Milano
Bicocca, igor.villa@unimib.it
430
temperature, as an effect of heterochemical recrystallization of
phengite to muscovite.
It is self-evident that an isolated grain of detritic muscovite
cannot be put into the context of a thermobarometric calculation
(where’s the rest of the paragenesis?), and that it is therefore
impossible to assess if the age on a detrital white mica grain dates
an eclogite-facies HP event or its greenschist-facies retrogression
20 Ma later. A further complication is provided by the stability
fields of minerals in a diagenetic environment. Illite-like
phyllosilicates can form in marine sedimentary environments, and
a white mica grain that spent enough time exchanging cations on
the sea-floor records post-sedimentation diagenesis and not
orogenic exhumation.
In conclusion, whenever the geological reality contrasts with
tectonic modelling, the key to reconcile observations with
interpretations must be sought in the petrology of the analyzed
minerals.

SESSIONE 13
Geologia e esplorazione petrolifera
(Sessione in memoria di Giovanni Flores e Marco Pieri)
CONVENERS
Francesco Bertello (ENI)
Ernesto Abbate (Università di Firenze)
431
SESSIONE 13

SESSIONE 13
Key words: Deformation bands, extensional faults, grain size,
fault permeability, poorly lithified sediments.
We present structural, granulometric and permeability data
from extensional fault zones developed in high-porosity sandy
sediments of the Crotone basin, southern Italy. Displacement
values span from few cm to about 100 m.
The fault zones generally consist of well defined narrow fault
cores bounded by damage zones on both hanging wall and
footwall sides.
Fault core rocks developed by progressive comminution and
consist of foliated granular material and gouge lenses along
indurated and striated slip surfaces.
Fault damage zones typically consist of closely spaced single
to anastomosing cataclastic deformation bands with different
degree of complexity. Undeformed sediments have mean
permeability values in the 103 to 105 mD range.
Mean fault core rock permeability broadly ranges between
101 and 104 mD, although we recorded permeability values
lower than 10 mD in gouge lenses.
Fault damage zones have a mean permeability between 102
and 104 mD, i.e. lower than host sands.
We obtained empirical relationships between bulk
permeability, fault zone thickness, and fault displacement. In
particular, both fault cores and damage zones tend to widen with
increasing fault displacement, especially in the first ten meters.
Most bulk permeability reductions in both fault cores and damage
zones occur at sub-seismic scale, and decrease for displacement
greater than 25-30 m.
_________________________
Structural and petrophysical evolution of extensional faults in
high-porosity sands from the Crotone basin, south Italy
(*) Dipartimento di Scienze Geologiche, Università degli Studi Roma Tre,
Roma, balsamo@uniroma3.it
FABRIZIO BALSAMO (*) & FABRIZIO STORTI (*)
432

Key words: Chaotic rocks, debris flow, frontal tectonic erosion,
Northern Apennines, olistostrome, scaly clays, slope collapse
The purpose of this work is i) to explore the historical and
cultural motivations behind the birth of the olistostrome concept,
showing that this concept is strictly related to the interpretation of
the Italian argille scagliose made during the 1950s, and ii) to
explain why only during the 1980s, i.e., 25 years later,
olistostromes in the Emilia Apennines were thoroughly
distinguished from the Ligurian/Epiligurian units and other types
of chaotic rocks. This work also aims to show the essential role
played by this distinction for a more detailed reconstruction of
the tectonic evolution of the Northern Apennine orogenic belt.
FLORES introduced the term olistostrome in the geological
literature in 1955. This term was a success and it spread out
around the world, so that currently it is one of the most
worldwide used terms coined by an Italian geologist, together
with argille scagliose (BIANCONI, 1840). The Italian community
immediately started a particularly intense discussion around what
rock assemblages can be named olistostrome, but also around the
term itself.
The debate about the definition of this term initiated – and it
is still open – because olistostrome is not a descriptive term, but a
genetic term describing the result of a depositional process. In
spite of this, and from a historical point of view, the “invention”
of the term olistostrome represents an essential contribution to the
progress of the geological knowledge. For the first time, in fact, a
new term was introduced conveying the idea that pure
gravitational sedimentary processes can also generate chaotic
rocks. It is not accidental that the word olistostrome was
introduced in Italy during the 1950s, when the argille scagliose –
about which Italian geologists struggled for a century – finally
brought to a general consensus on their allochthony. Allochthony
meant emplacement through tectonic processes driven by
gravitation (i.e., orogenic landslides: MERLA, 1951).
The great value of FLORES’s term (1955, 1956, 1959) is the
_________________________
Olistostromes and their importance for interpreting
the tectonic evolution of orogenic belts:
the example of the Northern Apennines, Italy
* Università di Modena e Reggio Emilia, giuseppe.bettelli@unimore.it
GIUSEPPE BETTELLI (*)
433
suggestion that part of the Italian argille scagliose are the result
of pure sedimentary-gravitational processes. This was in contrast
with the several previous interpretations implying, for example
mud volcanoes, diapirs, or tectonic-gravitational processes as in
the hypothesis of MERLA’s (1951). Nevertheless, the influence of
the geological thought of those years and some flaws in the
original definition (FLORES, 1955, 1956, 1959) of olistostrome
caused a serious limitation to the identification of the
corresponding rock mass in the field. At that time, the discussion
was driven by the lack of a clear conceptual distinction between
tectonic-gravitational processes and sedimentary-gravitational
processes (i.e., between gravity tectonics, sedimentary mass
wasting processes and turbidite sedimentation).
Following the original definition, the possible presence of
large inclusions (several km 3 ) of previously “bedded” rocks, i.e,
olistolithes (FLORES, 1955, 1956), caused problems in
distinguishing olistostromes from other types of chaotic bodies,
which at that time were thought to be generated by tectonicgravitational
processes (i.e., the argille scagliose).
The still most controversial examples of olistostromes in the
Northern Apennines contain quite large bodies – several km 2
wide – of “previously bedded” rocks. Within that discussion, we
can find the basis of the Italian controversy about the distinction
between the argille scagliose (i.e., the Ligurian/Subligurian units)
and true olistostromes. The result is that during the time interval
between 1955 and 1980, only few olistostromes were recognized
and separated form the argille scagliose or Ligurian/Subligurian
units. In large areas of the Northern Apennines and in particular
in the type area of the argille scagliose (i.e., the Emilia
Apennines: MERLA, 1951), the outcropping chaotic rocks
continued to be mapped all together although described with new
terms as alloctono indifferenziato, Chaotic complex, etc..
Starting from the ‘80ies, in the Emilia Apennines the
distinction of olistostromes from the argille scagliose or Chaotic
Complex (i.e., the broken and dismembered formations of the
Ligurian and Subligurian units) and other types of chaotic rocks
(tectonic mélanges and mélanges of unknown origin) was finally
achieved. This was done simply in restraining the olistostrome
concept in the field to include only the debris flow deposits. The
result of this experimental approach was the discovery that
reliable olistostromes (debris flow deposits), may contain sparse
blocks of “previously bedded rocks”, i.e., olistolithes, but that
SESSIONE 13

SESSIONE 13
their size is restricted to dimensions ranging from some meters to
some decameters. These findings seems to point out that the
original definition of olistostrome, comprising all the different
types of mass wasting deposits (from debris flow deposits to huge
slide masses of “previously bedded rocks”) was too extensive to
be of practical use in the field.
This definition, though, may be extremely useful in the field if
restricted to embrace only the debris flow deposits, following the
original important limitation of FLORES (1955) that the
olistostrome material should be in a “semifluid state” during its
deposition. The complex and intimate association of large kmsize
blocks and debris flow deposits, therefore should be
considered highly questionable if considered as representing an
original, unique mass wasting deposit unaffected by later large
tectonic deformation and mixing (tectonic mélange).
In the Emilia Apennines, the great value of the careful
distinction between true olistostromes and other types of chaotic
rocks (broken and dismembered formations, tectonic mélanges,
mélanges of unknown origin, etc.) brought to a better
understanding of the tectonic evolution of the Northern
Apennines, as widely shown by the recent geological literature.
Good examples of this improvement are two quite different and at
first sight unrelated cases: the Brecce argillose della Val Tiepido-
Canossa Epiligurian olistostrome and the Coscogno tectonic
mélange.
The first unit is one of the earliest olistostromes recognized
in the Emilia Apennines (PAPANI, 1963, 1971). At the beginning
it was mapped only in limited areas, but at present this pile of
debris flow deposits has been recognized as present along the
entire external belt of Emilia Apennines, even though the causes
of its deposition remained largely inadequate. The Coscogno
mélange is a tectonic mixture of large blocks of Ligurian,
Subligurian and Epiligurian units.
It is now interpreted as a tectonic mélange generated by
underthrusting processes with material deriving from the frontal
tectonic erosion of the Ligurian wedge during the Aquitanian. In
this tectonic scenario, the Brecce argillose della Val Tiepido-
Canossa olistostrome represents clearly the sedimentary signature
of this process of frontal erosion which caused the tectonic
destabilization of the Ligurian wedge, the collapse of the
Epiligurian slope sediments and the subsequent emplacement of
the debris flow deposits. The example shows that regional
widespread mass wasting deposits are important features for the
geodynamic reconstruction of ancient orogenic belts.
REFERENCES
BIANCONI P. (1840) – Storia naturale dei terreni ardenti, dei
vulcani fangosi, delle sorgenti infiammabili, dei pozzi
idropirici e di altri fenomeni geologici oprati dal gas
idrogene e dell’origine di esso gas. Marsigli, Bologna, 164
pp..
434
FLORES G. (1955) - Discussion. - In: E. Beneo: Les résultats des
études pour la recherche pétrolifère en Sicile. Proceedings,
Fourth World Petroleum Congress, Rome, Section I, A/2,
121-122.
FLORES G. (1956) – Lettera al Presidente della Società
Geologica Italiana. Boll. Soc. Geol. It., 75 (3), 220-222.
FLORES G. (1959) – Evidence of slump phenomena
(olistostromes) in areas of hydrocarbons exploration in
Sicily. Proceedings, Fifth World Petroleum Congress - New
York, 259-275.
MERLA G. (1951) – Geologia dell’Appennino Settentrionale.
Boll. Soc. Geol. It., 70 (1), 95-382.
PAPANI G. (1963) – Su un olistostroma di
intercalato nella serie oligomiocenica del Subappennino
reggiano. Boll. Soc. Geol. It, 82 (3), 195-202.
PAPANI G. (1971) – Geologia della struttura di Viano (Reggio
Emilia). Mem. Soc. Geol. It., 10, 121-165.

Key words: Algeria, Akabli basin, basin modeling, Reggane
basin, reservoir, source rock, tectonic event.
EXPLORATION OF ALGERIA
The significant number of oil and gas discoveries made in
North Africa and in particular in Algeria, in the last decade have
made this region among the most important and still promising
hydrocarbon provinces in the Mediterranean area.
North Africa formed during the Pan-African orogenesis (700-
530 Ma) due to the oblique continental collision which involved
the West African craton and the arc-trench systems. This collision
facilitated the formation of a number of regional fault systems:
the Pan-African strike-slip, the Trans-African features, the
Central Africa features and the Najd fault system. During the
Intracambrian (640-520 Ma) these existing structural features
were reactivated through extensional movements, thus triggering
the formation of a shear zone along the Trans-African lineaments
as well as the Najd fault system (Fig.1) .
These tectonic events generated a number of intraplate pullapart
basins and half grabens permitting the syntectonic
deposition which today outcrop in the South-Western Algeria.
The equivalent Silurian and Devonian black shale sequences have
also been identified in the Algerian Paleozoic basins. The
Hercynian orogenesis reactivated pre-existing fault systems and
brought new about NNW/SSE-trending thrusts and folds: the
magnitude of these structures progressively decreases towards the
eastern sector.
The tectonic events and diverse depositional environments
which shaped North African geology have favoured the
petroleum potential of the region, though particularly Algeria’s.
The considerably thick, fluvial Devonian successions deposited in
these asymmetric basins form good quality reservoirs. The most
significant outcrops of these fluvial sequences are located along
the central-southern Algerian sector where they overlie the
Hoggart Massif crystalline basement.
_____________________
Tectonic evolution and petroleum system of the
Reggane and Akabli Basins (Algeria)
GIORGIO BOLIS (*), ROBERTO CALABRÒ (*), LUCA FELTRE (*) & MANLIO MAZZARELLI (*)
(*) Edison S.p.A., Milan, roberto.calabro@edison.it
435
The interpretation of new 2D and 3D seismic data of the
Reggane and Akabli basins has permitted to determine critical
aspects of the complex structural relations existing between these
basins. The interpretation proposed here, conjectures the
presence of a partial thrusting or inverse faulting system relating
the Reggane and Akabli basins. In the Reggane basin these
tectonic movements brought the Khalouche structure into a
deeper structural position, while upthrusting eastwards the
Reggane structure. The relationship between the Reggane and
the nearby Akabli basin could also be elucidated as the result of
transpressive and transtensive movements through high-angle
faulting mechanisms. These events could be dated to the
Ordovician period, and thus indicate the onset of the compressive
regime which culminate of with the Hercynian orogeny. The
seismic reconstruction also permitted to confirm that the
Hercynian unconformity remained unaffected by subsequent
compressive events, indicating the pre-tectonic deposition of
these shales sequences.
The ‘basin modelling’ simulations performed in this study on
the Silurian and Devonian source rocks are in good agreement
with previously published results. The data gathered in this study
indicates gas generating mechanisms for the Reggane source
rocks, resulting from the rapid subsidence of the western sectors
of the Algerian basins.
These simulations also confirmed the presence of oil
producing source rocks in the northern sectors of the Ghadames
basin, as would be expected from the limited depth of burial
reached by the rocks. It could also be determined that the Silurian
and Devonian shales formations began producing during the early
Hercynian orogenetic stages in the Lower Carboniferous (350
Ma) and continued hydrocarbon generation throughout the
Cenozoic.
SESSIONE 13

SESSIONE 13
Lower Pliocene sedimentary evolution of Bradanic Foredeep in the
Val D’Agri subsurface area (Southern Apennines, Italy)
Key words: Bradanic foredeep, lower Pliocene, Southern
Apennines, tectono-sedimentary evolution, turbidite system.
The Southern Apennines formed during Tertiary collision of
the African and Euro-Asian plates. Large sectors of the Adria
foreland were progressively involved in the Apennine orogenesis
due to eastward migration of the thrust-and-fold belt. During late
Miocene to Plio-Pleistocene, the western margin of the
Mesozoic-Tertiary Apulian Platform (AP) underwent gradual
deformation due to Apennine orogenesis. As a consequence, large
sectors of the carbonate platform were affected by intense
Apennine subsidence with the creation of Plio-Pleistocene
foredeep depocenters (Bradanic Foredeep - BF), recording deepwater
siliciclastic sedimentation. The AP and the overlying Plio-
Pleistocene foredeep turbidites were then overthrusted
(MOSTARDINI &MERLINI, 1986) by the Allochthonous Complex
(AC), during its eastward displacement. The Lower Pliocene
siliciclastic succession of the Val d’Agri (VA) area, represents
the westernmost and oldest depocenter of the Plio-Pleistocene
Lucano Basin (SE sector of the BF). The present location of the
BF on top of the AP is the result of two subsequent phases of
eastward migration of the foredeep triggered, in the Pliocene, by
two dramatic tectonic events: the “Intra-Zanclean Phase” and the
“Gelasian Phase”.
The VA Oil Field, located in the south-western part of
Basilicata region, represents the major European onshore oil
discovery. The Mesozoic-Tertiary carbonate reservoir of the AP
is unconformably overlain by a thick succession of lower
Pliocene sandstone, shale and marl (PATACCA &SCANDONE,
2006). The lower Pliocene foredeep succession is directly
overthrusted by the Miocene Irpine Units of the AC (Fig. 1).
Large volumes of subsurface data from wells and seismic
acquisition (such as: explorative and development wells, ditch
cuttings, cores, conventional and image logs, 2D and 3D seismic
surveys), provided the opportunity to construct a detailed
sedimentological and geological model for the lower Pliocene
VA siliciclastic succession.
_________________________
(*) Eni S.p.A. - E.&P. Division, paolo.carubelli@eni.com
PAOLO CARUBELLI (*), MANLIO GHIELMI (*), PAOLA BOCCA (*), ALFREDO PUGLIESE (*),
LUCA ALFONSO RENNA (*) & VALERIA SCOLA (*)
436
In the study area, the entire lower Pliocene succession reaches
the maximum thickness of about 600 m (minimum thickness
about 70 m) with an average sedimentation rate of about 0,4m/ky.
It represents the turbiditic infill of a highly-subsiding foredeep,
set over a large portion of the AP. The VA foredeep is a
relatively narrow (2-8 km) and elongated (more than 25 km)
Fig. 1 – Lower Pliocene tectono-sedimentary evolution of the VA area.
basin, roughly parallel to the Apennines main structural trends
(NNW-SSE). During the sedimentation, the inner foredeep
margin is represented by the AC front; while the external one, by
a system of high angle normal faults cutting through the AP (Fig.
1). In the NW sector of the study area, the lower Pliocene
consists of a monotonous sequence of medium to thick bedded,
very coarse to medium graded sandstone (and pebbly mudstone)
with erosive base and abundant shale clasts. In the central and SE
sectors a thin section of marls (the so called Basal Marls, Fig. 2)
is overlain by medium to fine sandstones and shales with an

Fig. 2 – Simplified transect of depositional elements architecture of the Bradanic Foredeep.
overall coarsening-upward trend (Fig. 2). All these deposits have
been included in a new informal unit – named Volturino Fm. – as
part of the Eni Lithostratigraphy. From a petrographic point of
view the succession of the Volturino Fm. reveals a relatively high
content in carbonate lithic fragments that most likely, have been
strongly involved in processes of alteration and dissolution during
the early diagenetic events. In fact, the mineralogical composition
and the rapid tectonic burial are considered responsible for the
early and strong diagenesis observed in the lower Pliocene
succession. On the basis of the available well-logs and bottom
cores, three main turbidite facies associations (MUTTI et alii,
1999) have been recognized in the foredeep succession: proximal
sandstone lobes, distal sandstone lobes and fine-grained basin
plain deposits. The turbidite deposits belong to highly-efficient
longitudinal turbidite systems as revealed by an evident downcurrent
facies evolution from the NW to the SE sector. Two
smaller poorly-efficient sand-prone turbidite systems, directly fed
by the inner margin of the basin (SW), have been also recognized
and described in the southern part of the foredeep (Fig. 2).
According to the biostratigraphic data, the entire succession is
assigned to lower Pliocene (MPL1-MPL2-MPL3 biozone of
CITA, 1975). On the basis of these data the succession is
attributed to the PL1 large-scale sequence and to the LM
Allogroup (NASC, 1983) of the Eni Plio-Pleistocene Sequence
Stratigraphy. A tectonic sequence boundary, related to a phase of
NE migration of the AC and its partial overthrusting on the inner
margin of the foredeep, subdivides the PL1 Sequence into two
medium-scale sequences. The two sequences, named PL1a and
PL1b (in ascending stratigraphic order), span in time 0.5-0.9My.
The PL1a-PL1b Sequence Boundary (SB), which corresponds to
a narrowing of the foredeep depocenter (Fig. 1), has strongly
influenced the depositional systems distribution. It marks a sharp
forestepping of the turbidite system of the PL1b Sequence as
documented by the direct superimposition of PL1b sandstone
lobes on the PL1a basin plain deposits (Fig. 2).
A phase of severe deformation during the upper part of Lower
437
Pliocene (“Intra-Zanclean Phase” – PL2 SB) is responsible for
the rapid overthrusting of the Miocene Irpine Units of the AC on
the VA foredeep (Fig. 1) and of the interruption of the PL1
Sequence turbiditic sedimentation. The creation of a new and
more external foredeep depocenter takes place further NE.
Acknowledgements
The authors gratefully acknowledge Shell Italia S.p.A for the
permission to present this paper. The authors would also like to
thank M. Arduini, C. Cavalli, C. Magistroni, A. Ortenzi and all
other Eni colleagues that contributed with data, ideas and useful
discussions to the study.
REFERENCES
CITA M.B. (1975) - Studi sul Pliocene e sugli strati di passaggio
dal Miocene al Pliocene. VII. Planktonic foraminiferal
biozonation of the Mediterranean Pliocene deep sea record.
A revision. Riv. It. Paleont. Strat., 81(4), 527-544.
MOSTARDINI F. & MERLINI S. (1986) - Appennino centromeridionale.
Sezioni geologiche e proposta di modello
strutturale. Mem. Soc. Geol. It., 35, 177-202.
MUTTI E., TINTERI R., REMACHA E., MAVILLA N., ANGELLA S. &
FAVA L. (1999) - An introduction to the analysis of ancient
turbidite basins from an outcrop perspective. AAPG
Continuing Education Course Note Series 39.
NORTH AMERICAN COMMISSION ON STRATIGRAPHIC NOMENCLA-
TURE (1983) - North American stratigraphic code. AAPG
Bull., 67, 841-875.
PATACCA E. & SCANDONE P. (2007) - Geology of the Southern
Apennines. In: A.Mazzotti, , E.Patacca, and P.Scandone
(Eds.) - Boll. Soc. Geol. It., Spec. Issue No.7, 75-119.
SESSIONE 13

SESSIONE 13
Finding sand on muddy slopes: how can the study of the modern
seafloor improve the predictive power of 3D seismic analysis
Key words: Sedimentary architectural elements, seismic
geomorphology, slope clinoforms, trajectory analysis.
ABSTRACT
A research project (enigma) had been carried out by ISMAR
CNR – Bologna and eni exploration & production division in
order to develop proper sedimentological conceptual models for
seismic interpretation to improve the predictive power of seismic
analysis.
In particular, the project was focused on the areal and vertical
evolution of slope clinoforms, their sedimentary architectural
element distribution and their seismic facies.
For the analysis, a 2/3D eni proprietary seismic dataset of the
Adriatic Sea (Pescara Basin) was examined. The investigated
seismic sequence was limited approximately to the 1 st second
TWT where a Pleistocenic slope clinoforms are well developed.
The internal stacking patterns analysis of slope clinoforms
was carried out through three different methodologies:
rollover trajectory analysis
2D seismic facies analysis
3D seismic geomorphology
The combination of these techniques allows the sedimentary
environments reconstruction of a given depositional system and
in particular the understanding of how geomorphic elements
control the sediments dispersal and partitioning across the
clinoforms during margin development.
These informations can be used to improve the know how
about changes in paleo-environmental conditions, and
consequently to infer lithological occurrence and distributions
through time.In addition, morphometric observations (i.e.
changes in slope clinoforms characteristic recognized with 3D
seismic geomorphology techniques) allow the definition of key
elements and signature of sedimentary processes at basin scale
_________________________
GIACOMO DALLA VALLE (*), FABIANO GAMBERI (*), FABIO TRINCARDI (*), PATRIZIA ROCCHINI (°),
ALESSIA ERRERA (°) & LUCA BAGLIONI (°)
(*) ISMAR - Sezione di Geologia Marina, Bologna,
giacomo.dalla.valle@bo.ismar.cnr.it
(°) ENI- Exploration & Production Division, San Donato Milanese.
438
(source to sink analysis).
Avoiding the spatial limitation proper of 2D seismic data, this
approach may constitute an alternative interpretative tool
compared to the conventional sequence stratigraphy analysis of
depositional sequences and their constituents.
The prevailing muddy environment of the Pescara basin
characterized by many possible reservoir elements grouped in to
three different slope clinoform types. The position of these
elements within the clinoform stratigraphy appears predictable
being associated with specific characteristics of roll-over
trajectory, reflecting the interplay between accommodation space
and sediment supply. During low stand shelf exposure, slope
channels and their frontal splay complexes are fed by incised
valleys. Sediment oversupply can cause sediment to escape the
shelf also during its flooding, forming shelf-edge deltas, slope
chutes and related frontal splays.
These results have a great potential in developing
qualitative models for the prediction of deep-water coarser
lithology (possible reservoirs) distribution on the different slope
clinoform environments and their connection degree along the
clinoform segment.

The Po Plain laboratory thirty years after Pieri & Groppi (1981)
Key words: Po Plain, Southern Alps, foreland flexuring,
hydrocarbon exploration
PIERI & GROPPI (1981)
The hydrocarbon exploration in Po Plain has begun with the
research of biogenic gas in the Plio-Pleistocene terrigenous
succession and culminated in 1944 with the discovery of Caviaga
gas field, the greatest field of western Europe of that time
(BERTELLO et alii, 2008).
In the early seventies of the past century, the exploration of
the Mesozoic carbonate succession began thanks to the
introduction of the multiple coverage in the reflection seismic:
this first campaign led to the discovery of the Malossa oil field in
a Cenozoic compressional structure (ERRICO et alii, 1980;
MATTAVELLI & MARGARUCCI, 1992). The seismic surveys
acquired and the numerous Mesozoic targeted wells drilled
during that decade provided an important database for the
understanding of the geology of the Po Plain’s substratum.
These data, originally elaborated for the hydrocarbon
exploration purposes, have been subsequently summarized in the
“Subsurface geological structure to you of the Po Plain”, a paper
based on thirteen regional geologic sections and published by
Marco Pieri and Gabriele Groppi in 1981.
The interpretation of these sections (PIERI &GROPPI, 1981;
CASSANO et alii, 1992) allowed the reconstruction of the buried
margin of the Southalpine thust-and-fold belt (CASTELLARIN,
1984; CASTELLARIN &VAI, 1986; LAUBSCHER, 1985): the plain,
as an object of research, constituted just an appendix to apply on
which knowledge and models elaborated in the surrounding
chains.
THIRTY YEARS LATER
After the publication of the paper of Pieri & Groppi, the
hydrocarbon research continued with the exploration of the
Mesozoic extensional structures, which were partially
restructured during the alpine compression (FANTONI et al,. 2008)
_________________________
(*) Eni E&P, roberto.fantoni@eni.it
ROBERTO FANTONI (*)
439
and the discovery, in 1984, of Villafortuna-Trecate oil field
(FANTONI et alii, 2002a)
The complexity of these targets made it necessary to acquire
new geologic and seismic data, in order to reconstruct with
extreme detail the ages of deformation of the structures and the
ages of the foredeep infilling. New sets of geological section are
now available on the whole foreland (FANTONI &FRANCIOSI,
2008).
At the same time models have been elaborated to illustrate the
physical relationships between the load of the chain and the
flexuring of its foreland.
These data and models introduced a reversal of the research:
the Po laboratory concurs to observe the Alps from another point
of view.
The different age of flexuring of the western and eastern
sectors of the Po-Veneto Plain (FANTONI at al., 2002b, 2004)
suggests a subdivision of the Southern Alps, separated from the
undeformed block of the Lessini Mountains, in two chains with
two different deformation histories.
REFERENCES
BERTELLO F. FANTONI R. & FRANCIOSI R. (2008) - Exploration
Country Focus: Italy. AAPG–ER Newsletter, June 2008, 5-9.
CASSANO E., ANELLI L., FICHERA R. & CAPPELLI V. (1986) –
Pianura Padana. Interpretazione integrata di dati geofisici e
geologici. 73°Congr. Soc. Geol. It., 29 sett-4 ott. 1986, Roma,
27.
CASTELLARIN A. (1984) - Schema delle deformazioni tettoniche
sudalpine. Boll. Oceanologia Teor. Appl., 2, 105-114.
CASTELLARIN A. & VAI G.B. (1986) - Southalpine versus Po
Plain Apenninic Arcs. In: Origin of Arcs. Development in
Geotectonics, 21, 253-280.
ERRICO G., GROPPI G., SAVELLI S. & VAGHI G.C. (1980) –
Malossa Filed: A Deep Discovery in the po Valle, Italy. In
M.T.Halbouty, (Ed.), Giant Oil and Gas Fileds of the Decade
1968-1978, AAPG, 525-538.
FANTONI R., BELLO M., RONCHI P. & SCOTTI P. (2002a) - Po
Valley oil play: from the Villafortuna-Trecate field to South-
SESSIONE 13

SESSIONE 13
Alpine and Northern Apennine exploration. EAGE
Conference Florence 2002, Extended Abstracts Book, 4 pp.
FANTONI R., CATELLANI D., MERLINI S., ROGLEDI S. &
VENTURINI S. (2002b) - La registrazione degli eventi
deformativi cenozoici nell’avampaese veneto-friulano. Mem.
Soc. Geol. It., 57, 301-313.
FANTONI R., BERSEZIO R. & FORCELLA F. (2004) - Alpine
structure and deformation chronology at the Southern Alps –
Po Plain border in Lombard. Boll. Soc. Geol. It., 123, 463-
476.
FANTONI R., BERTELLO F. & FRANCIOSI R. (2008) - Reservoirs
and source rocks in Mesozoic carbonate units of Italy. Rend.
Soc. Geol. It., 3/1, Riassunti dell’84° Congresso Nazionale
Sassari 15-17 settembre 2008 (Italy), 365-366.
Appennine
foredeep
Fig. 1 – Geological sections across the Po Plain
western southalpine
foredeep
Appennine
foredeep
Appennine
foredeep
western Southern
440
FANTONI R. & FRANCIOSI R. (2008) - 8 geological sections
crossing Po Plain and Adriatic foreland. Rend. Soc. Geol. It,
3/1, Riassunti dell’84° Congresso Nazionale Sassari 15-17
settembre 2008 (Italy),. 367-368.
LAUBSCHER.P. (1985) - Large scale, thin-skinned thrusting in
theSouthern Alps: kinematic models. Geol. Soc. Am. Bull.,
96, 710-718.
MATTAVELLI L. & MARGARUCCI V. (1992) - Malossa field-Italy.
In: Treatise of Petroleum Geology, Atlas of Oil and Gas
Fields, Structural Traps, 7, 119-133.
PIERI M. & GROPPI G. (1981) - Subsurface geological structure of
the Po Plain, Italy. Prog. Finalizzato Geodinamica C.N.R.,
Publ. 414.
Southern Alps and Appennine outcrops
geological sections
CL Cremosina Line
IL Insubric Line
GL Giudicarie fault system
SVL Schio-Vicenza Line
VSL Valsugana Line
VTL Val Trompia Line
CL
Northern Appennines
IL
Alps
western Southern Alps
VTL
Po Plain
Appennines foreland (Lessini
G
L
eastern southalpine
foredeep
Lessini
eastern Southern Alps
SVL
VSL
western Southern
IL
Adriatic sea

Key words: Marco Pieri, esplorazione petrolifera, Italia
Marco Pieri, nato a Bolzano il 20 novembre 1926, si è spento
a Firenze il 25 maggio 2009.
Laureatosi brillantemente in Scienze Naturali presso
l'Università di Firenze il 20 Novembre 1948, per un breve
periodo effettuò un internato nell'Istituto di Geologia di quella
Università, diretto dal prof. Giovanni Merla, sotto la cui guida
approfondì la sua preparazione geologica.
Nel gennaio 1951 Pieri iniziò la sua attività come geologo
dell’Agip. Nella sede di Lodi fu intensamente coinvolto in attività
varie, dall'assistenza geologica nei cantieri di perforazione, alla
stesura di programmi e rapporti di lavoro (specialmente per la
Pianura Padana), a rilievi geologici in alcuni settori
dell'Appennino. Inseritosi positivamente nell'ambiente
dell’Azienda, ancora in corso di strutturazione, si fece subito
apprezzare per la sua disponibilità a compiti importanti e per le
sue capacità di operare organicamente e correttamente.
La sua figura asciutta e il suo aspetto riservato rivelarono
forte personalità e determinazione, grande apertura mentale e
notevole preparazione culturale, e capacità di creare un aperto
cameratismo con i colleghi.
Da allora Pieri è stato per molti anni uno dei testimoni e, in
parte, anche uno dei protagonisti, dello sviluppo della ricerca e
dell’evoluzione dell'AGIP dalle condizioni di gestione quasi
artigianale del periodo prebellico, a quelle di una Società
internazionale con tecnologie e idee moderne.
Nel 1953 fu promulgata la nuova Legge mineraria che istituì
l'ENI (Ente Nazionale Idrocarburi); seguì una riorganizzazione
dell’Azienda con un rilancio dell’attività esplorativa.
Nel 1954 Pieri eseguì rilievi geologici in Sicilia (Monti Iblei e
Sicani); nel definire le formazioni stratigrafiche delle successioni
sedimentarie esaminate, applicò criteri formazionali di
avanguardia (per quel tempo) che costituiranno un modello
innovativo da adottare anche in altri settori di indagine.
Nel 1955, rientrato nella sede di Lodi, fu incaricato di
organizzare la nuova attività di campagna nell’Appennino
settentrionale. Con un lavoro notevole curò la composizione di
_________________________
(*) doc.91@hotmail.it
Ricordo di Marco Pieri
RENATO GHELARDONI (*)
441
squadre geologiche di rilevamento, in modo che risultassero più o
meno standardizzate, come organico e, soprattutto, come
metodologie di operazioni, supportato dall'esperienza fatta in
Sicilia che, oltre tutto, gli aveva procurato un certo prestigio
personale.
Nel frattempo, collaborò alla preparazione dell'importante
"Convegno sui giacimenti gassiferi dell'Europa occidentale" che
si tenne nel 1957 a Milano (su iniziativa di Enrico Mattei); inoltre
organizzò l’escursione geologica del Convegno sull’Appennino
parmense.
Nel 1957 fu promosso dirigente (tra i più giovani) - "in
relazione agli incarichi affidatigli e alle capacità dimostrate" - e
destinato a gestire l'attività di esplorazione, inizialmente
nell'Italia centro settentrionale, in seguito nel resto del territorio
italiano.
I primi rilievi geologici, metodicamente programmati ed
eseguiti negli anni 1955-59, su una vasta area dell’Appennino
settentrionale, comprendente anche "Permessi di ricerca"
petrolifera, condussero alla ricostruzione della stratigrafia e della
tettonica all'interno della coltre alloctona delle fatidiche "Argille
Scagliose".
Lo schema di "Formazioni litostratigrafiche", definite in
accordo con i criteri raccomandati dalla American Commission
on Stratigraphic Nomenclature, AAPG 1956 (già applicati in
Sicilia) risultò correlabile con le serie "autoctone"
precedentemente esaminate sul crinale appenninico, nelle quali
erano stati riconosciuti rapporti di continuità stratigrafica dal
"Macigno"' alla "Marnoso - arenacea".
I rilievi, rappresentati in una moderna carta geologica
(1:10.000) comprendente il settore appenninico tra le Valli del
Dolo e dell' Idice, negli anni ’60 furono integrati e ulteriormente
dettagliati nell'ambito della nuova edizione della Carta Geologica
d'Italia, su incarico affidato all'AGIP dal Servizio Geologico
Italiano. Sotto la direzione di Pieri furono rilevati i Fogli 84
(Pontremoli) e 85 (Castelnovo ne' Monti) e, nello stesso periodo
anche i Fogli 118 (Ancona) e 212 (Montalbano Jonico) e
compilate le relative Note illustrative.
Le importanti ricostruzioni paleogeografico-strutturali
dell’Appennino effettuate da Pieri, hanno dato risalto alla
tettonica di accorciamento delle masse calcaree mesozoiche
sovrascorse verso Est, con movimenti tangenziali molto
accentuati (Appennino meridionale), e hanno evidenziato anche il
livello di distacco principale identificato nella spessa serie
SESSIONE 13

SESSIONE 13
evaporitica triassica presente alla base delle successioni
carbonatiche mesozoiche, istituita formalmente, nel 1964 con
Bruno Martinis, come "Formazione delle anidriti di Burano".
Le ricostruzioni sono state inquadrate sia nel panorama
evolutivo della Geosinclinale mediterranea, sia nel complesso
sistema paleogeografico e tettonico "Appennino - Dinarico".
Pieri, che fin dal 1951 aveva approfondito in più riprese le
conoscenze sul sottosuolo della Pianura Padana, nel 1981 volle
sintetizzare, con Gabriele Groppi, tali conoscenze con la
prestigiosa interpretazione geologica della "Struttura profonda
della Pianura Padana".
In base ai risultati del moderno rilievo sismico "digitale",
eseguito dall'AGIP nella Pianura Padana tra il 1968 e il 1982, e
con l'ausilio dei sondaggi, furono identificati e rappresentati con
chiarezza i grandi lineamenti strutturali della tettonica pliocenica
e postpliocenica, consistenti nei grandi archi di pieghe del fronte
sepolto dell’Appennino settentrionale, analoghi agli archi di
pieghe che più a sud caratterizzano il fronte dell'Appennino
centrale; inoltre fu messa in evidenza la profonda monoclinale
pedealpina che rappresenta l'avanfossa sia delle pieghe
appenniniche sia di quelle sudalpine.
Le ricostruzioni geologiche di questa particolare area sono
state ripetutamente utilizzate da ricercatori italiani e stranieri,
giacché il sottosuolo padano, grazie ai risultati del rilievo sismico
dell'AGIP, è divenuto un tassello con caratteristiche peculiari
dell'edificio strutturale compreso tra 1’Appennino e l'avanfossa.
Varie volte Pieri ha puntualizzato, anche in collaborazione
con altri Autori, lo stato della ricerca e delle prospettive
petrolifere del territorio italiano; le diverse situazioni italiane
produttive di idrocarburi sono state messe in relazione con i vari
bacini sedimentari o province geologiche coinvolte
nell'evoluzione tettonico - sedimentaria dell'area mediterranea, e
con i tipi di strutture che ospitano i giacimenti.
In particolare (con Luigi Mattavelli, nel 1986) sono state
sviluppate interessanti trattazioni dei meccanismi di genesi,
migrazione e accumulo dei vari tipi di idrocarburi contenuti nei
principali giacimenti italiani, distinguendo giacimenti a gas
biogenico e termogenico, generato e depositato nei clastici
dell'avanfossa pliocenico - quaternaria, e giacimenti
prevalentemente a olio termogenico generato da rocce triassiche e
depositato in rocce carbonatiche mesozoiche.
Le pubblicazioni di Pieri, costituenti contributi di notevole
originalità e di elevata valenza scientifica, hanno indubbiamente
concorso a valorizzare l'impegno e il prestigio dell'AGIP nel
sostenere il progresso della ricerca scientifica.
Tuttavia quanto è stato pubblicato non rivela a sufficienza
l’importanza della partecipazione diretta e indiretta, e,
soprattutto, l'apporto ideologico che si devono riconoscere a Pieri
per la mole di studi e ricerche sviluppate all'interno dell'AGIP e
che, per vari motivi e vincoli, non sono state divulgate.
Nel 1970 conseguì la “Libera docenza” universitaria.
Fin dal 1957 aveva tenuto corsi e seminari di Geologia
442
regionale e di Geologia del Petrolio, presso la scuola di Studi
Superiori degli Idrocarburi "E. Mattei" (1957-61), e in seguito
presso le Università di Modena (1963-68), di Milano (1973-76),
di Pisa (1981-1993) e di Firenze (1984-1993).
Nel 1988 esordì con il volume “Il Petrolio – origine, ricerca,
produzione, dati statistici e aspetti economici”, un’opera
completa e un ottimo testo destinato agli studenti di scienze
geologiche; nel 1981, insieme all’amico Giovanni Flores, aveva
pubblicato il volume “L’Italia geologica – Storia degli ultimi 230
milioni di anni”, nel quale con rigore scientifico fu presentato un
quadro unitario dell’evoluzione geologica del nostro paese, per
lettori non specializzati ma interessati alle Scienze della Terra.
Negli ultimi anni Pieri veniva spesso incaricato dalla
Direzione dell'Agip di tenere importanti contatti con Società
petrolifere, istituzioni pubbliche e governative italiane e straniere;
inoltre partecipò a numerose missioni, anche lunghe e
impegnative (come quella del 1980 in Cina), per effettuare
valutazioni di aree e progetti petroliferi nei più disparati e remoti
paesi.
Pieri non disdegnava questo genere di attività, che svolgeva
con impegno, con autorevolezza e con una certa autonomia
decisionale, anche perché appagava la sua tendenza a estendere la
conoscenza e l’esperienza.
Nel 1983, tenuto conto dei cambiamenti avvenuti
nell’ambiente, che ormai non era più quello in cui aveva vissuto
per molti anni, e ritenendo di avere raggiunto risultati personali
più che soddisfacenti, Pieri decise di lasciare anticipatamente
l'AGIP per ritirarsi nella sua Firenze.
Ma l'attività di Pieri continuò ancora molto intensamente,
dalla ricerca scientifica, talora anche in collaborazione con i
colleghi dell’AGIP, all’insegnamento, alla partecipazione a
congressi geologici e del petrolio, e a escursioni geologiche, in
Italia e all’estero.
Le prestazioni come consulente internazionale di
Esplorazione petrolifera per conto di numerose e importanti
Società lo impegnarono molto e gli procurarono lusinghieri
successi personali.
La sua preparazione professionale e il rigore scientifico
applicato negli studi e ricerche gli hanno meritato una grande
stima, sia nell'ambiente aziendale, sia presso la comunità
geologica, che ha voluto ricordare il suo prezioso contributo al
progresso delle conoscenze della Geologia Italiana. Infatti, nel
2005 Marco Pieri è stato inserito tra i "Soci Onorari" della
Società Geologica Italiana come segno di riconoscimento dei
grandi meriti per avere magistralmente coniugato l'attività in
ambito industriale con la ricerca, la didattica e la divulgazione nel
campo delle discipline geologiche.
Noi, che siamo stati al suo fianco fin dagli anni pionieristici
dell'attività esplorativa dell'AGIP, abbiamo sempre dimostrato
grande apprezzamento per la sua notevole personalità e onestà
intellettuale e, nello stesso tempo, siamo stati gratificati dal suo
esempio di rigoroso ricercatore e di valente scienziato.

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Olistostromes, mélanges and mass-transport deposits
GIAN ANDREA PINI (*), ANGELO CAMERLENGHI (**), KEI OGATA (°), ANDREA FESTA (°°), GIULIA CODEGONE (°°),
CLAUDIO CORRADO LUCENTE (§) & ROGER URGELES (§§)
Key words: Block-in-matrix rocks, chaotic bodies and units,
mass-transport deposits and processes, olistoliths,
olistostromes.
OLISTOSTROMES AND MÉLANGES
The terms olistostrome and olistolith have been introduced by
G. Flores (4th World Petroleum Congress, 1955, Rome) to
indicate either sedimentary bodies with a chaotic block-in-matrix
fabric or single slide blocks, intercalated between layered
sequences in the Tertiary succession of Sicily. Both terms soon
became extensively used by the international geological
community worldwide. With the extended usage, they evolved to
generally indicate stratally disrupted to chaotic complexes and
“exotic” bed packages, which originated by mass-transport
events. In this extended meaning, the concept of olistostrome
played a significant role in other, important scientific debates,
such as the origin of mélanges.
Mélanges are considered the products of either tangential
tectonics, sedimentary processes, mud diapirism, or the interplay
of these processes (FESTA et alii, 2010 and references therein).
Among the sedimentary processes, mass gravitational transport is
appointed to create chaotic, blocks-in-matrix rocks
(olistostromes) that is a possible sedimentary end-member for
mélanges.
Most studies in literature have been aimed at distinguishing
olistostromes from chaotic bodies deriving from other processes
(broken formation, tectonic mélange, mud diapirs), to outline
their paleogeographic distribution according to certain
geodynamic and structural conditions (i.e., subduction vs.
_________________________
(*) Dipartimento di Scienze della Terra e Geologico-Ambientali, Università
di Bologna, gianandrea.pini@unibo.it
(**) Departament d'Estratigrafia, Paleontologia i Geociències Marines,
Universitat de Barcelona, Spain.
(°) Dipartimento di Scienze della Terra, Università di Parma.
(°°) Dipartimento di Scienze della Terra, Università di Torino.
(§) Servizio Tecnico di Bacino, sede di Rimini, Regione Emilia-Romagna.
(§§) Departament de Geologia Marina, Institut de Ciènces del Mar,
Barcelona, Spain.
445
obduction, accretion vs. erosion, subduction of sea mounts), or to
define more or less cyclic tectonic-stratigraphic events. As a
result, olistostromes have been poorly studied from a
sedimentological point of view, with some notably exceptions
(see, e.g., ABBATE et alii, 1981).
OLISTOSTROMES AS MASS-TRANSPORT DEPOSITS
More types of sedimentary bodies are within the
olistostromes, ranging from three end-members:
- bodies with blocks ranging in size from a centimeter to a
meter, dispersed in a clay or sand-silt matrix (type A);
- bodies with larger blocks (olistoliths) ranging in size from
tens to hundreds of meters sustained by a matrix with the features
of a type A olistostrome (type B);
- bodies almost completely consisting of olistoliths, without a
matrix (type C).
Summarizing, the genetic mechanisms of such units span from
debris flows (type A) to blocky flows and slide (B) (MUTTI et
alii, 2006), to avalanches and independent block sliding (C).
The striking feature shared by these units is the more or less
abundant occurrence of a sedimentary matrix, thought to be
primarily produced by 1) recycling of an already formed matrix
from previous mud diapirs- volcanoes or from broken formationstectonic
mélanges, 2) the partial desegregation of the internal
blocks and the erosion of the substrate (MUTTI et alii, 2006;
OGATA, 2010).
DISTRIBUTION OF MASS-TRANSPORT DEPOSITS
In the sedimentary record of collisional chains, the majority of
fossil mass-transport deposits (MTD), including olistostromes,
originated during the stages of intracontinental deformation,
having been deposited in foreland and wedge-top basins. In some
cases, collisional orogeny has allowed MTD related to
extensional tectonics and passive margin to become exposed.
This contrasts with the observed abundance of present-day
MTD, which prevail in passive and divergent margins and along
the flanks of volcanic islands. The present-day submerged
contractional margins, however, do not show a significantly high
concentration of MTD, apart from the erosional margins off the
SESSIONE 13

SESSIONE 13
Fig. 1 – Distribution of olistostromes and olistoliths in the circum-Mediterranean chains (from CAMERLENGHI &PINI, 2009).
coasts of Peru. Basin-wide MTD are only present when
catastrophic events occur, as in the case of the subduction of
seamounts and volcanoes (CAMERLENGHI & PINI, 2009, and
references therein).
There are more, possibly concomitant, explanations to these
discrepancies: 1) the method of investigation might prevent the
imaging of geometrically complicated MTD in present-day
submerged active margins; 2) the large scale MTD originated in
the passive margins completely lack of preservation because of
the intense tectonic reworking during the stages of subduction,
collision and intracontinental deformation, or 3) the MTD
originated in passive margins and accretionary wedges are still
present in the geological record of collisional chains, but their
presence has been disregarded so far.
CONCLUSIONS
Olistostromes are complex MTD, often involving the entire
spectra of mass-wasting processes, which lead to the stratal
disruption and chaoticization of sediments. MTD are a consistent
part of mélanges worldwide, even if strongly deformed by postdepositional,
tectonic and/or mud-diapiric processes. A complete
and integrated sedimentological study of the “olistostromes” can
add a wider spectra of internal structures and flow mechanisms to
the sedimentological knowledge of mass-transport processes.
Moreover, the study of these bodies might help in explaining the
discrepancies about the present-day vs. fossil MTD distribution.
446
REFERENCES
ABBATE E., BORTOLOTTI V. & SAGRI M. (1981) - Olistostromes
in the Oligocene Macigno formation (Florence area).
Introduction: an approach to olistostrome interpretation. In:
F. Ricci Lucchi (Ed.) Excursion Guidebook, IAS 2 nd
European Regional Meeting, Bologna, April 13-15, 1981,
165-185.
CAMERLENGHI A. & PINI G.A. (2009) - Mud volcanoes,
olistostromes and Argille scagliose in the Mediterranean
region. Sedimentology, 56 (1), 319-365.
FESTA A., PINI G.A., DILEK Y., CODEGONE G., VEZZANI L.,
GHISETTI F., LUCENTE C.C., & OGATA K. (2010), Peri-
Adriatic mélanges and their evolution in the Tethyan realm.
Int. Geol. Rev., 52 (4-6), 369-406,
MUTTI E., CARMINATTI M., MOREIRA J.L.P. & GRASSI A.A.
(2006) - Chaotic Deposits: examples from the Brazilian
offshore and from outcrop studies in the Spanish Pyrenees
and Northern Apennines, Italy. - A.A.P.G. Annual Meeting,
April 9-12, 2006, Houston, Texas.
OGATA K. (2010) - Mass transport complexes in structurallycontrolled
basins: the Epiligurian Specchio Unit (Northern
Apennines, Italy). PhD thesis, University of Parma, 476 pp.

A new interpretation of the log of the Pontremoli 1 drilling
(Tuscany, Italy)
Key words: Drilling, hydrocarbon, stratigraphy.
ALBERTO PUCCINELLI (*), GIACOMO D’AMATO AVANZI (*) & NICOLA PERILLI (*)
The Authors propose an updated interpretation of the
Pontremoli 1 stratigraphic log, based on the new tectonic,
lithostratigraphic and biostratigraphic data resulting from the
realization of the new Geological Map of Italy - Sheet n. 233
Pontremoli at 1:50,000 scale.
The Pontremoli 1 hole was drilled in 1971 close to Pontremoli
(Massa-Carrara province, Tuscany) for hydrocarbon searching
(Fig. 1). The first interpretations pointed out some out-of-
447
sequence units (ANELLI et alii, 1994, and bibliography therein)
that the new surface surveys did not verify: the need of
reconstructing a new underground structure comes from this fact.
The Fig. 2 compares the old interpretation of the log and the
new one. From top to bottom, the sequence was reconstructed as
follows (Fig. 2 A). Under a 50 m thick fluvial conglomerate
deposit (Olivola conglomerate), down to the depth of 1285 m the
Ottone Unit (External Liguride Unit) is formed of a great
thickness of the Helminthoid flysch Fm., underlain by its basal
Fig. 1 - Geologic map of the Pontremoli 1 drilling area (after PUCCINELLI et alii, 2004, modified). h1: filling; aa: debris; b: present alluvial deposit; a1a: active
landslide; a1q: dormant landslide; bn: terraced alluvial deposit; OLP: Olivola conglomerate; OTO: Helminthoid flysch Fm.; ARB: Arenarie di Ponte Bratica Fm.;
CGV: Calcari di Groppo del Vescovo Fm.; ACC: Argille e calcari Fm.; MMA: Marne di Marmoreto Fm.; MAC: Macigno Fm.; STO: Scaglia toscana Fm.; MAI:
Maiolica Fm.; DSD: Diaspri Fm.; LIM; Calcare selcifero di Limano Fm.; 1: normal fault; 2: thrust; 3: terrace edge; 4: bedding; 5: debris fan; 6: cross section.
_________________________
(*) Dipartimento di Scienze della Terra, pucci@dst.unipi.it,
damato@dst.unipi.it, perilli@dst.unipi.it
complex (Santa Maria Breccia).
Further down (up to 1794 m) the Canetolo Unit was found. It
is mainly formed of the Argille e calcari Fm. (shale with
SESSIONE 13

SESSIONE 13
Fig. 2 - The the old interpretation of the Pontremoli 1 log (A - after
ANELLI et alii, 1994 - redrawn) and the new one (B).
interbedded limestone) and by subordinate limestone (Calcari di
Groppo del Vescovo Fm.) and sandstone (Arenarie di Ponte
Bratica Fm.).
A cataclasite was pointed out at a depth of 1838 m: it might
have been produced by an east dipping normal fault.
Further down the Falda Toscana Unit (Tuscan Unit) was met:
up to 2567 m the Macigno Fm. (sandstone) and up to 2636 m the
Scaglia toscana Fm. (shale with interbedded limestone) were
drilled, respectively. Between 2636 m and 3060 m of depth an
interval referable to the Calcare cavernoso Fm. and related
breccia was passed. Finally, down to the hole bottom (3520 m)
the metamorphic bedrock was met.
The Pontremoli 1 drilling did not find any hydrocarbon. This
might be attributable to the absence of a reservoir, since the
normal faults displaced eastward the Mesozoic carbonate
sequence of the Falda Toscana.
448
REFERENCES
ANELLI L., GORZA M., PIERI M. & RIVA M. (1994) - Subsurface
well data in the Northern Apennines (Italy). Mem. Soc. Geol.
It., 48, 461-471.

Key words: Biogenic/abiogenic oil generation, expanding earth,
hydrocarbon origin, noncompressional orogenic model.
POSSIBLE NEW HARMONIC SCENARIO FOR
HYDROCARBONS FORMATION
Oil and associated phenomena can be found preferentially
along old fold belts and margins which building models can be
very different in different global tectonics theories. The fold belt
building model proposed in preceding papers by SCALERA (2005,
2007, 2008) can be used to judge if the difficulties encountered
by the different biogenic/abiogenic conceptions can be solved. In
Fig.1 the main characteristics of the model are shown in
connection to the abiogenic/biogenic oil production problem.
The tectonic overpressures (MANCKTELOW, 2008), together
with the higher temperatures available in the model of SCALERA
(2005, 2007, 2008) at shallower depth, can bear a relation with
the synthesis of biogenic and abiogenic hydrocarbons. Indeed
GLASBY et alii (1984) argued that most HCs fields occur in areas
of higher than normal thermal gradient, and the above proposed
model leads just to higher gradients that are produced by the
isostatic uplift of very deep materials (from and above the
transition zone). These higher gradients together with uplifted
contents of mantle metals (catalysts) and hydrogen, can favour
the occurrence of the conditions leading to the development of
the Fischer-Tropsch reaction. The underthrust carbonate slabs can
interact at proper high temperature with hydrogen and catalityc
metals. Pressure range can be very wide both because the
nonlithostatic overpressures (MANCKTELOW, 2008) at the
boundary between uplifting material and adjacent stable or
underthrust lithosphere and occasionally because the inevitable
occurrence of strong earthquakes in some periods of the thrustfold
belts building. Laboratory experiments have ascertained that
calcareous-marly rocks to which friction is applied produce a
strong emission of carbon dioxide and methane of inorganic
origin.
_________________________
(*) INGV – Istituto Nazionale di Geofisica e Vulcanologia – Roma,
giancarlo.scalera@ingv.it
Lavoro eseguito nell’ambito del progetto Geodinamica e Paleogeografia
Globale, con fondi istituzionali INGV
Biogenic and abiogenic hydrocarbons in Italy
GIANCARLO SCALERA (*)
449
Fig. 1 – The connection between the proposed model (SCALERA 2007, 2008)
and various kind of hydrocarbons generation. The convergence of cold and
hot materials, oxiding and reducing environments, the presence of high
nonlithostatic overpressures, and ascending fluids and catalysts, constitute a
favourable dynamical environment in which different types of metamorphism
can be realized at shallower depth, ore deposits can form near the surface and
the synthesis of biogenic and abiogenic hydrocarbons can occur at depths not
exceeding few tens of kilometres.
The compressional state of the gravity-driven nappes, together
with the general rifting environment of the proposed model and
the aperiodic activation of deep change of phase with extrusion of
material below the fold belt, can be facilitating factors in oil
migration towards the surface and its accumulation under
impermeable layers, following the slopes of the underthrust
strata.
The lack of reducing conditions in the upper part of the upper
mantle to be possible the Fischer-Tropsch reaction (GLASBY,
2006), is overcome in this model by the upward isostatic
transport of the reducing transition zone environment. The
criticism of Kenney that suitable TP conditions to produce HCs
can be found only at depth greater than 100 km is overcome by
the transport of such conditions toward the surface. In my
framework a high-temperature reducing environment of
undepleted mantle rises up and come in contact with the
relatively cold oxidizing lithospheric environment. In the
interposed region of thermal gradient, and of hydraulic gradient
due to nonlithostatic overpressures – all at depths not overcoming
few tens of km – a continuum of very different physicochemical
conditions come in existence. A number of chemical reaction are
then favoured in this sort of tectonic oxidizing-reducing pile,
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Fig. 2 – The data of locations and productivity of hydrocarbon fields in Italy
are from PIERI (2001). The maps of the MCS degrees from VIII to XI is
extracted from the Maximum Felt Intensity in Italy that was elaborated by
INGV. The front of the orogen is also shown (from BIGI et alii, 1991). The
hydrocarbons are located beside the eastern side of the highest seismic energy
releases. The further adding to this map of the zones of heat flow greater than
100 mW/m2 shows that a similar warm/cold zonation exists like the one
proposed in the model (fig.1). Highest CO2 emissions can be of mantle origin
or can be produced by the margin of the underthrust carbonatic platform with
the help of the earthquakes. Adjacent to the eastern side of the higher degree
seismicity, and following the Adriatic plate margin (revealed by the long
magnetic anomaly in fig. 2, right), the hydrocarbons has been found in
commercial quantities. They can mostly or partially came from the chemical
reactions envisaged in this paper, and then pushed toward east by hydraulic
gradients and favorable disposition of microfractures and impermeable
sedimentary layers. The two flesh ribbons in the Adriatic sea represent main
seismogenic faults along which new HC fields may be found.
leading to a multiple origin of hydrocarbons.
In addition, near to the surface – in the first few tens of
kilometres – a considerable amount of fluids and of organic
biogenic material of various provenance is present in the
underthrust sedimentary layers, which can participate in a passive
way (contaminant) or active way (transmuting materials,
kerogens) to the HCs forming. However, no evaluation of the
abiogenic/biogenic hydrocarbons rate is yet possible.
The cold side of these regions (e.g. the continental side of the
450
Apennines, the Andes, etc.) should be more suitable for
petroleum exploration, because the squeezing of fluids caused
occasionally by the aperiodic overpressures towards the
decreasing horizontal hydraulic gradient. The horizontal flow
toward the warm side should with great probability disintegrate
the heavy HCs molecules, while they should conserve integrity
going toward the cold region.
In Italy, a simple comparison of the petroleum and gas fields
(data from PIERI, 2001) with the maximum felt intensity (VIII,
XI, X and XI MCS degrees; fig. 2) shows a initial good
agreement of the model and the highest seismic energy release.
The earthquakes seems to enclose an elongated area of tectonic
working in which hydrocarbons can be produced in the depts. and
then expelled laterally toward the cold side of the region. The
‘warm side’ can be considered the region where the volcanic
rocks and the seismicity are located. On this side oil cannot
migrate without be disintegrated. The carbon coming from the
Adriatic carbonatic platform – enriched in 12 C formed by remains
of marine organisms – and the carbon coming from the eventual
maturation and ‘distillation’ of fossil organic remains contained
in buried sediments are today not distinguishable. More deep
geochemical investigations and analyses need in determining the
real nature (biogenic or abiogenic or mixing of them) of the
Italian hydrocarbons.
REFERENCES
GLASBY G.P. (2006) - Abiogenic origin of hydrocarbons: an
historical overview. Resour. Geol. 56 (1), 85-98.
MANCKTELOW N.S. (2008) - Tectonic pressure: Theoretical
concepts and modelled examples. Lithos, 103 (1-2), 149-177.
PIERI M. (2001) - Italian petroleum geology. In: G.B. Vai & I.P.
Martini (eds): Anatomy of an Orogen. The Apennines and
Adjacent Mediterranean Basins Kluver Academic Publishers,
London, 533-549.
SCALERA G. (2005) - A new interpretation of the Mediterranean
arcs: Mantle wedge intrusion instead of subduction. Boll.
Soc. Geol. It., Volume Speciale, 5, 214-218.
SCALERA G. (2007) - A new model of orogenic evolution. Rend.
Soc. Geol. It., Nuova Serie, 5, 214-218.
SCALERA G. (2008) - Great and old earthquakes against great
and old paradigms – paradoxes, historical roots, alternative
answers. Advances in Geosciences, 14, 41-57.

Key words: Divulgazione scientifica, esplorazione geologica,
Giovanni Flores, Italia.
La vita di Giovanni Flores è avventurosa e affascinante. La
sua esistenza passa attraverso profonde esperienze personali e
professionali che colpiscono chi cerca ora di ripercorrerle. Era
nato a Napoli nel 1917 da una antica famiglia di lontane origini
spagnole, che contava anche una discendenza inglese. Si laureò
“cum laudae” presso l’Università di Napoli, nel 1939, in Scienze
Naturali, con una tesi di Geologia. Lavorò, poi, per le più
importanti Compagnie petrolifere, fra cui: Agip, Esso, Gulf,
Amoco, Total, Chevron, Shell e studiò la geologia dei paesi dove,
in quegli anni, cominciava a muoversi l’esplorazione petrolifera.
Le ricerche geologiche lo portarono in giro per il mondo, prima
della II Guerra Mondiale fu in Albania, dopo la guerra a Cuba,
nell’Honduras Britannico (oggi Belize), in Sicilia, in Mozambico,
in Portogallo, in Zaire (oggi Repubblica Democratica del Congo).
In quegli anni i geologi del petrolio erano ancora degli
avventurieri in cerca dell’oro nero attraverso giungle, montagne
deserti. Giovanni Flores è morto il 29 maggio 2008.
All’inizio del suo libro autobiografico “Arc of theSun” Flores
racconta un episodio da lui vissuto in Africa mentre camminava
nella savana verso il kraal 1 ‘Nziri. Le carte che aveva a
disposizione erano imprecise e quando, finalmente, incontra un
anziano indigeno gli chiede quanta strada ci fosse ancora da
percorrere. L’anziano uomo alzò solennemente il suo braccio, lo
puntò al sole e lentamente scese fino a un punto situato circa a
metà strada tra il sole e l’orizzonte: “Lì - disse - è quando tu sarai
a ’Nziri”.
E’ un significativo esempio della capacità di Flores di
comunicare messaggi e sentimenti che fanno profondamente
riflettere. Ma è anche un’interessante osservazione scientifica: lo
spazio da percorrere, talvolta, può essere rappresentato meglio
con il tempo (necessario per attraversarlo).
Troviamo questo sistema di descrizione delle distanze anche
in Europa, dall’antichità fino ai viaggiatori medioevali; poi si
cominceranno ad utilizzare le mappe e le carte, che riportano, in
scala, lo spazio.
1 Kraal deriva da una parola afrikaans kraalen, piccolo insediamento tradizionale
con un recinto per proteggere il bestiame.
__________________
(*) mattia_sella@fastwebnet.it
Arc of the Sun, la forza comunicativa di Giovanni Flores,
pioniere geologo
MATTIA SELLA (*)
451
Ma, forse, come suggerisce Flores, il gesto del vecchio
africano è ancora più efficace di una indicazione che usi dei
numeri convenzionali: giornate, ore, minuti. Questa bellissima
immagine, da lui scelta per il prologo della sua autobiografia,
rappresenta come lui stesso afferma, l’espressione simbolica della
vita di un uomo, dalla nascita alla morte.
Scorrendo quello che Flores ha prodotto durante la sua vita, al
di fuori della sua attività lavorativa, cogliamo la sua grande forza
comunicativa, non solo un’abilità descrittiva ma anche capacità di
sollecitare l’interesse e la curiosità di chi legge i suoi lavori.
Scrisse numerosi articoli scientifici, pubblicati dal Corriere della
Sera, alcuni libri divulgativi, sull’origine delle montagne, sui
terremoti e sulla storia geologica d’Italia. Fu autore anche di due
interessanti romanzi storici. Bellissima è anche la sua affascinante
autobiografia che, giustamente, porta il titolo: “Arc of the Sun.
Adventures of a Petroleum Geologist”. Si dedicò anche alla
docenza a Firenze, a Parma, e in Portogallo. Fu membro del CAI
e di varie associazioni scientifiche (SGI., EAPG, AAPG), alle
quali ha sicuramente portato interessanti contributi.
Proviamo ad analizzare i suoi lavori separatamente, perchè
ognuno è caratterizzato da un diverso modo di “divulgare” e di
comunicare, anche se alcuni efficaci “strumenti” (foto, schizzi,
dipinti ad olio) li ritroviamo, giustamente, riproposti in varie
occasioni.
ARTICOLI DI DIVULGAZIONE SCIENTIFICA
Dal 1983 al 1991 Giovanni Flores scrisse una quarantina di
articoli. In quegli stessi anni furono pubblicati anche interventi di
Marco Pieri con cui, spesso, collaborava. Gli articoli di Flores,
interessanti, curiosi, a volta dilettevoli sono anche capaci di
educare ad osservare e a capire i fenomeni che descrive e a
stimolare l’attenzione su fatti nuovi. I temi trattati, che seguono
forse anche le “mode” di quegli anni, sono abbastanza vari.
La struttura interna del nostro Pianeta ricostruita con i
terremoti era un argomento di interesse, ma i terremoti visti anche
come causa dei cambiamenti della superficie della Terra. In
quegli anni si cominciava a consolidare la Teoria delle Placche e,
quindi, Flores affronta anche il tema del movimento dei
continenti. L’impatto di un meteorite, come causa dell’estinzione
dei dinosauri (65 milioni di anni fa), era certamente un tema
affascinante in quegli anni. Flores scrisse anche su un’altra teoria:
la caduta di un meteorite in Canada, circa 200 milioni di anni fa,
avrebbe causati una rapida estinzione, seguita dalla nascita di
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nuovi generi, fra cui i dinosauri. Abbastanza frequenti sono anche
gli argomenti di geologia, di stratigrafia e di astronomia del
sistema solare. Scrisse, invece, pochi articoli sulle risorse
energetiche, di cui uno, abbastanza originale, sull’esplorazione di
metano abiogenico (“Bucano un cratere di meteorite per scoprire
il metano nascosto”, 1987).
LIBRI DI DIVULGAZIONE SCIENTIFICA
COME NASCONO LE MONTAGNE (UNEDIT, Firenze,
1977) - E’ un piccolo e maneggevole libretto che vuole
comunicare interesse per la geologia e forse Flores pensava
proprio ai frequentatori delle montagne. Il testo è accompagnato
da schizzi e disegni semplici ma estremamente efficaci e di
straordinaria immediatezza, che non hanno niente da invidiare
alle elaborazioni di grafica informatica, a volte di difficile
comprensione. Per spiegare certe situazioni geologiche usa delle
immagini che ricorrono a banali esempi, tratti dalla vita di ogni
giorno, e che proprio per questo sono di straordinaria chiarezza.
Come, per esempio, quando vuole spiegare come riportare
indietro nelle ere geologiche (retrodeformare) la Catena Alpina e
allora schizza una serie di cime, formate da strutture e pieghe
accavallate, disegna sopra un ferro da stiro e, come didascalia,
scrive “se potessimo stirare le Alpi ,,,”. Uno schizzo rappresenta
le grandi fratture dell’Africa Orientale e, con lungimiranza e
sfidando le dottrine allora vigenti (rischiò il licenziamento),
Flores osa correlare, legate agli stessi fenomeni di rift, le fosse a
nord del Lago Vittoria con quelle a sud .
L’ITALIA GEOLOGICA. STORIA DEGLI ULTIMI 230
MILIONI DI ANNI (Longanesi & C., Milano, 1981) - Scritto in
collaborazione con Marco Pieri è la descrizione della storia che
ha modellato le forme del paesaggio, geologico e morfologico,
dell’Italia, dal Triassico ad oggi. Nelle note dei risvolti di
copertina c’è un esplicito collegamento al geologo Stoppani,
autore del “Bel Paese”, abilissimo divulgatore. La prima parte, in
forma scorrevole e discorsiva vuole dare nozioni generali con
particolare attenzione nell’insegnare a osservare. La seconda
parte racconta la storia geologica del nostro Paese, prima a
ritroso attraverso le ere geologiche, dal Quaternario al Triassico,
e poi, di nuovo indietro fino ad oggi. Gli autori non tralasciano un
pizzico di humour e qualche spunto polemico. L’apparato
iconografico è molto ricco: anche qui schizzi e disegni semplici
ed efficaci, foto, carte, e la riproduzione di 18 stupende tempere
settecentesche, paesaggi geologici della zona vesuviana e dei
campi Flegrei, di William Hamilton (1730-1803), ambasciatore
di S.M. Britannica presso il Re delle due Sicilie.
IL TERREMOTO (Longanesi & C., Milano, 1981); nuova
edizione, PERCHE’ IL TERREMOTO (TEA, Varese, 1999) -
Dopo aver spiegato cos’è e come avviene un terremoto, la
previsione, gli effetti e la sismicità in Italia, già nel volume del
1981 Flores inserisce un capitolo dedicato a problemi pratici:
“Vivere con il terremoto”. Nella seconda edizione vengono ancor
452
più approfonditi questi aspetti educativi con l’aggiunta di due
capitoli: “Che fare in caso di terremoto”, “Il dopo terremoto”.
Anche in questi due libretti ci sono chiari disegni e schizzi
esplicativi. L’edizione del 1981 è arricchita da interessanti
documenti storici, difficilmente reperibili altrove.
NARRATIVA
ARC OF THE SUN. ADVENTURES OF A PETROLEUM
GEOLOGIST (Ellen Sue Blakey Ed., Lyon & Thorne Ltd., Tulsa,
1987) - Ellen Sue Blakey, editrice di questo libro, scrive,
nell’introduzione, che sono rimasti in pochi della generazione dei
geologi pionieri dell’industria petrolifera, quando i rilievi
geologici erano lo strumento fondamentale dell’esplorazione,
prima dell’avvento delle tecnologie moderne. E Giovanni Flores
è uno dei pochi rappresentanti di questa generazione. E’ uno
splendido racconto autobiografico, ricco di avventure, emozioni,
sentimenti e poesia, anzi poesie, splendide poesie che si
accompagnano ai momenti gioiosi e a volte anche tristi della sua
vita. Anche in questo libro troviamo bellissimi schizzi e disegni,
fatti non solo per descrivere caratteristiche geologiche ma anche
ambienti e paesaggi. Ci sono anche dei dipinti ad olio molto
suggestivi. Interessanti sono anche le foto, istantanee nate per
documentare aspetti scientifici o tecnici, ma che esprimono anche
le sensazioni e i sentimenti dell’autore.
IL RE NON RISPONDE (Piero Lacaita Ed., 1997) - Anche la
vita della famiglia di Giovanni Flores è affascinante, soprattutto
quella del nonno e dei suoi prozii che vissero la fine del Regno
delle Due Sicilie. Cinque dei sei figli maschi del Colonnello Don
Francesco Flores seguirono la carriera militare. Faceva eccezione
Ferdinando che frequentò l’ambiente liberale di Napoli ed era
amico di Francesco De Sanctis. Filippo sposò Isabella. figlia di
John Oates Vice Console di S. M. Britannica in Sicilia e
proprietario di importanti miniere di zolfo. Ferdinando sposò,
Luisa, sorella di Isabella. Ferdinando era il nonno di Giovanni
Flores. Il libro racconta la storia dell’Unità d’Italia, della
conquista di Palermo e di Napoli, vista dall’altra parte, di chi per
tradizione, cultura, onore, non poteva che restare fedele al Re
borbonico anche quando le illusioni stavano cadendo e ci si
rendeva conto che la guerra era ormai persa. Giovanni Flores
scrive questo bel racconto con profondo affetto, ma anche con
una brillante capacità descrittiva, passando da momenti di grande
storia e momenti di storia minima e intima che, comunque,
costituiscono tasselli insolubili della Storia, con la S maiuscola.
CALABRIA IN FIAMME 1806 (Ursini, Catanzaro, 2002) - Il
romanzo storico descrive i momenti iniziali dell' occupazione
francese della Calabria, che cominciò, nel 1806 con la rivolta di
Soveria Mannelli e con la battaglia di Maida 2 , e si concluse con
la tragica fine di Murat, nel 1815.
2
Maida è in provincia di Catanzaro, la battaglia tra francesi ed inglesi si risolse
in favore di questi ultimi.

Jointing and faulting as a record of stress field variability
at the tip of a salt ridge: the deformation pattern
of the chalk at Laegerdorf, NW Germany
FABRIZIO STORTI (*), FABRIZIO BALSAMO (*), FEDERICO CAPPANERA (**) & GIAMBATTISTA TOSI (°)
Key words: Chalk, faults, joint, salt-related structures, stress
field.
Chalk is predominantly a relatively weak, high porosity white
biomicrite consisting almost entirely of fine grained skeletal
material, particularly coccoliths.
The very small grain size results in a very low primary
permeability.
Despite this, high effective permeability is imparted to chalk
by tectonic fracturing and, consequently, chalk is a well known
hydrocarbon reservoir rock, particularly in regions with salt
diapirs and ridges like the Gulf of Mexico and North Sea,
because of the different trap types associated with these
structures.
The orientation, spacing, persistence, and type of mechanical
discontinuities are all important factors controlling both
permeability magnitude and anisotropy in chalk.
The wide variety of kinematic pathways that can drive the
growth of salt-related structures, and of the corresponding stress
fields, imply that predictions of fracture (joints and fault zones)
and stylolite attributes greatly benefit from field analogue studies.
In this contribution we present results of a field study of the
fracture pattern in the chalk overlying the Krempe salt ridge at
Laegedorf, in NW Germany.
We describe the occurrence, orientation and spacing of joints
and extensional faults as a function of bed thickness and attitude.
The deformational architecture of fault zones as a function of
displacement is also described. Moreover, we present in situ
permeability data collected in undeformed chalk, across tight
joints, and in brecciated chalk.
The field evidence is interpreted in terms of the evolution of
the stress field during salt ridge growth, which is influenced by
both periclinal folding and gentle subsidiary transversal folding.
Implications for fracture pattern predictions in chalk reservoirs
are discussed.
_________________________
(*) Dipartimento di Scienze Geologiche, Università degli Studi Roma Tre,
Roma, storti@uniroma3.it
(**) ENI E & P. Division, S. Donato Milanese
(°) Eni Norge AS, Stavanger, Norway
453
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454

SESSIONE 14
L'inquinamento da fonti naturali:
stato dell'arte e prospettive delle ricerche
CONVENERS
Fabrizio Franceschini (ARPA Toscana)
Massimo Guidi (CNR Pisa)
455
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SESSIONE 14

SESSIONE 14
Occurrence of fibrous minerals from Northern Apennine ophiolites:
comparison among three different tectonic settings
Key words: Asbestos, environmental exposure, Ligurian units,
Northern Apennine, ophiolites.
INTRODUCTION
Northern Apennine is a fold and thrust belt consisting of a
stack of continental and oceanic units. The latter, known as
Ligurian Units, are characterized by Jurassic ophiolite sequences
interpreted as remnants of oceanic and transitional lithosphere of
the western Tethys domain. The ophiolite sequences, according
to their lithostratigrafic and tectonic settings, are assigned to
Internal and External Units (MARRONI et alii, 1998; MARRONI &
PANDOLFI, 2007). In Tuscany, the rocks belonging to ophiolite
sequences may contain fibrous minerals either classified as
asbestos, like chrysotile and tremolite, as well as minerals with
fibrous morphology not still reported as dangerous for the health.
Despite the ban of asbestos for industrial use in Europe, the
excavation of asbestos-bearing rocks, like serpentinites and
gabbros, is allowed for both ornamental stones and raw material
quarrying.
COMPARISON AMONG OPHIOLITES IN DIFFERENT
TECTONIC SETTING
We compared three dissmissed borrow pits belonging to
Ligurian Units in Northern Apennine. Detailed geological
surveys has been performed in the quarry sites in order to identify
the different lithotypes and define their geometrical relationships.
1) Pomaia quarry is a dismissed and restored borrow pit
located in Cecina Valley (Pisa). The quarry face shows good
exposures of all the lithotypes, consisting of lherzolites and
gabbros both cut by cataclasites. These lithotypes belong to an
ophiolite sequence referred to Internal Ligurian Units, where
_________________________
FLAVIA BOTTI (*), DEBORAH DONATIO (*), MAURIZIO GEMELLI (*), MICHELE MARRONI (*),
LUCA PANDOLFI &SERGIO ROCCHI (*)
(*) Dipartimento di Sciente della Terra – Università di Pisa
donatio@dst.unipi.it
Lavoro eseguito nell’ambito del progetto CaMAm - con il contributo
finanziario del Fondo Sociale Europeo 2007-13 – Programma operativo -
Regione Toscana
458
continous, even if deformed under very low-grade orogenic
metamorphism, oceanic sequence can be found. The lherzolites
are affected by serpentinization due to oceanic metamorphism,
ranging from zeolite to upper amphibolite facies. The
serpentinization is responsible of development of fibrous
minerals, like chrysotile and antigorite. In addition, also sepiolite,
mainly along the cataclastic fault zones, is found.
2) Sasso Cinturino quarry is a dismissed and not restored
borrow pit located in Garfagnana, near to Villa Collemandina
(Lucca) and opened in serpentinite rocks belonging to the
External Ligurian Units. The quarry shows bad exposures of
serpentinites and rare rodingites. In the serpentinites, derived
from subcontinental lherzolites, chrysotile and actinolitetremolite
occur as fibrous minerals.
3) Monte Fico quarry is a dismissed and restored borrow pit
opened on the western slopes of Monte Fico in Elba Island, near
Rio Marina (Livorno). According to BORTOLOTTI et alii (2001),
in the Monte Fico area, the serpentinized lherzolites belong to a
tectonic unit regarded as deformed during HP/LT metamoprhism
and thus referred to Schistes Lustrés complex of Alpine Corsica.
This quarry exhibits quite good esposures of serpentinized
lherzolites with antigorite and chrysotile occurrences.
A representative sampling of lithotypes from the three sites
has been carried out, paying special attention to different kinds
and occurrences of fibrous phases. Mineralogical and petrological
observations were performed and required the integrated use of
several analytical techniques. Optical microscopy was useful to
study petrological and mineralogical features, as well as to
observe geometrical relationships of veins at microscale. Powder-
XRD spectra of samples were collected and allow to identify
mineral species in rocks and fibrous phases. Micro-Raman
spectroscopy was a useful technique to distinguish the different
mineralogical species with similar optical and chemical features
(RINAUDO et alii, 2003). SEM-EDS allowed mineral chemistry
determinations as well as observations of their possible fibrous
morphology at the micrometer scale.
The study of these three occurrences allows a comparison
among ophiolitic lithotypes in three different tectonic setting, in
order to highlight the difference in content and tipology of fibrous
minerals. The results of this study represent the starting point for
a correlation between the tectonic setting and the fibrous mineral
content.

Fig. 1 – Serpentine veins in serpentinites from Monte Fico (Elba Island).
Fig. 2 – SEM image of actinolite-tremolite from Sasso Cinturino (Lucca) .
CONCLUSIONS
Fibrous minerals identified in the studied pits are chrysotile
and actinolite-tremolite, classified as asbestos, as well as sepiolite
and antigorite, both occurring with fibrous habit, but not
considered dangerous by present-day regulations. These phases
are widespread in the studied sites: in the host rock, in veins, as
fragments in the ground debris, and in weathered surfaces of
rocks.
Among the acknowledged health problems caused by asbestos
inhalation, epidemiological studies highlight cases of
mesothelioma from environmental exposure. So it would be
necessary to identify and localize the different fibrous minerals in
ophiolitic outcrops. The identification of different fibrous
minerals in Internal and External Ligurian units and the
comparison between these studied sites make ophiolitic outcrops
from Northern Apennine a valuable case study for the estimation
of the enviromental risk linked to the dispersion of asbestos
fibers.
459
REFERENCES
BORTOLOTTI V., PANDELI E. & PRINCIPI G. (2001) – The geology
of Elba Island: an historical introduction. Ofioliti, 26 (2a),
79-96.
MARRONI M. & PANDOLFI L. (2007) - The architecture of the
Jurassic Ligure-Piemontese oceanic basin: tentative
reconstruction along the Northern Apennine - Alpine Corsica
transect. Int. J. Earth Sci., 96, 1059-1078.
MARRONI M., MOLLI G., MONTANINI A. & TRIBUZIO R. (1998) -
The association of continental crust rocks with ophiolites in
the Northern Apennines (Italy): implications for the
continent-ocean transition in the Western Tethys.
Tectonophysics, 292, 43-66.
RINAUDO C., GASTALDI D. & BELLUSO E. (2003) –
Characterization of chrysotile, antigorite and lizardite by FT-
Raman Spectroscopy. Can. Min., 41, 883-890.
SESSIONE 14

SESSIONE 14
Tetrachloroethylene contamination on drinking water wells field in
Pianura Padana
ELEONORA BULLERI (*), MARCO IACOPINI (*), MARCO DOVERI (**), LUIGI MARINI (°) (**),
BARBARA NISI (**) (°°) & FRANCO TASSI (°°) (**)
Key words: Drinking water, pollution, tetrachlorethylene,.
INTRODUCTION
Since 1997 the presence of Tetrachlorethylene (PCE) has
been recognized in the drinking water wells field (DWWF) of the
Pianura Padana plain. In this framework a detailed
hydrogeological and hydrogeochemical study was performed to
formulate a hypothesis on the origin of PCE contamination.
The studied system is a multilayer aquifer with four
permeable horizons, made up of gravel and sandy-gravel,
intercalated to low-permeable horizons (clay and silt). The
drinking water wells field is composed by five wells that intercept
all the four levels.
The first step of this investigation consisted of collecting
information about location of potential pollutant sources like
factories that might produce or use PCE, and of reconstruction of
geological and hydrogeological features of studying area. In the
second step, a field survey has been realized. Sampling waters
from DWWF, domestic wells, piezometers and superficial waters
around the area and measurement of piezometric levels have been
carried out in February 2010. These levels were noted in static
condition except for that of the main drinking well, which is
continuously pumping.
Temperature, pH, Eh, electric conductivity and alkalinity
were measured in the field, whereas major and minor ion (Cl - ,
SO4 2- , NO3 - , Na + , K + , Ca 2+ , Mg 2+ , Cr TOT) and isotopic content
(d 18 O‰ e d 2 H‰) were analyzed in the laboratory using routine
methods. Tetrachlorethylene, trichlorethylene, benzene, carbon
disulfide, 1,1,1-trichlorethane, dimethylsulfide, toluene, 1,1,1trichlorethane,
ethylbenzene were determined according to TASSI
et alii (2008), in order to recognized hydrochemical facies and to
mapping the concentration of PCE on field survey. The
elaboration of piezometric levels allowed to understand the flow
pattern of studying area in two extreme stress condition of the
aquifer.
_________________________
(*) MASSA Spin-off, e.bulleri@massaspinoff.com
(**) IGG-CNR - Pisa, m.doveri@igg.cnr.it
(°) Dipartimento per lo Studio del Territorio e delle sue Risorse – Università
degli Studi di Genova, lmarini@dipteris.unige.it
(°°) Dipartimento di Scienze della Terra – Università di Firenze,
franco.tassi@unifi.it
460
RESULTS
This aquifer have been study through a multidisciplinary
approach: (i) hydrogeological, (ii) geochemical.
From an hydrogeological point of view, the water levels
measured were elaborated obtaining a pseudo-static (only the
main drinking well was pumping) piezometric surface. Moreover,
the elaboration was done also in the extreme situation of
pumping, considering all drinking water wells in operation.
Pumping tests data (ZAVATTI, 1992) regarding the multi-screened
wells of the DWWF show average values of 2*10 -3 m/s, 5.5*10 -3
m 2 /s and 2*10 -4 for K, T and S, respectively. The dynamic levels
were calculated by means of Theis-Jacob methods and using the
known pumping rate and hydrodynamic parameters. Both the
elaborations highlighted a principal feeding of the drinking wells
from the South-East part of the area. In fact, the morphology of
dynamic and pseudo-static piezometer surfaces shows a general
SE-NO flow direction. In the dynamic condition, DWWF
receives water from all directions, at the same time the major
flow rate is from S-E (Fig. 1).
Fig. 1 – Piezometric sketch map in dynamic condition.
For what concerns geochemical investigation, this include a
deterministic approach, consisting of binary diagrams related to
waters classification and isotopic composition, and a

0.75
1.00
50
0.00
0.00 0.25 0.50 0.75 1.00
Mg meq/l
0.75
0.50
0.25
Na+K meq/l
0.00 1.00
geostatistical approach for mapping the parameters of interest.
The DWWF is located next to a river but the analytic results
shows the lack of interaction between superficial water and
groundwater; both are characterized in the triangular plots (fig 1 e
2) by a Ca-HCO3 composition except few waters that show a
Ca,Mg-HCO3 composition (74a, 94a, 50) or a NaOH-HCO3
composition (74b) (Fig. 2). These samples have been collected at
different depth.
As regards the isotopic contents, there is a clear distinction
between groundwater and stream waters, in fact these latter are
characterized by a lower isotopic content on d 18 O‰ and d 2 H‰
likely due to dissolution of the snow fell down on site the
previous weeks. Moreover, the large range of isotopic values of
shallow wells/piezometers (until 45 m) is compatible with a
short-time influence on shallow aquifer by local meteoric
precipitation. Otherwise, for deeper wells (including DWWF) the
isotopic values are within a restrict range and are very similar to
that registered on the same wells by IACUMIN et alii (2009) in
2003-2005 period. These features subject the presence of a longer
and deeper circulation, which is likely fed from the Apennine
relief.
Finally, the spatial distribution of PCE on groundwater shows
that this polluting substance arises with a variable concentration
from 0.2 μg/L to 35.7 μg/L in a restrict area with distinct depths
(Fig. 3) especially on E-SE of DWWF. Because the viscosity of
PCE is much less and the density is larger than those of water,
PCE can infiltrates easily in the unsaturated zone and reaches the
groundwater table (EGUSA et alii, 1993). PCE is present as
0.75
74b
74a
94a 92
0.50
0.25
Ca meq/l
1.00
0.00
0.00 0.25 0.50 0.75 1.00
SO 4 meq/l
Fig. 2 – Ternary plots.
0.50
0.25
Cl meq/l
0.00 1.00
0.75
Drinking water wells
Domestic wells
Piezometers
Stream waters
0.50
0.25
HCO 3 meq/l
461
separate liquid phase and probably accumulates itself in
correspondence to depression zones of the bottom of the aquifer.
Fig. 3 – Spatial distribution of PCE. In blue are represented piezometric contours
and the value of piezometric level (m s.l.m), in black are represented the sampled
points and their code (49, 57, 53, 51 and 62 are drinking water wells) and in red
the fluctuation of PCE.
The lack of Cr TOT in water sampled allows to exclude the
hypothesis of an accidental leakage from galvanic processes
adopted by carpentry industry located on upstream of DWWF.
The comparison between hydrogeological and geochemical
results and the presence of an zone characterized by high PCE
concentration located in the S-E of the investigated area, indicate
that possible origin of contamination could be an illegal disposal
of mud’s laundry on S-E of DWWF.
REFERENCES
EGUSA N., JINNO K., NAKAMUTA K., HIRONAKA H., MATSUFUJI
Y. & ISHIBASHI T. (1993) – A hydrogeological study of
groundwater pollution by tetrachloroethylene. Tracers in
Hydrology, 215, 125-134.
IACUMIN P., VENTURELLI G. & SELMO E. – Isotopic features of
rivers and groundwater of the Parma Province (Northern
Italy) and their relationships with precipitation. J. Geochem.
Explor., 102, 56-62.
TASSI F., BUCCIANTI A., CAPECCHIACCI F., MONTEGROSSI G.,
VASELLI O. & MINISSALE A. (2008) – Metodo d’analisi e di
riconoscimento dei Composti Organici Volatili (COV) in gas
vulcanici, idrotermali e del suolo. CNR-IGG Rapporto
Interno n. 1/2008, 12 pp.
ZAVATTI A. (1992) – Studi sulla vulnerabilità degli acquiferi 3,
alta e media pianura parmense. Quaderni di tecniche di
protezione ambientale, 20, 163.
SESSIONE 14

SESSIONE 14
Key words: Asbestos, fibrous minerals, Northern Apennine
ophiolites, serpentinites.
INTRODUCTION
The Northern Apennine is characterized by the occurrence of
well preserved Jurassic ophiolites in the Ligurian Units.
Ophiolitic lithologic types may contain fibrous minerals, with
most of them, although not all, classified as asbestos. Only the
minerals classified as asbestos are considered dangerous, even if
several Mg-rich fibrous silicates are regarded as potential
candidates to promote adverse effects on human health.
The environmental risk connected with the exposure to
natural-occurring asbestos can derive from the fiber dispersion
produced by both natural processes and human activities.
In the ophiolitic sequences of the Northern Apennine there are
almost seventy quarry sites where rocks are crushed for the
production of raw materials (VOLTAGGIO & SPADONI, 2007).
Different countries adopt their own regulation for the evaluation
of fiber dispersion from asbestos-bearing rocks. Despite this, no
standard protocols are up to now defined for a complete
assessment of the fibrous mineral content preliminar to
excavation.
THE STUDY CASE
The study case is represented by ophiolitic rocks, belonging
to the Internal Ligurian units, well exposed in a restored quarry
near Pomaia, Santa Luce (Pisa).
The quarry face shows good exposures of all the lithotypes,
consisting of serpentinites, gabbros and cataclasites. Serpentinites
are almost all tectonitic lherzolites having variable degrees of
serpentinization. These rocks display a network of veins filled by
serpentine group minerals, which occur as emerald green
isotropic or light green to white fibrous. Veins with fibrous
_________________________
Estimate of fibrous mineral content in asbestos-bearing rocks
from southern Tuscany: a case study
(*) Dipartimento di Scienze della Terra - Università di Pisa,
donatio@dst.unipi.it, marroni@dst.unipi.it, rocchi@dst.unipi.it
DEBORAH DONATIO (*), MICHELE MARRONI (*) & SERGIO ROCCHI (*)
462
infilling show well-developed mediam line and fibers showing
progressive rotation. Gabbros are intruded in serpentinites as 5-
60 cm thick dykes or 1x20 m sized stocks (Fig. 1). Wide
cataclastic zones cut both serpentinites and gabbros. These zones
contain brownish mm-thick sheets of a fibrous phase (Fig. 2).
At the meso-scale, the geometric relationships between the
different lithotypes indicate that the lherzolites were intruded by
gabbro dykes and subsequently serpentinized with widespread
development of serpentine veins. The cataclastic deformation,
that affects both gabbros and serpentinites, represents the latest
event, probably still in the oceanic setting, according to
recrystallization of chrysotile among the fragments. Integrated
analytical methods allowed to identify the fibrous phases.
The identification of fibrous phases has required the
Fig. 1 – Gabbro dyke intruded in serpentinite, both crosscutted by
serpentine veins.
Fig. 2 – Cataclasite and brownish sheets of sepiolite.

integration of several analytical techniques (COMPAGNONI &
GROPPO, 2006), such as XRPD, SEM-EDS (Dip. di Scienze della
Terra, Università di Pisa), and micro-Raman spectroscopy
(Centro Scansetti, Dip. di Scienze Mineralogiche e Petrologiche,
Università di Torino). Minerals occurring with fibrous shape in
Pomaia quarry are: chrysotile, antigorite and sepiolite.
Fig. 3 – Fibrous serpentine veins.
The quantitative estimate of lithotypes and fibrous phases of
the Pomaia quarry was performed using a multi-scale image
analysis, from outcrop scale to thin section scale. A multi-scale
approch for quantitative estimation of fibrous phases was set up
for serpentinites.
The processing of a photographic survey, integrated with field
data, led to a quantitative estimate of lithotypes: 67% for the
serpentinites 9% for the gabbros, and 24% for the cataclasites. A
photographic sampling of ten areas on serpentinitic exposures
was performed in order to take a representative picture of the
distribution of discontinuities in the studied rocks. The serpentine
veins at meso-scale were quantified by image analysis and turned
out to be about 13 vol% of the total serpentinite volume.
Analytical evidences and observations on thin sections were
integrated. An image analysis was performed to quantify the
minerals representing potential source of fibers at the microscale.
The percent of these minerals amounts to 73% of the
serpentinites.
CONCLUSIONS
Detailed field observations as well as petrological and
mineralogical studies of the ophiolitic samples have been
integrated with image analysis at different scales. This integration
of methods allowed to quantify the phases which are potentially
sources of mineral fibers.
The integration of data at outcrop, meso- and micro-scale
suggests that this material represents about 54 % of the total
volume.
The set-up of a multi-scale investigation protocol to study
463
asbestos-bearing rocks, is thus essential also to perform a
representative sampling for the evaluation of potential fiber
dispersion.
REFERENCES
COMPAGNONI R. & GROPPO C. (2006) - Gli amianti in Val di Susa
e le rocce che li contengono. Rend. Soc. Geol. It., 3, 21-28.
VOLTAGGIO M. & SPADONI M. (2007) – Variation of geochemical
risk associated with the use of ophiolitic washing mud as
refilling material in a basalt quarry of the Northern Apennine
(Italy). Environ. Geol., 53, 417-432.
SESSIONE 14

SESSIONE 14
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SESSIONE 14

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SESSIONE 14

SESSIONE 14
Boron concentration in humic and fulvic acids of soil epipedon in
San Vitale pinewood (Ravenna, Italy)
MADDALENA PENNISI (*), EMMA DI GREGORIO (*), SERENA CARBONE (**) & LIVIA VITTORI ANTISARI (**)
Key words: Boron, fulvic acid, humic acid, soil epipedon.
INTRODUCTION
The aim of this study is to investigate boron in humic
substances (e.g. humic and fulvic acids) of soil epipedon. The
knowledge of the mechanisms of boron interaction with soil
organic matter (SOM) is important to better constrain the
water/rock interaction in the shallow environment. High
concentration of humic and fulvic acids are available in soils and
subordinately in sediments. These substances could potentially
act as a significant reservoir of boron as well as a source of this
element to soil solution, rivers, and lakes. SOM consists of
complex polymeric organic compounds which are more resistant
to decomposition than the non-humic material. Humified SOM
plays a crucial role in the assessment of soil quality, since it
makes up significant part of the total organic carbon and nitrogen
in soils, recalcitrant to microorganisms. Humus also increases the
buffering action of soil and the capacity in ion exchange,
facilitating thus the absorption of micronutrients by the plant
roots. Humus-enzime complexes are considered to be of great
importance in soil fertility since they represent a link between
inorganic and organic reaction in soils (CECCANTI et alii, 1994).
Compared with other nutrient elements, the chemistry of boron in
soils is very simple. Boron does not undergo oxidation-reduction
reactions or volatilization in soils. Boric acid is a very weak,
monobasic acid, that in solution forms borate anion. Boron
concentration in soil solution is mainly related to
adsorption/desorption reactions, that are controlled by its
availability in soils, solution pH, soil texture, soil moisture, and
temperature (GOLDBERG, 1997).
_________________________
(*) Istituto di Geoscienze e Georisorse, CNR, Pisa, m.pennisi@igg.cnr.it,
e.digregorio@igg.cnr.it
(**) Dipartimento Scienze e Tecnologie Agroambientali, Università Bologna,
s.carbone@unibo.it, livia.vittori@unibo.it
The research is partially supported by a grant from the Italian Ministry of
University and Research (PRIN 2007-20077A9XJA), coordinated by Prof.
U.Masi
474
Boron is an essential micronutrient for plants, but the
concentration range between deficient and toxic is narrower than
for any other nutrient element. Plants respond directly to boron
content in soil solution, and only indirectly to boron adsorbed
onto soil constituents.
Togheter with inorganic compounds (oxides, hydroxides, clay
minerals) organic matter represents one of the significant boronadsorbing
surface. SOM adsorbs more boron than mineral soils
on a weight basis (GU &LOWE, 1990); this process increases with
increasing pH, and reaches a maximum at pH=9 (GU &LOWE,
1990, LEMARCHAND et alii, 2005). Boron adsorption reaches
equilibrium rapidly (hours) and is enhanced by increasing ionic
strength of the solution. Important insight on the mechanisms that
control boron adsorption and isotopic fractionation on humic
acids were achieved by LEMARCHAND et alii (2005). An attempt
is here done to determine the boron content of humic and fulvic
acids (HA and FA, respectively), isolated by soil epipedon in San
Vitale pinewood (Ravenna, Italy).
METHODS AND RESULTS
The San Vitale pinewood is a site of community importance
and its soil is affected by contamination from saline waters and
from atmospheric deposition. The soil profiles here studied are
classified as Sodic Psammaquents (Pin 3 and Pin 9) and Typic
Psammaquants (Pin 5). The humic substances are extracted from
epipedon (A-1 horizon), that is more rich of organic carbon than
the deeper horizons. The extraction is carried out using NaOH
1M Suprapur, with a 1:10 ratio (wt/vol) for 24 hours at 65°C.
After centrifugation, the samples are filtered at 0.45μm
(Millipore system). The supernatant is acidified at pH

weighted (about 0.1 and 0.02 g, respectively), then mixed with
boron free- K2CO3 (1:5 wt ratio) in Pt-Ir crucibles. The samples
are then fused, and the fusion cake dissolved in ultrapurified
water. The insoluble phase is centrifugated, and a weighted
amount of the supernatant processed according to the three-steps
ion-exchange procedure, described in TONARINI et alii (1997).
HNO3 (2%) is then added to the eluted, and the solution finally
analyzed by ICP-OES.
Boron concentration measured in humic substances ranges
between 65 and 240 μg B/g organic acid. FA samples result
enriched in boron respect to HA. Data gained on the three soil
samples do not highlight a clear correlation between boron and
organic carbon. Results of this study confirm that boron sorption
on HA and FA is significant, and could play an important role in
the boron geochemical cycle.
To evaluate the influence of SOM on boron sorption (and
release) in soils further investigation is required in soils from
different geological context and/or areas with different soils use
and management. These preliminary data encourage carrying on
sophisticated analyses, including PTIMS ( 11 B/ 10 B ratio), and 11 B
NMR.
ACKNOWLEDGEMENTS
Dr Matteo Lelli is thanked for the availability of ICP-OES
facilities. MP and EDG are grateful to B. Ceccanti and C.
Macci for helpful discussion.
REFERENCES
CECCANTI B., MASCIANDARO G. & GARCIA C. (1994) -
Biomonitoring the environment and its functionality. InB.
Ceccanti and C. Garcia (eds) - Environ. Biochem. Practice
Waste and soil Management. Pisa, 1-24.
CIAVATTA C., GOVI M., VITTORI ANTISARI L. & SEQUI P. (1990) -
Characterization of humified compounds by extraction and
fractionation on solid polyvinil pirrolidone. J. Chrom., 509,
141-146.
GOLDBERG S. (1997) - Reaction of boron with soils. Plant and
Soil, 193, 35-48.
GU B. & LOWE L. (1990) - Studies on the adsorption of boron on
humic acids. Can. J. Soil Sci., 70, 305-311.
LEMARCHAND E., SCHOTT J. & GAILLARDET J. (2005) - Boron
isotopic fractionation related to boron sorption on humic
acid and the structure of surface complex formed. Geochim.
Cosmochim. Acta, 69 (14), 3519-3533.
TONARINI S., PENNISI M., & LEEMAN W.P. (1997) - Precise
boron isotopic analyses of complex silicate (rock) samples
475
using alkali carbonate fusion and ion-exchange separation.
Chem. Geol., 142, 129-137.
SESSIONE 14

SESSIONE 14
Natural origin hydrocarbon contamination in waters of carbonatic
domains of Abruzzi Apennines
Key words: Abruzzi Apennines, bituminous impregnations,
hydrogeochemistry, natural contamination, oil shales.
The work descends from presence within carbonatic
stratigraphic successions in Apennines of situations connected to
naphtogenesis and their potential interaction with groundwater.
To perform the investigation several sites are been located: 13
springs of different contexts like oil shales, liquid and solid
petroleum happenings, mineralized and sulphurous waters are
been analyzed for their geological, stratigraphic, hydrogeological,
hydrochemical and hysotopic characteristics.
Results display presence of not-anthropic pollution-derivation
contaminants those are sometimes higher than legal limit for
human drinking water.
The points where is studied water-rock interaction concern
with 3 different geological contexts: Gran Sasso Range, Majella
and Morrone mountains; in each site geological, stratigraphic,
hydrogeological, hydrochemical and isotopic features have been
analyzed. Study cases already treated have been collected as
following (Figs. 1 and 2):
- South Gran Sasso Range, springs fed by partially or totally by
aquifers formed of black shales belonging to Dolomie
Bituminose Formation (Upper Triassic; ADAMOLI et alii,
1990);
- Morrone Mountain, springs partially or totally supplied by
aquifers that have within hydrogeological complexes with
liquid petroleum impregnations of Bolognano Formation
(Miocene; CONESE et alii, 2001);
- Majella Mountain, springs partially or totally supplied by
aquifers that have within hydrogeological complexes with
solid impregnations as asphalt like it happens in Bolognano
Formation (Miocene; NANNI &RUSI, 2003);
- North Gran Sasso Range, springs flowing from Apennines
carbonatic aquifers affected by apparently anomalous
contaminations due to by-products of hydrocarbons
(PETACCIA &RUSI, 2008).
Work methodology primarily considered historical review of
information regarding study sites particularly quarries, followed
by geological and hydrogeological setting definition.
_________________________
(*) Università degli Studi “G. d’Annunzio” di Chieti Dipartimento di
Geotecnologie per l’Ambiente ed il Territorio (DiGAT),
riccardopetaccia@hotmail.it
(**) Università degli Studi “G. d’Annunzio” di Chieti Dipartimento di
Geotecnologie per l’Ambiente ed il Territorio (DiGAT), srusi@unich.it
RICCARDO PETACCIA (*) & SERGIO RUSI (**)
476
Fig. 1 – Geological sketch map of studied areas (PETACCIA, 2010).
Studies conducted till now regarded chemical characterization
of bituminous rocks s.l. and physical-chemical and
hydrochemical ones of water points. In order to characterize solid
matrix (bituminous rocks s.l.) two different analytical methods
have been used: the first is normally used to determine organic
matter concentration in natural soils and/or sewage sludge (italian
law limit: threshold concentration of contamination, CSC=1000
mg/l – D. Lgs. 152/2006); the second one (transfer test) in waste
in order to find the amount of hydrocarbons that can be
transferred to water (CSC=350 mg/l).
On the other hand with respect to water samples, the analysis
carried on concern with parameters that can evaluate the
concentration and presence of hydrocarbons in water: total,
volatile and polycyclic aromatic hydrocarbons (THCs with
CSC=350 mg/l, VHCs and PAHs respectively with various
CSCs; Tab. 1).
Surveying of data have been completed by using previous
isotopic characterization of waters with new determination of 18 O
and 2 H stable isotopes.

Tab. 1 – Results of chemical analysis carried out on water samples collected at interest points from February 2008 to August 2009; expressed values in μg/l.
THC confidence limit = 20 μg/l; CSC of THCs 350 mg/l; in grey values above CSC; at March 2009 there is systematic presence of PAHs (PETACCIA, 2010).
Ongoing investigations are carried on to determine polycyclic
aromatic hydrocarbons (PAHs) dissolved in water by validating
and calibrating analytical methods to be applied to interest sites
and whose results must be compared with both existing
legislation and still open questions here studied.
Fig. 2 – Geological section across Fornaca spring (South Gran Sasso Range;
PETACCIA, 2010).
Obtained results show how there is certain presence of
hydrocarbons largely in analyzed water points, so that initial
hypothesis is confirmed.
In two sources, according to existing legislation, is exceeded
the threshold concentration of contamination so that they would
be “contaminated sites” (Tab. 1): one is Rionne spring, collected
for drinking water; until now, exceeding of THCs’ CSC is happen
one time (September 2008). So, there's a need to revalue the
threshold concentrations of contamination in studied areas, in
similar zones and in geological frameworks not considered yet,
increasing case studies: in fact, can one suppose that alluvial and
lacustrine deposits that leached peats, for example, may enrich
with examined substances. One also need to find out laws to
adopt whereas this kind of “natural contamination” is so high to
pass the concentration threshold. Among open issues, there are:
execution of new research campaigns, with chemical analyses
even in double blind and the expansion of researches to other
Italian areas characterized by similar geologic conditions.
Moreover one should estimate the effects of results on the
management and distribution of drinking water together with
responsible agencies (ARTA, aqueduct consortia, etc.).
477
REFERENCES
ADAMOLI L., BIGOZZI A., CIARAPICA G., CIRILLI S., PASSERI L.,
ROMANO A., DURANTI F. & VENTURI F. (1990) – Upper
Triassic bituminous facies and Hettangian pelagic facies in
the Gran Sasso Range. Boll. Soc. Geol. It., 109, (1), 219-230.
CONESE M., NANNI T., PEILA C., RUSI S. & SALVATI R. (1990) –
Idrogeologia della Montagna del Morrone (Appennino
Abruzzese): dati preliminari. Mem. Soc. Geol. It., 56, 181-
196.
NANNI T. & RUSI S. (2003) – Idrogeologia del massiccio
carbonatico della Majella (Appennino centrale). Boll. Soc.
Geol. It., 122, 173-202.
PETACCIA R. (2010) – Contaminazione da idrocarburi di origine
naturale nelle acque dei domini carbonatici e terrigeni
dell’Appennino abruzzese. Tesi di dottorato XXII ciclo in
Geologia Applicata all’Ambiente ed al Territorio, Università
degli Studi “G. d’Annunzio” di Chieti-Pescara.
PETACCIA R. & RUSI S. (2008) – Idrogeologia delle sorgenti del
Ruzzo (Gran Sasso d’Italia). Giorn. di Geol. App., 8 (1), 17-
28.
SESSIONE 14

SESSIONE 14
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478

Isotope geochemistry to assess water quality in artificial canal
network from the Ravenna coastal plain (Italy)
LIVIA VITTORI ANTISARI (*), SERENA CARBONE (*), GILMO VIANELLO (*), MADDALENA PENNISI (**),
ALESSANDRA BRACCESI ADORNI (**), UMBERTO AVIANI (°) & RICCARDO PETRINI (°)
Key words: Coastal plain, geochemistry, isotopes, metals,
surface waters, water/rock interaction.
Several trace elements are considered priority pollutants in the
environment. They can be derived from both natural (geogenic)
and anthropogenic sources. Natural sources include rocks and
minerals, while anthropogenic sources include mainly agriculture,
industrial activity and energy production. In aquatic systems,
freshwater are contaminated by trace elements due to runoff and
drainage of soils and sediments. In the near-surface environment
metals and metalloids undergo a series of dynamic geochemical
and biogeochemical processes that affect the speciation and
consequently solubility, mobility, bioavalibility and toxicity.
Coupled to fluid chemistry, isotopes provide a powerful tool to
trace the origin and processes controlling trace elements
distribution in the shallow environment. Isotopes of elements
with a conservative behaviour, such as oxygen and hydrogen,
trace the effects of mixing between different water reservoirs and
physical-chemical processes such as evaporation, while the
isotopic composition in water of non-conservative elements, such
as strontium and boron, provides information on both mixing
process, including the possible effects of anthropogenic input/s,
and on interaction processes between water-soil and waterorganic
compounds.
In the last century main topographic changes were induced in
the Ravenna area by groundwater exploitation. These variations
combined with a natural subsidence rate of 1 mm/year, caused by
compactation of local alluvial deposits.
Land subsidence has dropped most of the territory below the
mean sea water level, requiring the organization of a drainage net
in order to keep the agricultural land dry. The geochemical and
____________________
(*) Dipartimento di Scienze e tecnologie Agroambientali, Università di
Bologna, livia.vittori@unibo.it, serena_carbone@libero.it,
gilmo.vianello@unibo.it
(**) Istituto di Geoscienze e Georisorse, CNR, Pisa, m.pennisi@igg.cnr.it,
a.adorni@igg.cnr.it
(°) Dipartimento di Scienze della Terra, Università di Trieste,
aviani@units.it, petrini@units.it.
The research is partially supported by a grant from the Italian Ministery of
University and Research (PRIN 2007-20077A9XJA), coordinated by Prof.
U. Masi.
479
isotopic characteristics of irrigation canals and ditches in the
Ravenna area were investigated in order to characterize the
elemental sources, and to evaluate their relationship with the
management of the hydrographical system.
The investigated canal network is delimited northward by the
Lamone river, southward by the Montone river, and by the
Canale Emiliano Romagnolo (CER) in the western sector. On the
eastern boundary a coastal lagoon, called Piallassa Baiona, is
located; it was formed after the hydraulic action devoted to the
optimization of canal, ditches and river regime. Today, the
lagoon allows to prevent salinitation along the historical
landmark of the San Vitale forest, planted by monastic
communities on the fossil dunes formed in the period 10th – 15th.
Above the Pleistocene alluvial plain, continental (marsh
lagoon) and marine (sand and sand-clay alternation) sediments
were deposited in a coastal environment of the Po plain. Along
the catchment of the Lamone river marl-arenaceous, silty-clay
and sandy formations Pliocene and Pleistocene in age, and chalk
are present; thermal springs overflow occur (e.g. Brisighella
area). In the Montone river catchment marly and clay, mainly
outcrop.
The ditches net and the Lamone river are partly equipped with
dams and draining pumps that allow surplus discharge into the
Pialassa during the winter, and prevent saltwater encroachment.
Some locks designed to capture water for irrigation, however are
too far inland to prevent the saltwater from coming in. Land use
and irrigation of the area is mainly related to distribution of the
CER water, that during summertime fed about 25000 ha, and
contributes significantly in supplying the 33.2million m 3 /year
needed for local industrial and agriculture uses. CER, feed by an
impressive pumping station that takes water from the Po river,
was built in response both to the need to defend the land against
the flood water of the different rivers (e.g. Reno river, Lamone
river) and to demand for irrigation water.
From February 2009 till October 2009, surface waters were
collected monthly from selected canals and ditches. Isotope
analyses were performed in waters from canals, and from the
Lamone and Montone rivers, sampled on Mars and July i.e.
during contrasting seasonal regime, related to the agricultural
activity.
Seven ditches were also selected for sediment sampling.
SESSIONE 14

SESSIONE 14
In canal samples, the positive correlations of metals with
aluminum suggest that the alluvial deposits of this area have
similar geochemical features; Lamone sediment makes exception.
In surface water major, minor, and trace elements were
analyzed, togheter with H, O, B, Sr isotopic compositions. The
O2 content, and the chemical and biochemical oxygen demand
were also determined. Different processes concurs to infer the
chemical and isotopic characteristics of the shallow waters here
investigated. Light-induced processes control the cycling of
metals, and in particular of Fe, and Mn, as indicated by
correlations between O2, pH and metals.
Biological photosynthesis is also suspected to play a role in the
transformation of N-compounds; waters are generally
characterized by high NO2 contents (up to 0.2 mg/l), while NO3
is less than 10 mg/l. On march, δD and δ 18 O deviation indicates
that evaporation occurs during the low-flow period, i.e. when
canals are not feed by CER. A moderate saline intrusion (up to
15%) is evidenced by δ 18 O, δ 11 B, and Cl content, in canal waters
sampled 8-10 km far from the coastal line, while sea water
dominates (=80%) in samples located close to the Pialassa
Baiona, as also shown by δ 11 B value of 37‰, that approaches the
marine (39‰). However, water chemistry cannot simply be
explained by mixing process between the fresh component
(Lamone and Montone rivers, CER) and sea water.
Evidence of mineral weathering and/or leaching are mainly
inferred by the 86 Sr/ 86 Sr signature, the Ca and Sr elemental
concentrations, and subordinately by the δ 11 B signature.
Chemical and isotopic characteristics of water from canals,
ditches and rivers that feed the Pialassa Baiona confirm that
drainage from the agricultural area play a role in assessing canal
chemistry but, exception made for Fe and Mn, it does not cause
significant pollution on the water network.
.
480

SESSIONE 15
Sistemi carbonatici, antichi e moderni.
Processi e prodotti sedimentari
CONVENERS
Bruno D'Argenio(CNR Napoli)
Gloria Ciarapica (Università di Perugia)
Anna Gandin (Università di Siena)
481
SESSIONE 15

SESSIONE 15
Barremian-Aptian shallow-water carbonates
of Monte Faito (Sorrento Peninsula, southern Italy).
Microstratigraphy, cyclostratigraphy and sequence stratigraphy
Key words: carbonate platform, depositional sequences,
eustatic cycles, facies analysis.
Shallow-water carbonates are sensitive recorders of eustatic
and climatic changes and can reveal the relative importance of
global and regional controls on carbonate platform evolution.
This study contributes to better understanding of the
Barremian-Aptian interval, a period of well-known climatic and
environmental changes towards more intensified greenhouse
conditions.
This work is part of a larger project concerning the timeequivalent
carbonate platform sediments cropping out in central
and southern Apennines and belonging to different
paleogeographic domains (cfr. AMODIO, 2006, 2008; AMODIO
et alii, 2008; D’ARGENIO et alii, 2004; 2008; FERRERI et alii,
2004: RASPINI 2001). Here are presented results on highresolution
sedimentological analysis of the Monte Faito
carbonate sequence (Campanian Apennines) about 90m thick,
that includes the Barremian/Aptian boundary. This succession
is well exposed in a road-cut along the south-western flank of
Monte Faito (Monti Lattari, Sorrento Peninsula) which is part
of the Alburno-Cervati Unit, derived from the Late Tertiary
deformation of a carbonate platform-basin system. This section
was chosen for its stratigraphic completeness, low tectonic
deformation and well-stratified calcareous rocks that allow to
continue downwards the microstratigraphic analysis of RASPINI
(2001) who studied the upper Aptian – lower Albian interval.
Microfacies analysis has been carried out using more than
500 polished rock slabs and 144 thin sections. The most
common fossils are benthic foraminifers, green algae and
ostracods locally associated with bivalves and gastropods. In
some case, encrusting assemblage of Bacinella-Lithocodium
forms very dense framework associated with rudists,
orbitolinids, echinid fragments, rare corals or more frequently it
shapes large and small oncoids. Salpingoporella muhelbergi
_________________________
(*) Dipartimento di Scienze per l’Ambiente, DiSAm, Università degli Studi
Parthenope, Napoli, sabrina.amodio@uniparthenope.it
SABRINA AMODIO (*)
482
and Salpingoporella melitae, associated with Debarina sp
suggest a Barremian age for the lower-middle part of the
section, while Salpingoporella dinarica, Triploporella
marsicana, Coptocampylodon fontis, associated with Debarina
sp., Palorbitolina lenticularis (as more evolute forms) and
Praechrysalidina infracretacea indicate the Aptian for the
upper part of the section.
The microstratigraphic analysis of depositional and early
diagenetic features has allowed to recognize 11 lithofacies
organized in 4 lithofacies associations (AMODIO, 2008). For-
Ostr-Algal and Bio-Peloidal limestones, intercalated with
Laminate limestones are dominant in the lower-central part of
the section; here early marine diagenesis passes more
frequently to early meteoric, deeply penetrating diagenesis
testified by paleokarstic dissolution and cavities, pseudobreccia
or paleosols with laminated-massive horizons (Em2type
surface). Bacinella-Molluscan and Bio-Peloidal limestones
locally intercalated with For-Ostr-Algal limestones prevail in
the upper part of the section, where microkarst and weakly
pedogenesis (Em1-type surface) are normally superimposed on
subtidal deposits. The environmental interpretation has allowed
a facies model to be restored, that corresponds to a shallow
carbonate platform, where open lagoon environments are
transitional to peritidal zone.
By these observations, recurrent variations of lithofacies
and their grouping as well as evidence of variable penetration
depth of early meteoric overprint directly superimposed on
subtidal deposits, record sea-level oscillations, suggesting a
cyclicity hierarchically organised in elementary cycles, bundles
and superbundles. Commonly, 2-6 elementary cycles form a
bundle while 2-4 bundles constitute a superbundle; this
suggests that some elementary cycles and/or bundles may be
missing when accommodation space was reduced. Considering
the total 90m-thick section, 127 elementary cycles were
individuated with an average thickness of 71cm; these are
organised into 34 bundles and into 11 superbundles (Fa1-Fa11)
with an average thickness of 260 cm and 872 cm respectively.
These high-frequency cycles appear to be superimposed on
lower-frequency (=800 ka) Transgressive/Regressive Facies
Trends (T/RFTs).
As recognised for other carbonate sections, elementary

cycles correspond to precession/obliquity signal, while bundles
and superbundles evidence short and long eccentricity signals
(Milankovitch cyclicity). However, in addition to the allocyclic
control, autocyclic processes can not be excluded. The external
(allocyclic) control on sedimentary cyclicity could be
confirmed by spectral analysis of stratal features and
thicknesses that will be possible carried out briefly.
Moreover, by using sequence-stratigraphy concepts, it was
possible to recognize emersion and maximum-flooding surfaces
as well as upwards deepening-shallowing stacking patterns of
cycles. This platform was able to fill up all the accommodation
space until its emersion, forming more pronounced cycle limits
(sequence boundaries, SB), corresponding with the Em2 type
surfaces. The superbundles and the Transgressive/Regressive
Facies Trends (T/RFTs), interpreted as depositional sequences,
can be used for high-resolution regional correlations with time
equivalent sections (Monte Raggeto and S. Maria) already
studied in the same way.
To this aim a high-resolution isotope stratigraphy was
produced at the IAMC-CNR (Naples) isotope geochemistry
laboratory to confirm the regional correlation and to evaluate
relationships between global C-cycle perturbations and biotic
turnover documented in this time interval.
REFERENCES
AMODIO S. (2008) - Barremian-Aptian shallow-water
carbonate of Monte Faito (Sorrento Peninsula, southern
Italy). Record of bio-sedimentary rhythmicity?
Preliminaruìy results. Rendiconti on-line Soc. Geol. It., 3,
23-24.
AMODIO S. (2006) - Foraminifera diversity changes and
paleoenvironmental analysis: the Lower Cretaceous
shallow-water carbonates of San Lorenzello, Campanian
Apennines, southern Italy. Facies, 52, 53-67.
AMODIO S., FERRERI V., D’ARGENIO B., WEISSERT H. &
SPROVIERI M. (2008) - Carbon-isotope stratigraphy and
cyclostratigraphy of shallow-marine carbonates. The case
of San Lorenzello, Early Cretaceous of southern Italy.
Cretaceous Research, 29, 803-813.
D’ARGENIO B., FERRERI V., WEISSERT H., AMODIO S.,
BUONOCUNTO F.P. & WISSLER L. (2004) - A
multidisciplinary approach to global correlation and
geochronology. The Cretaceous shallow-water carbonates
of southern Appenines, Italy. In: B. D’Argenio, A.G.
Fischer, I. Premoli Silva, H. Weissert & V. Ferreri (Eds.) -
Cyclostratigraphy: Approaches and case histories. SEPM
Society for Sedimentary Geology, Spec. Publ., 81, 103-122.
D’ARGENIO B., FERRERI V. & AMODIO S. (2008) - Sequence
stratigraphy of Cretaceous carbonate platforms: a
cyclostratigraphic approach. GeoActa, Spec. Publ. 1,157-
171.
FERRERI V., D’ARGENIO B., AMODIO S. & SANDULLI R. (2004)
- Orbital chronostratigraphy of the Valanginian-
483
Hauterivian boundary. A cyclostratigraphic approach. In:
B. D’Argenio, A.G. Fischer, I. Premoli Silva, H. Weissert
& V. Ferreri (Eds.) - Cyclostratigraphy. Approaches and
Case Histories. SEPM Society for Sedimentary Geology,
Spec. Publ., 81, 153-166.
RASPINI A. (2001) - Stacking pattern of cyclic carbonate
platform strata: lower Cretacous of southern Apennines,
Italy. J. Geol. Soc., London, 158, 353-366.
SESSIONE 15

SESSIONE 15
Intrinsic feedbacks and external controls on travertine productivity
Key words: Climate, Control mechanisms, Quaternary,
Travertines.
Large part of Quaternary travertines of central and southern
Italy form calcium carbonate piling that may be considered in
different ways: simply as sedimentary accumulations of
precipitates at springs and/or river-beds (often modifying their
substrate morphology) or as the result of specific climatic
conditions, favouring periodic culminations in size and
variability of their growth forms. In view of the above, two
mechanisms of travertine formation may be discussed: a)
intrinsic depositional trends that cause the carbonate
encrustations to modify their accumulation profiles (increasing
the frontal slope while decreasing the summit outline) and b)
external (climatic and eustatic) control that cluster the peaks of
travertine formation in the interglacial intervals (melting of icecaps,
increasing volumes of calcium carbonate-rich waters in
the karstic reservoirs). Parent water temperature is a key factor
in these deposits: high values bring on elevated carbonate
precipitation rates and a decrease of abudance, size and
diversity of the eukaryotic organisms colonizing the
depositional sites, while the decrease of temperature has an
opposite effect. This allows to distinguish between thermal- and
ambient-water travertines; the transition between these two endmembers
being often gradual.
According the radiometric datation of the studied travertine
bodies there is a close correlation between their formation and :
a) some stages of orbitally driven chronostratigraphy of the
δ 18 O record; b) the atmospheric CO2 content of the time of their
formation (as recorded in the Vostok core) and c) high sea level
phases, in turn ruled by climate.
In fact, the travertine formation appears strictly related to
specific warm-wet climatic intervals characterized by
increasing volumes of the spring waters in the mountain
foothills and by areal forest expansion.
_________________________
(*) Istituto per l’Ambiente Marino Costiero, I.A.M.C. (CNR),
erlisiana.anzalone@iamc.cnr.it
ERLISIANA ANZALONE (°), BRUNO D’ARGENIO (°) & VITTORIA FERRERI (°)
484
The latter enhances supply of CO2 to the soils and leads to
saturation of the karstic waters which, precipitating at (or next
to) springs, build travertine bodies. In conclusion, the following
considerations may be briefly expressed: a) the Quaternary
travertines cropping out in central and southern Italy, regardless
from parent water temperature, developed mostly during
interglacial periods; in particular, they appear strictly related to
specific warm-wet climatic intervals, characterized by
increasing volumes of spring-water in the mountain foothills
and by areal forest expansion, b) the temperature of parent
waters is an important factor controlling life development in
travertine systems.
This allows to distinguish between ambient and thermal
water travertine deposits also on the basis of their textures,
biological composition and biotic (mostly microbic)
precipitates; c) the CaCO3 precipitation processes tend to
modify the original substrate morphology; in particular, the
areal and vertical evolution of the original sedimentary
environments (slopes, shallow-lakes/swamps; rapids/waterfalls)
makes up a terraced travertine body whose upward growth is
punctuated by recurrent discontinuity surfaces (erosional and/or
non depositional).
Finally the authors note that, even if intrinsic and external
control mechanisms normally concur at the formation of large
volumes of travertines, their relative importance is not always
easily recognized, particularly for colder intervals. On the
contrary, during deglaciation times, the external controls tend
to dominate, and thus obscure the intrinsic feed-backs.

The tectonic control on the deposition of Pleistocene continental
carbonates in the Sarteano area (southern Tuscany)
ANDREA BROGI (*), ENRICO CAPEZZUOLI (*), ELENA BURACCHI (*), MARILÌ BRANCA (°) & MARIO VOLTAGGIO (°)
Key words: Neotectonics, Pleistocene, Sarteano, southern
Tuscany, travertine.
INTRODUCTION
In the last years studies on continental carbonates, in terms of
travertines and/or calcareous tufa (FORD &PEDLEY, 1996), have
been intensified not only for sedimentological and stratigraphical
investigation but also for studies on neotectonics,
pelaeosismology, climatic changes and hydrothermal circulation
in geothermal systems. The evolution of the travertinescalcareous
tufa deposits can reveal much about the age, geometry
and kinematics of faults and related minor brittle structures.
Several studies dealing with tectonically driven travertine
deposition have reconstructed the relationships between faulting
and the hydrothermal fluids arising from deeper levels up to the
surface (HANCOCK et alii, 1999).
In this presentation we describe the role of faults and related
fractures for the deposition of Pleistocene travertine and
calcareous tufa in the Sarteano area (Central Italy), located along
a tract of the Monti del Chianti-Monte Cetona ridge.
DISCUSSION
The calcareous body of Sarteano occupies an area of about 10
km 2 , at least. It is characterized by a lobate-shaped structure in
plain view, with a flat surface on the top (520 m a.s.l.), and three,
well-defined, terraces at lower altitude (410 m, 350 m and 310 m
a.s.l.) downward the Astrone valley.
The upper surface is very flat, only gently sloped towards the
valley. It is formed by two bulges of different extension and
separated by a small valley (Fosso della Foce Creek). The widest
is the southern one and it is characterized by the presence of two
elongated, NE-SW oriented mounds, similar in dimensions (about
70 m high and 600 m long) and symmetrically located respect to
_________________________
(*) Dipartimento di Scienze della Terra, Università di Siena,
brogiandrea@unisi.it, capezzuoli@unisi.it, elenb77@alice.it
(°) CNR-IGAG c/o Dipartimento di Scienze della Terra Università di
Roma “La Sapienza”, m.branca@igag.cnr.it, mario.voltaggio@igag.cnr.it
485
the axis of the bulge. On one of these mounds, it is located the
medieval part of the Sarteano village (Fig. 1) while the second (Il
Poggione) appears to be partially dismantled and divided in two
portions.
The Sarteano deposit is formed by carbonate facies laterally
and vertically organized into 3 facies associations: FA1 -
Fig. 1 – Outcrop of carbonate deposits below the Medieval castle of Sarteano.
decimeter-scale beds of subhorizontal, irregularly shaped,
micritic and peloidal lithofacies that form planar to undulose
stromatolitic crusts (Fig. 2) characterized by the local presence of
patchy grass tussocks in life position; FA 2 – decimeter-scale
alternation between beds of lithoclastic sediments and thickening
upward beds of bioconstructed facies formed by well-cemented,
generally vertical, straight pipes of hanging plants with abundant
primary framework voids; FA 3 – Only in the partially dismantled
SESSIONE 15

SESSIONE 15
structure of il Poggione is possible to observe the internal portion
of the mound, that results composed of sharply defined, regularly
laminated, subhorizontal beds consisting of dense, centimetric,
white calcite laminae alternated with thin, millimetric layers of
porous, peloidal aggregates. Calcite laminae are composed of
arborescent crystalline and shrublike vertical structures
alternated with micritic mudstone.
From a morphological point of view, the Sarteano calcareous
deposit resemble to a mature perched-spring system (FORD &
PEDLEY, 1996; PEDLEY et alii, 2003). According to the
classification of FORD &PEDLEY (1996) and PEDLEY et alii
(2003) the FA 1 and FA 2 are respectively characteristic of a
lobe–top terrace environment and step and terrace environment.
The presence of travertine deposit in the internal part of the
mounds (FA3) probably indicates a low-thermal origin of waters
that deposited the Sarteano calcareous body. The low thermal
waters still outflowing at the Sarteano Spa indicate that
hydrothermal circulation is still active, suggesting the occurrence
of a low-enthalpy geothermal system.
Fig. 2 – Example of undulose, centimetric stromatolic crust (FA1).
These waters were able to form a travertine mound (unusual
morphology in calcareous tufa depositional environment; FORD &
PEDLEY, 1996) in correspondence of the spring vent.
U-Th dating has been performed on several samples collected
in the two different mounds at different stratigraphic levels. The
results allow to refer the beginning of the carbonate deposition in
the Sarteano area to the Middle Pleistocene.
The thermal springs which gave rise to the carbonate
deposition were tectonically controlled. They are aligned along
WSW-ENE faults characterized by left-lateral strike-slip or
oblique-slip movements, or along the traces of related minor
structures. Such faults were active during the Pleistocene and
interfered with pre-existing normal faults of regional relevance,
such as the normal fault and associated minor faults, delimiting
the western side of the Valdichiana Basin.
486
REFERENCES
FORD T. D. & PEDLEY H.M. (1996) - A review of tufa and
travertine deposits of the world. Earth Sci. Rev. 41, 117-175.
HANCOCK P.L., CHALMERS R.M.L., ALTUNEL E. & ÇAKIR Z. (1999)
- Travitonics: using travertines in active fault studies. J.
Struct. Geol., 21, 903-916.
PEDLEY M., GONZALÈZ MARTÌN J.A., ORDOÑÈZ DELGADO S. &
GARCIA DEL CURA M.A. (2003) - Sedimentology of
Quaternary perched springline and paludal tufas: criteria for
recognition, with examples from Guadalajara Province,
Spain. Sedimentology 50, 23-44.

Key words: Brachiopods, crura, chemosynthetic-based
environments, Dimerelloidea, functional morphology.
Brachiopods are one of the mayor components of ancient
chemoshynthesys-based environments (CAMPBELL, 2006).
In particular the brachiopod superfamily Dimerelloidea shows
numerous fossils genera associated to cold seeps and
hydrothermal vents (chemosynthesis-based) environments. All of
these genera are characterized by long ensiform crura showing a
larger ratio of length of crura to length of shell than other
rhynchonellid genera.
Animals adapted to cold seeps and hydrothermal vents
(especially polychaetes, mollusks, and crustaceans) are
characterized by adaptation to hypoxia and have a large brachial
surface and abundant oxygen binding proteins in common.
Considering that crura support the lophophore, the
characteristic feeding and respiratory organ of brachiopods, it is
suggested that ensiform crura can represent an adaptation to
oxygen depleted environments typical of cold seeps and
hydrothermal vents. These crura could be associated to a larger
lophophore and/or to the necessity of position closer to the shell
margin of the lophophore. Both features argue for an
improvement of the feeding and respiratory capacities.
Dimerelloids show also other possible adaptations to
chemosynthesis-based environments. One of these could be
represented by their relatively flattened shape (e.g. Peregrinella)
possibly linked to the massive and highly packed communities
setting typical of these environments. More speculative, but not
improbable, are other survival strategies like symbiosis with
bacteria or higher quantity oxygen binding proteins.
These assumptions will be discussed with special focus on
functional morphology and on their evolutionary significance
within this brachiopod taxon.
Finally all these considerations seem support the suggestion
that all Dimerelloidea could represent a monophyletic group
linked to chemosynthetic-based environments (see also
discussion in GISCHELER et alii, 2003).
_________________________
Dimerelloidea (Brachiopoda): a chemosynthetic-based life style
monophyletic group?
(*) School of Geography, Earth and Environmental Sciences (SoGEES).
University of Plymouth, giuseppe.buono@plymouth.ac.uk
The author is supported by FP7-PEOPLE-IEF-2008 Marie Curie Action:
"Intra-European Fellowships for Career Development"
GIUSEPPE BUONO (*)
487
REFERENCES
CAMPBELL K.A. (2006) - Hydrocarbon seep and hydrothermal
vent paleoenvironments and paleontology: past developments
and future research directions. Palaeogeogr. Palaeocl., 232,
362–407.
GISCHLER E., SANDY M.R. & PECKMANN J. (2003) -
Ibergirhynchia contraria (F.A. Roemer, 1850), an early
Carboniferous seep- related rhynchonellide brachiopods
from the Harz Mountains, Germany: a possible successor to
Dzieduszyckia? J. Paleontol. 77, 293–303.
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Key words: Brachiopods, Early Jurassic, palaeobiogeography,
palaeobiology, Toarcian, Tethys.
Thethyan Toarcian brachiopod associations show some
fluctuations in diversity that seem to be linked to relative sea
level changes. These variations are more evident in western
areas. According to GARCIA JORAL &GOY (2000), 6 phases of
transgression/regression cycles associated to faunal variations are
recognizable.
Another important destabilizing factor is represented by the
Early Toarcian mass extinction that basically led to a complete
faunal turnover. The widespread occurrence of the
Nannirhynchia and Koninckella fauna (Phase 1) (see VÖRÖS
2002) and of the disaster species Soaresirhynchia bouchardi
(Phase 2) (see GRAZIANO et alii 2006) can also be related to the
Early Toarcian mass extinction environmental effects.
This environmental deterioration resulted in a decrease of
diversity and homogenization of western Thethys associations.
Consequently, Pliensbachian palaeobiogeographic units are less
well detectable in the Early – Middle p.p. Toarcian. These seem
to occur again within Phase 4 that is characterized by a major
development of endemic genera.
REFERENCES
GARCIA JORAL F&GOY A. (2000) - Stratigraphic distribution of
Toarcian brachiopods from the Iberian Range (Spain) and its
relation to depositional sequences. In: Hall, R. L. & Smith, P.
L. (Eds.) - Advances in Jurassic Research 2000. GeoResearch
Forum, 6, 381-386.
GRAZIANO R., BUONO G. & RUGGIERO E.T. (2006) - Lower
Toarcian (Jurassic) brachiopod-rich carbonate facies of the
Gran Sasso range (central Apennines, Italy). Boll. Soc. Pal.
_________________________
Toarcian (late Early Jurassic) Thethyan Brachiopods:
palaeobiogeography and response to
palaeoenvironmental variations
(*) School of Geography, Earth and Environmental Sciences (SoGEES).
University of Plymouth, giuseppe.buono@plymouth.ac.uk
The author is supported by FP7-PEOPLE-IEF-2008 Marie Curie Action:
"Intra-European Fellowships for Career Development"
GIUSEPPE BUONO (*)
488
It., 45, 61-74.
VÖRÖS A. (2002) - Victims of the Early Toarcian anoxic event:
The radiation and extinction of Jurassic Koninckinidae
(Brachiopoda). Lethaia, 35, 345– 357.

The Pliensbachian Brachiopod fauna of Case Canepine (Monti
Martani, Umbria) in the contest of Liassic carbonate platforms of
Tethys
Key words: Brachiopods, central Apennines, central Italy,
Corniola Fm., Lias, Mediterranean Province,
Palaeobiogeography, Pliensbachian, Tethys.
The Monti Martani anticline is located in central Umbria,
between Terni and Perugia and belongs to the inner belt of the
Umbro-Marchigiano Apennines. It consists of Mesozoic-Tertiary
sediments, that are folded in an asymmetrical anticline (North-
West – South-East oriented), which is partially overthrusted
eastward and cut in the western side by a normal fault.
The Central Apennines record well-known localities yielding
Jurassic brachiopods, of which the Pliensbachian ones are the
most represented (e.g. VÖRÖS, 1994). Of these, the Monti
Martani area has been studied by PRINCIPI (1910).
Here we report the results of a preliminary study on a
brachiopod assemblage sampled in two “localities” about 1 km
apart on Monte Rotondo, near the town of Case Canepine (Castel
del Monte, Acquasparta, Terni, Monti Martani, Umbria, Central
Italy). It is possible that our outcrops are partially coincident with
those described by PRINCIPI (1910) (localized between Case
Canepine and Colle Lungo). However the fauna described by
Principi (1910) is only partially figured and it seems lost (VÖRÖS,
1994).
Brachiopods are preserved mainly as re-crystallized shells
and sometimes show internal geopetal structures. They are
contained in a mainly pink to brownish or whitish 15 and 50 cm
thick re-crystallized micritic limestone with other bioclasts,
especially crinoids. These layers are referable to the Corniola
Fm.
The fauna seems an impoverished version of that described
by Principi (1910), even if possibly this is linked to less
sampling. It is dominated by small smoothed rhynchonellids
(Basioliolidae morpho-type; see also VÖRÖS 2005), with almost
no strongly ribbed rhynchonellids (the exception is given by one
specimen of Tetrarhynchia zitteli, and one tentatively attributed
to Lokutella liasina). Spiriferida are also represented by
_________________________
(*) School of Geography, Earth and Environmental Sciences (SoGEES).
University of Plymouth, giuseppe.buono@plymouth.ac.uk
(**) Laboratorio Ecologico di Geo-Paleontologia, Assisi,
federico.famiani@gmail.com
The first author is supported by FP7-PEOPLE-IEF-2008 Marie Curie
Action: "Intra-European Fellowships for Career Development"
GIUSEPPE BUONO (*) & FEDERICO FAMIANI (**)
489
Liospiriferina obovata, and at least one specimen of
Liospiriferina rostrata.
The combination of lithostratigraphy and biostratigraphy
permit us to refer this fauna to the Domerian (upper
PLIENSBACHIAN) AND TO A PALAEOENVIRONMENT OF SEAMOUNT
SLOPE (E.G.VÖRÖS, 1994).
In a palaeobiogeographic context this mainly smooth-shelled
fauna is clearly representative of the Mediterranean Province,
and in spite of the presence of some species that are more
abundant in other areas (the Carpatho-Sicilian sub-bioprovince),
it can be also ascribed to the Appennino-Transdanubian subbioprovince.
(cf. VÖRÖS 1993)
REFERENCES
PRINCIPI P. (1910) - Brachiopodi del Lias medio di Castel del
Monte (presso Acquasparta). Riv. Ital. Paleontol., 16, 3, 63-
88.
VÖRÖS A. (1993) - Jurassic microplate movements and
brachiopod migrations in the western part of the Tethys.
Palaeogeogr. Palaeocl., 100, 125–145.
VÖRÖS A. (1994) - Umbrian Liassic brachiopods in Hungary:
review and comparison. Paleopelagos special publication, 1.
Proc. of the 3rd Pergola Intern. Symp., 357 - 366.
VÖRÖS A. (2005) - The smooth brachiopods of the
Mediterranean Jurassic: Refugees or invaders? Palaeogeogr.
Palaeocl., 223, 222–242.
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Key words: Brachiopods, Mass extinctions events, Permian-
Triassic (P-Tr) extinction, Statistical analyses, Triassic-
Jurassic (Tr-J) extinction.
During the last 500 Million years brachiopods show several
changes in diversity and distribution. Since the earliest Mesozoic
their distribution increased rapidly and other marine invertebrates
overtook their place as an important member of shallow marine
benthos. This study documents changes in abundance,
distribution, diversity, and composition of brachiopod faunas
during two major events of brachiopod decline, the Permian-
Triassic and the Triassic-Jurassic Extinction event.
The occurrence of each genus through these extinction
intervals is described. A matrix of absence and presence with
environmental settings and latitudinal records of each geographic
area was carried out based on data provided by the Treatise on
Invertebrate Palaeontology (AA.VV., 1997-2007), Palaeobiology
database (AA.VV., 2010), and other references. K-cluster was
used to group localities, NMDS to evaluate faunal relationship
with latitudinal and climatic differences, and variations in
distribution of order for each stage. Climate settings are
interpreted by relative abundance. Finally the general pattern is
tested by affinity analysis (SCHEINER, 1992).
Our results show remarkable differences between these
extinction events: the P/Tr event shows a larger magnitude and a
dramatic reduction of faunas and spatial distribution, whereas the
T/J Event is characterized by a large number of genera with wide
overlapping geographical distribution above the extinction
interval resulting in a reduction in spatial distribution.
_________________________
Testing brachiopod faunal turnovers across the Permian-Triassic
(P-Tr) and Triassic-Jurassic (Tr-J) mass extinctions events
GIUSEPPE BUONO (*), LUIS-FELIPE OPAZO MELLA (*), BRETT METCALFE (**),
MENA SCHEMM GREGORY (°) & RICHARD TWITCHETT (*)
(*) School of Geography, Earth and Environmental Sciences (SoGEES).
University of Plymouth , giuseppe.buono@plymouth.ac.uk
(**) Faculteit der Aard-en Levenswetenschappen, afdeling
Aardwetenschappen, subafdeling Marine Biogeology, Vrije Universiteit,
Amsterdam, Nederland
(°)Senckenberg Forschungsinstitut und Naturmuseum, Paläozoologie III,
Frankfurt am Main, Germany
The first author is supported by FP7-PEOPLE-IEF-2008 Marie Curie
Action: "Intra-European Fellowships for Career Development"
490
REFERENCES
AA.VV. (1997-2007) - Treatise on Invertebrate Paleontology,
Part H (Revised), Brachiopoda, 1-6
AA.VV. (2010) - Paleobiology Database (main contributors of
used dataset: W. Kiessling, M. Clapham, D. Bottjer, T.
Olszewski, M. Aberhan, F. Fursich, A. Mc Gowan, A. Miller)
(http://paleodb.org/cgi-bin/bridge.pl).
SCHEINER S.M. (1992) - Measuring pattern diversity. Ecology,
73, 1860-1867.

Key words: Banded travertine, bedded travertine, neotectonics,
travertine fissure-ridge, western Anatolia.
INTRODUCTION
Banded Travertine is a distinctive lithofacies consisting of
crystalline carbonate laminae vertically grown within a fissureridge
which is a morphotectonic feature developed along the
traces of brittle structures in many thermal systems (Fig. 1).
In particular the Banded Travertine is deposited on the walls
of the fissure during its progressive opening and enlargement, by
upwelling thermal waters that afterwards outflow at the top of the
ridge building upwards and laterally an epigean Travertine
system. In this view the Banded Travertine represents an useful
tool to understand the mechanism of fissure-ridge development as
well as the relationships between tectonic activity and carbonate
sedimentation in a thermal system.
An excellent example of the evolution of a fissure ridge and
associated deposits is exposed in western Anatolia (Turkey) on
the northern shoulder of the Neogene-Quaternary Denizli Basin.
Close to the Pamukkale area, the Çukurbag fissure-ridge (ÖZKUL
et alii, 2005), about 360m long and 10m high (Fig.2), formed as a
consequence of the activity of a minor normal fault development
in the hangingwall of the regional normal fault system.
DISCUSSION
The ridge is flanked by bedded Travertine forming steep
marginal slopes ranging from near-vertical up to 5°. Its profile
resulting from the neotectonic activity, shows a marked
asymmetry mainly in its central part where the northern slope is
about 3 m higher than the southern one. The crest is affected by
_________________________
Migration of banded travertine during the evolution of the
tectonically controlled Çukurbag travertine fissure-ridge
(Pamukkale, Denizli Basin, Turkey)
ENRICO CAPEZZUOLI (*), ANDREA BROGI (*), ANNA GANDIN (*) & MEHMET OZKUL (**)
(*) Dipartimento di Scienze della Terra, Università di Siena
brogiandrea@unisi.it, capezzuoli@unisi.it, gandin@unisi.it
(**) Department of Geological Engineering, University of Pamukkale,
Denizli, Turkey mozkul@pau.edu.tr
491
fractures/fissures which are partially to fully filled by Banded
Travertine. Quarry cuts of Roman times, occurring in the central
portion of the ridge allow to investigate the internal part of the
Çukurbag fissure-ridge which is characterized by several subparallel,
meter-spaced fissures running along its long axis.
Fig. 1 – Vertical Banded Travertine in the Çukurbag fissure ridge (Pamukkale
- Turkey).
Bedded Travertine along the flanks of the ridge consists of
superposed lenticular bodies bounded by angular unconformities
attesting successive depositional events. They are composed of a
variety of lithofacies (fan ray, feather like crystalline crusts,
shrubs, paper thin rafts, bubble) reflecting the irregular shifting in
time of the depositional conditions corresponding to waterfalls,
terraced or fans/smooth slopes, cones, shallow pools, drainage
channels (ÖZKUL et alii, 2002).
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Fig. 2 – Panoramic view of the Çukurbag fissure ridge (Pamukkale - Turkey). Car in the right corner for scale.
The analysis of the relationships between Bedded Travertine
and Banded Travertine suggests that the fissures and related
Banded Travertine were not synchronous and migrated through
time. Fissuring affected progressively the northern half of the
ridge producing its asymmetric growth.
The resulting network of Banded Travertines, coupled with
the sedimentological features of the Bedded Travertine, indicate
that the growth of the Çukurbag fissure-ridge was strictly
influenced by the progressive development, in a substratum
composed of continental, semi-lithified Neogene sediments, of
deformation bands, probably starting with a single band and
ending with a full zone.
REFERENCES
ÖZKUL M., GÖKGÖZ A., YAGIZ S., EKMEKÇI M., ALÇIÇEK M.C.,
ALÇIÇEK H., HORVATICIC N. & AKGÜN M. (2005) –
Travertines of Denizli Basin, western Turkey. Field trip Guide
Book International Travertine Symposium, Denizli, 21-
25/09/2005.
ÖZKUL M., VAROL B. & ALÇIÇEK M.C. (2002) - Depositional
Environments and petrography of Denizli Travertine. B. Min
Res. Expl, 125, 13-29.
492

Paleoclimatic record of the terminal Pleistocene in a stalagmite
from Southern Italy
SIMONA ESPOSITO (*), VINCENZO DI FIORE (*), VITTORIA FERRERI (*) & BRUNO D’ARGENIO (*)
Key words: Image processing, Late Pleistocene–Holocene,
microstratigraphy, solar periodicities, Southern Apennines,
stalagmite.
A microstratigraphic analysis of a stalagmite collected in a
cave of the Monte Avella, Campania Apennines, yielded
interesting paleoclimatic records for a Th/U time interval ranging
from ˜ 20.000 to ˜ 10.000 y BP (lowermost and uppermost dated
stalagmite laminae).
493
Three other Th/U intermediate datations have allowed to
distinguish 4 segments in the studied speleothem, each
caracterized by different rates of accretion and laminae
organization, as well as to identify climatic episodes recorded
also in other coeval speleothems.
Several climatic events of general relevance were recognized,
among which the Younger Dryas and two main meltwater pulses
(Bølling-Allerød and base of Holocene).
Fig. 1 – Correlation among the main intervals (A to F) distinguished in the studied stalagmite and other significant coeval events.
_________________________
(*) Istituto per l’Ambiente Marino Costiero (I.A.M.C. – CNR),
simona.esposito@iamc.cnr.it
The studied stalagmite shows a repetitive pattern of laminae
(0,05 to 1,9 mm in thickness) and groups of laminae (average
thickness of about 1 cm). In order to numerically analyze the
above laminae organization and related thickness changes, image
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processing techniques were performed, using digitalized images
of numerous thin sections. On this basis three main periodicities,
connected with solar activity were recognized, namely ˜ 11, 22
and 100 years.
Even though this study is under development and several
significant analyses are still in progress (among which the
isotopic microstratigraphy) the first results appear of interest and
fill a gap in the areal location and in the timing of stalagmite
studies.
494

Travertine and Calcareous tufa: distinctive fabrics and related
isotopic signatures
Key words: Calcareous tufa, continental carbonates,
flowstones, petrology, stable isotopes, travertine.
Terrestrial limestones are known to form in different subaerial
settings such as karstic cave systems or along fluvial valleys and
near cool water springs or at the emergence of thermal springs.
Flowing carbonate-rich waters derived from groundwaters
mostly of meteoric provenance but with different
circulation/recharge records give rise to carbonate deposits
respectively known as Speleothems, Calcareous tufa and
Travertines .
The calcareous deposits formed in these different setting show
specific lithologic features reflecting the physico-chemical
conditions of the depositing fluids, and although lithofacies and
petrographic features of Speleothems and Calcareous tufa are
already sufficiently known, those of Travertines still need a
definite characterization and classification.
Speleothems forms in dark caves: they are made up of
dominantly abiotic, limpid macrocrystalline calcite;
Calcareous Tufas are deposited along fluvial tracts: they are
commonly biomediated, massive deposits containing remains of
macrophytes and invertebrates;
Travertines grows around thermal springs: they are
represented by associations of dominantly abiotic crystalline
crusts and bacterial laminites, calcified-bubbles and paper-thin
rafts.
The depositional fluvial/palustrine system where Calcareous
Tufas develop is fed by carbonate-rich waters mostly deriving
from karstic springs or in some cases from diluted and cooled,
originally thermal waters.
The carbonate deposits are dominantly microcrystalline
precipitates of calcite of biotic and abiotic origin forming
stromatolitic, phytohermal or phytoclastic facies. They mainly
derives from biologic (photosynthetic) and mechanic
(vaporization/evaporation) removal of CO2 from flowing or
standing waters.
_________________________________________________
(*) Dipartimento di Scienze della Terra, Università di Siena,
gandin@unisi.it
Lavoro eseguito con il contributo finanziario dell’Università di Siena
(PAR 2007)
ANNA GANDIN (*)
495
Their growth results to be controlled by the availability of
meteoric water and thus by climatic conditions.
Travertines are well bedded, often finely laminated compact
limestones, connected with thermal systems. Peculiar crystalline
crusts composed of dense, complex crystals develop in the
proximal part of the thermal complex while in the distal part,
bacterial/cyanobacterial laminites often associated with thin
crystalline crusts, lenses of calcified-bubbles and paper-thin rafts
prevail.
In this system the carbonate deposition mainly derives from
intense degassing of the emerging waters consequent to the rapid
drop in temperature of the waters flowing along the drainage
network.
Their mineral content originates in deep
geothermal/hydrothermal conditions where hot waters charged
with HCO 3- of meteoric and hypogean derivation, are able to
dissolve high quantities of carbonate and/or evaporitic bedrock.
The circulation of hot waters, allowed by open fractures/faults is
ultimately controlled by extensional tectonics.
The critical elaboration and comparison of the petrofacies of
deposits related to the three main genetic groups of terrestrial
carbonates and in particular of the lithofacies of Calcareous Tufa
and Travertines that are still connected with the parent water and
source systems, will provide criteria for their univocal lithologic
identification so that the mainly climate-controlled Calcareous
Tufas and the mainly tectonics-controlled Travertines can be
correctly detected even on the field.
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Different depositional environment in the Lagonegro Basin during
the Norian – Rhaetian time interval (Southern Apennines, Italy).
NICOLA GIORDANO (*), GLORIA CIARAPICA (*), ANGELA BERTINELLI (*) & MANUEL RIGO (**)
Key words: basinal facies, conodonts, Lagonegro Basin, Late
Triassic, radiolarians, Southern Apennines.
The refined biostratigraphy for the Upper Triassic basinal
successions of the Lagonegro area (GIORDANO et alii, 2010)
allows to calibrate the age of the Late Triassic sedimentary events
in the Lagonegro Basin (Southern Apennines, Italy) and to
interpret the sedimentary variations related to the evolution of
Western Tethys in the Late Triassic.
The Lagonegro units consist in pelagic facies from Ladinian
up to Miocene. The Upper Triassic to Upper Jurassic
stratigraphic succession is represented by hemipelagic and
pelagic carbonate and siliceous deposits bearing conodonts,
radiolarians, bivalves, and rare ammonoids (Calcari con Selce
and Scisti Silicei Fms). Four stratigraphic sections belonging to
Lagonegro succession (Mt. St. Enoc, Pignola-Abriola, Mt.
Volturino and Sasso di Castalda) have been studied providing a
new micropaleontological dataset based on conodonts and
radiolarians for the characterization of the Norian/Rhaetian time
interval (GIORDANO et alii, 2010). The studied sections well
represent the different setting of the Lagonegro Basin and are
characterized by excellent stratigraphic continuity and absence of
condensed facies. Particular attention has been focused on the
lithological changes occurred in the transitional interval between
Calcari con Selce and Scisti Silicei Fms that exhibits different
features for the stratigraphic sections.
In Mt. St. Enoc and Pignola-Abriola sections the carbonate
sedimentation continued for most of the Rhaetian, represented by
the upper part of the Calcari con Selce Fm that is characterized
by an alternation of cherty limestones, richness in organic matter,
thin silicified calcarenites with black cherty layers and the Scisti
Silicei Fm (bedded cherts with radiolarians) begins in the upper
Rhaetian, after the appearance of Misikella ultima (BAZZUCCHI et
alii, 2005; GIORDANO et alii, 2010a) (Fig. 1).
The upper part of the Calcari con Selce Fm of the Mt.
_________________________
(*) Dipartimento di Scienze della Terra Università di Perugia,
nikgiordano@hotmail.it
(**) Dipartimento di Geoscienze, Università di Padova
Lavoro eseguito nell’ambito del progetto PRIN 2008 (resp. Ciarapica G.)
496
Volturino and Sasso di Castalda sections is marked by a red shale
interval (4 m thick) and exhibits intermediate characteristics
between the Calcari con Selce and Scisti Silicei Fms, with cherty
limestones, shales and radiolaritic beds (Transitional Interval of
MICONNET, 1982; AMODEO, 1999). The Scisti Silicei Fm begins
at the Upper Norian (Sevatian 2) (GIORDANO et alii, 2010) (Fig.
1).
The comparison between these sections shows how the
transition between the Calcari con Selce and Scisti Silicei Fms
takes place in different ways and at different times within the
Lagonegro Basin. The Transitional Interval between the Calcari
con Selce and Scisti Silicei Fms is present in both Mt. Volturino
and Sasso di Castalda sections. This Transitional Interval
represents the beginning of sedimentary change into the basin
(Upper Norian Sevatian 1, RIGO et alii, 2005; GIORDANO et alii
2010), characterized by an increase of clay interpreted as
evidence of the climate change throughout the Western Tethys at
the end of the Norian (CIARAPICA et alii, 1987; JADOUL et alii,
1992; AMODEO, 1999; BERRA et alii, 2009). The beginning of the
Scisti Silicei Fm seems to be linked to a volcano-tectonic activity
into the Lagonegro Basin produced by an intensification of
oceanic spreading (Ionian Ocean). The CO2 input in the
atmosphere, or directly in the ocean, and the greater availability
of SiO2 could have triggered variations in the sedimentary
process, favoring a bloom of radiolarians and the end of the
deposition of the carbonate in the Basin (according to RACKI &
CORDEY, 2000).
At the same time, carbonate sedimentation is instead present
in the Mt. St. Enoc and Pignola-Abriola sections after the
increase of clay input (red shales level). The Transitional Interval
and the upper part of Calcari con Selce Fm is in fact not present
in the Mt. St. Enoc and Pignola-Abriola sections that are
characterized by richness in organic matter, absence of
radiolaritic layers and carbonate sedimentation up to the end of
Triassic. These differences cannot be fully explained by the
different position of the studied sections respect to the adjacent
carbonate platform that influenced the amount and the origin of
calciruditic/calcarenitic beds.
The Lagonegro Basin was probably an articulate basin, and
the different evolution of the described facies can be due to a
different palaeobathymetry of the Basin. The lower depth of the
Mt. St. Enoc and Pignola-Abriola sections (above the CCD)
probably improves the increase of sedimentation rate, due to the

high primary productivity, and the continuous carbonate
deposition, producing the preservation of carbonate sediments
and organic matter.
The end of the Rhaetian is characterized in both facies by
euxinic conditions linked to the Triassic/Jurassic crisis.
Fig. 1 – Stratigraphic logs of the Mt. St. Enoc and Mt. Volturino sections
(Lagonegro Basin) with conodont and radiolarian biozonation (after
GIORDANO et alii 2010).
497
REFERENCES
AMODEO F. (1999) – Il Triassico terminale - Giurassico del
Bacino Lagonegrese. Studi stratigrafici sugli Scisti Silicei
della Basilicata (Italia meridionale). Mém. de Géol.
Lausanne, 33, 121 pp.
BAZZUCCHI P., BERTINELLI A., CIARAPICA G., MARCUCCI M.,
PASSERI L., RIGO M. & ROGHI G. (2005) – The Late Triassic-
Jurassic stratigraphic succession of Pignola (Lagonegro-
Molise Basin, Southern Apennines, Italy. Boll. Soc. Geol. It,
124, 143-153.
BERRA F., JADOUL F. & ANELLI A. (2009) – Environmental
control on the end of the Dolomia Principale/Hauptdolomit
depositional system in the Central Alps: Coupling sea-level
and climate changes. Palaeogeogr. Palaeoclimatol.
Palaeoecol., doi: 10.1016/j.palaeo.2009.06.037.
CIARAPICA G., CIRILLI S., PASSERI L., TRINCIANTI E. & ZANINETTI
L. (1987) - “Anidridi di Burano” et “Formation du Monte
Cetona” (nouvelle formation), biostratigraphie de deux
series-types du Trias supérieur dans l'Apennin Septentrional.
Rev. de Paléobiol., 6, 341–409.
GIORDANO N., RIGO M., CIARAPICA G. & BERTINELLI A. (2010) –
New biostratigraphic constraints for the Norian/Rhaetian
boundary: data from Lagonegro Basin, Southern Apennines,
Italy. Lethaia, DOI: 10.1111/j.1502-3931.2010.00219.x.
JADOUL F., BERRA F. & FRISIA S. (1992) – Stratigraphy and
paleogeographic evolution of a carbonate platform in an
extensional tectonic regime: the example of the Dolomia
Principale in Lombardy (Italy). Riv. It. Paleont. Strat., 98, 29-
44.
MICONNET P. (1982) – Précisions stratigraphiques et tectoniques
dans un secteur du Lagonegro (Italie méridionale). Ann. Soc.
Geol. Nord, 102, 17-24.
RACKI G. & CORDEY F. (2000) – Radiolarian palaeoecology and
radiolarites: is the present the key to the past? Earth-Sci.
Rev., 52, 83 – 120.
RIGO M., DE ZANCHE V., MIETTO P., PRETO N. & ROGHI G.
(2005) – Biostratigraphy of the Calcari con Selce formation.
Boll. Soc. Geol. It., 124, 293-300.
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Coral Assemblages of Mobarak Formation in the Vali-abad section -
south of Marzan-Abad, North Iran
Key words: Central Alborz, coral, Lower Carboniferous
Mobarak Formation, ramp, Vali-abad.
The Mobarak Formation in the Vali -abad section (south of
Marzan-Abad, central Alborz) consisting of alternation of lime
stones and interbeddeds shale, which is divided into three litho
logical units, attains 200 m in thickness.
It has formed in a shallow carbonate ramp based on the
evidences from micro facieses, corals fauna, litho logical
composition and field data.
According to extant corals' fauna it has been determined that
the Mobarak Formation deposits in this region are included
Tournaisian to upper Visean - ? Namurian in ages. 37 species of
Rugosa corals belong to 17 genera, and 2 species of Tabulata
corals belong to 2 genera have been recorded and assigned to 2
local assemblage zones.
First assemblage belongs to the lithozone B and it has occurred
in the shallow water of platform shelf (oolithic reef), and suggests
a Tournaisian to Middle Visean in age, and whole of existent
corals are solitaire, giant and dissepimented.
Second assemblage belongs to the lithozone C and it is present
in the back reef zone and indicates Upper Visean- ? Namurian in
age. There are dominantly belonging to Cyathaxonia fauna and
some Tabulata.
_________________________
(*) Islamic Azad University, Rud-Hen branch, Civil Department, Rud-Hen
City-Iran, kavehkhaksar@gmail.com
(**) Islamic Azad University, Qom branch, Iran
KAVEH KHASAR(*) & KEYVAN KHASAR (**)
498

Paleoenvironmental evidence from sedimentological and palynologic data of
the late Quaternary cave-fills in the Buca dell’Onice (Massa, Italy)
MARCO MASSINI (*), MARIANNA RICCI (*), MIGUEL BARBIERI (*), LEONARDO PICCINI (*) & ADELE BERTINI (*)
Key words: Cave deposit, palynology, Pleistocene,
sedimentology.
Buca dell’Onice is a small cave located in the Frigido River
Basin (Alpi Apuane, Massa) at an elevation of 570 m asl in the
“Grezzoni” dolostone formation. This cave has a simple access
and allows the study of an exceptionally thick flowstone inside,
thank to the past mining exploitation as a quarry of ornamental
materials (calcareous onyx).
The flowstone is more than 3.1 m thick and it is well exposed
on a vertical cut obtained with helicoidal wire. The speleothem
was formed by a laminar flow of CaCO3-enriched waters fed by
local seepage through metamorphic dolostone. At least two cycles
of deposition, separated by a physical discontinuity, can be
recognized. The lower part, more than 1.7 m thick, is massive and
regularly laminated. The upper part is less regular and displays
several strata and small pockets of carbonate sands. At the top,
the succession is characterized by sharp colour contrasts,
probably related to an important environmental change that
influences and then interrupts the laminar deposition of the
flowstone. A small stalagmite, grew over the flowstone, was
dated at 290 (+85/-55) ka, whereas the top of the flowstone is
older than 350 ka (PICCINI et alii, 2003). In the lower part of the
cave, a 5-6 m thick deposit of carbonate silts and sands buries the
flowstone. This clastic deposit is divided in two deposition cycles
by a calcite crust, dated at 120 (±10) ka (PICCINI et alii, 2003).
The upward transition from mainly chemical to mainly clastic
deposit is probably the result of the reduction of the infiltration
feeding, due to the progressive erosion of the rock volume over
the cave, which was formed as a phreatic, water filled tube at the
base level and then uplifted at 400 m above the present river bed.
This not gradual transition, characterized by the alternation of
calcite and clastic sediments, is probably related to the
superimposition of cyclical climatic changes.
Flowstone and clastic deposits were sampled for pollen
analysis. 12 samples were preliminary collected and about 100 g
for each sample were treated for palynological analyses. The
_________________________
(*) Università di Firenze, marco.massini@poste.it, marianna.ricci@unifi.it,
barbieri.miguel@gmail.com, leonardo.piccini@unifi.it,
adele.bertini@unifi.it
499
three clastic samples were barren in palynomorphs, while pollens,
though with very low concentrations (2.4-20.8 grains/g), was
recovered in the flowstone samples. The palynoflora includes
thirty-seven well-preserved pollen taxa. Arboreal taxa, such as
Pinus, Abies, Fagus, Quercus ilex and deciduous Quercus,
dominate the assemblage whereas herbaceous plants, represented
mainly by Poaceae, are subordinate. Taxa typical of Pliocene and
Early Pleistocene have not been detected. The analysis of
vegetational assemblages, inferred by the pollen record, permits
to point out some climatic changes. The physical discontinuity at
about 1.4 m from top, lies between the beginning of a glacial
phase (increase of Abies related to a decrease of temperature but
still humid conditions) and the start of the interglacial cycle
(increase of Quercus ilex-coccifera attesting an increase of
temperature). Because of the hiatus, pollen record lacks the
glacial acme phase (minimum values of temperature and
humidity) and in fact no expansion of open vegetation has been
observed. Such glacial climate condition probably induced a stop
in the water feeding of the cave and in the flowstone deposition,
or a change from over-saturated to unsaturated waters, as usually
happens when the soil is removed from the epikarst during a cold
stage.
Such preliminary results promote high resolution pollen
analyses, integrated with geochemical and petrographic studies
and new datings, in order to better precise the environmental and
climatic history of this late Quaternary cave.
REFERENCES
PICCINI L., DRYSDALE R. & HEIJNIS H. (2003) - Karst caves
morphology and sediments as indicators of the uplift history
in the Alpi Apuane (Tuscany). Quatern. Int., 101-102, 219-
227.
SESSIONE 15

SESSIONE 15
Key words: benthic foraminifera, Eastern Africa coast, Indian
Ocean, mixed sediments .
INTRODUCTION
The morphology of the Indian Ocean coast of Africa from
Kismayu (southern Somalia) and Lamu (northern Kenya) is
mainly influenced by the drowning of the continental platform
during the Holocene rise of the sea level (Fig. 1).
Various channels, remnants of a previous fluvial system, open
to the sea with estuaries drowned by the Holocene transgression;
the present-day drainage affects a vast inland area of the flat,
partly endorheic, coastal belt; fluvial discharge is low, as in the
Fig. 1 – Study area.
Present-day carbonate-siliciclastic sedimentation and foraminiferal
assemblages along the coast of southern Somalia and northern
Kenya
_________________________
JOHANNES PIGNATTI (*), VIRGILIO FREZZA (*), ANDREA BENEDETTI (*),
FEDERICO CARBONE (**) & RUGGERO MATTEUCCI (*)
(*) Dipartimento di Scienze della Terra, Sapienza - Università di Roma,
johannes.pignatti@uniroma1.it
(**) IGAG-CNR c/o Dip. Scienze Terra, Sapienza - Università di Roma
Lavoro eseguito nell’ambito del progetto “Barriere coralline” con il
contributo finanziario della Sapienza-Università di Roma (Resp. R.
Matteucci)
500
Lamu embayment (northern Kenya), or very low, as along the
Somali coast, where a thin superficial fresh-water body only
reaches the sea during the brief rain periods.
The physiography of the channels and the modern distribution
of the sedimentary facies in the estuaries are strongly related to
the pre-drowning morphology of the fluvial system and to the
present-day high tidal flows.
The channels of Burgao area of southern Somalia are incised
in the Pleistocene bioclastic substrate and are part of the intertidal
zone, mainly covered by a thin muddy layer in their inner more
protected parts and by sandy deposits or small ostreid reefs on
their margins. These intertidal marginal zones are often covered
by mangroves, mainly Rhizophora. The axial part of the channel
estuaries, 5-20 m deep, usually has steep lateral walls. Bottom
sediment is mainly carbonate in the Somali channels and mixed
carbonate-siliciclastic in the Lamu channels. Along the channels,
up to 5-8 km long, the carbonate component decreases rapidly
and sediment becomes siliciclastic, mainly made up of quartz
grains. On the coastal subtidal shelf, especially in southern
Somalia, bioclastic sedimentation prevails. On the platform,
separated from the open sea by a long (>100 km) alignment of
small islands parallel to the coast (Bajuni Archipelago),
flourishing seagrass meadows develop in very shallow waters,
trapping bioclasts produced in the patch and fringing reef areas.
The shelf of the Lamu embayment, facing the very articulated
coast, is much deeper (up to 60 m) and open.
MATERIALS AND METHODS
A total of 23 bottom samples collected between 0.4 and 13.5 m
water depth along the Burgao channel (18 samples) and the
Somali coast (5 samples) and 55 samples collected at depths
ranging from 0.5 to 60 m on the continental shelf of the Lamu
Archipelago (Kenya) were analysed. Wherever possible about
300 specimens of benthic foraminifera were counted and
classified from the >125μm fraction. Q-mode Hierarchical
Cluster Analysis (HCA) was performed using SPSS software
(version 13); only foraminiferal taxa with a relative abundance
≥5% in at least one sample were considered. The α-Fisher index
and the percentage of Dominance were also calculated.

RESULTS AND DISCUSSION
In southern Somalia 130 benthic foraminiferal species
belonging to 61 genera were classified in 20 samples. Three
siliciclastic samples from the inner part of the Burgao channel
from 1-2 m depth were barren in foraminifera. The a-Fisher index
ranges between 3.53 and 17.04, i.e. from very low to relatively
high values.
Q-mode HCA performed on a matrix with the 19 taxa having
a frequency ≥5% has evidenced six assemblages. An assemblage,
dominated by Ammonia convexa (11.2-76.7%), with A. tepida
(3.7-15.2%), A. beccarii (0-10.7%) and miliolids
(Quinqueloculina spp.: 0.3-14.2%; Triloculina spp.: 0-19.1%), is
probably linked to salinity variations. It was found in the
intermediate stream of Burgao (5 samples; 0.4-13.5 m), where
there is a mixed carbonate-siliciclastic sedimentation. A second
assemblage represented by a single sample of the Burgao channel
is characterised by abundant Elphidium craticulatum (38.1%)
together with Challengerella bradyi (13.5%); this sample was
collected at 11 m water depth, on carbonate sediment and
vegetated bottom.
The Discorbina turbo (15.8-42.8%) assemblage includes 4
samples (2-10.5 m) from the Burgao channel, on carbonate
sediments; Neorotalia calcar (4.6-17.3%) and miliolids
(Quinqueloculina spp.: 8.6-16.7%; Triloculina spp.: 5.7-20.5%)
are frequent. In one sample from Burgao channel and two from
Ngumi Island (Bajuni Archipelago) from 1 m water depth an
assemblage dominated by Quinqueloculina spp. (16.6-17.4%)
was found. This assemblage, linked to carbonate sediment in an
intertidal shore environment, is characterised by N. calcar (6.0-
10.6%), Miliolinella spp. (3.6-13.2%) and Triloculina spp. (5.3-
11.5%). A Textularia agglutinans (14.2-45.5%) and
Amphistegina lessonii (12.9-29.9%) assemblage was found in 5
samples (3 from the mouth of Burgao channel and 3 from the
Somalian coast; 0.5-13.5 m) characterised by carbonate
sediments. N. calcar (1.3-24.5%), Quinqueloculina spp. (1.7-
15.9%) and Triloculina spp. (1.3-7.3%) are other main taxa of
this assemblage, linked to marine conditions. Finally, a very
oligotypic assemblage dominated by C. bradyi (74,8%)
characterises one sample in the inner part of Burgao channel (2 m
water depth; carbonate sediment).
On the continental shelf of the Lamu Archipelago (northern
Kenya), 55 bottom samples yielded a total of 205 benthic species
belonging to 100 genera; 3 samples were barren in foraminifera.
Q-mode HCA on 28 species with a relative abundance ≥5% led to
the identification of 7 assemblages.
Along the shelf, the shallowest assemblage (1-9 m) is
dominated by Amphistegina lobifera (>39% in three samples). A
second assemblage, up to 51 m water depth, is represented by
Amphistegina radiata (17-35%), E. craticulatum (4-15%), A.
lobifera (0.3-14%), A. lessonii (1-10%), Heterostegina depressa
(0.3-7%), and Quinqueloculina spp. (3-14%). Finally the
501
assemblage between 16 and 60 m water depth is dominated by A.
radiata (43-62%) with subordinate A. lobifera (1-22%), E.
craticulatum (3-9%), and A. lessonii (1-5%).
The spatial distribution of assemblages is closely associated
with sedimentary environments and water depth.
In the Lamu, Manda and Pate bays (0.5-22 m) the
assemblages are different and reflect seasonal siliciclastic supply.
One sample from Manda Bay is dominated by Ammonia spp.
Mangrove environments show high diversity (a-Fisher index
ranges from 12.5 to 25.4) and lack in abundant species (E.
craticulatum ranges from 1 to 10%; D. turbo from 0.9 to 5.3%
and N. calcar from 0 to 19%). Along the channel mouths two
assemblages are recognised, the first one near the channel
margins, between 2 to 10 m water depth is characterised by N.
calcar (27-34%) and D. turbo (3-28%); the second one at the
centre of a channel is characterised by Neorotalia spp. (31-76%)
and D. turbo (2-12%).
The distribution of several infralittoral symbiont-bearing
species such as A. radiata, H. depressa and Operculina
ammonoides within shallowest assemblages are clearly influenced
by the terrigenous input that increases the turbidity of the water
and by local hydrodynamic conditions.
CONCLUSIONS
The evidence outlined above allows us to draw some
preliminary considerations. The foraminiferal assemblages of the
drowned channels and of the subtidal platform nearby are rather
diverse, in spite of the water energy due to the marine currents on
the sediment bottom. The other recognised assemblages depend
from the normal marine shallow-water parameters, as bathymetry,
water energy and type of substrate. Many of the species are
recognised for the first time in the area or are as yet undescribed.
The low species richness in the samples from the Burgao area
depends on smaller exchange with the open sea in comparison
with the Lamu embayment.
SESSIONE 15

SESSIONE 15
Quantitative analysis of ancient reefs: looking for a correct
approach. A case study from the reef facies of Mt. Bardia formation
(Late Tithonian-Berriasian, Easter Sardinia)
Key words: Ancient reef, Early Tithonian-Berriasian,
quantitative analysis.
Quantitative analyses in reef studies are seen as a useful tool
in order to the better understanding of the distribution of reef
organisms, their potential for the formation of reef structures, and
to facilitate the comparison among different reefs.
Similar techniques are used for the quantitative
characterization of reefs both in modern and ancient settings:
1) plot techniques (belt-quadrant transect method), using
quadrants as sampling units. Plots are distributed
randomless or arranged in belts considering ecological
zonations;
2) plot-less techniques (line transect method, quarter point
method, point-counting method), utilizing line transects
with a defined length.
Quantitative studies on modern reefs point on the definition of
distributional and diversity patterns of the reef organisms and are
largely based on data obtained during diving observations (e.g.
DODGE et alii, 1982). Reef bibliography contains a lot of
references where results, issued by the application of different
techniques, are compared (e.g. DODGE et alii., 1982; CHIAPPONE
&SULLIVAN , 1991).
As for ancient reefs, despite the amount of papers dealing
with quantitative analyses has improved considerably in the last
two decades (e.g. KIESSLING et alii, 2000; 2002), only few
authors applied quantitative techniques to define the
distributional patterns of organisms at the field mapping scale
(e.g. WEIDLICH et alii, 1993; BRAUN et alii, 1994; BOSELLINI,
1994, BERNECKER et alii, 1999). The FLÜGEL &HÖTZL (1976)’s
paper represents the only comparison test between plot and plotless
techniques. These authors conclude that the plot-less
techniques has not disadvantage over quadrant plot
measurements.
Quantitative analyses of ancient reefs are of course outcrop-
_________________________
CRISTIANO RICCI (*), ALESSANDRO LANFRANCHI (**), FAVIO JADOUL (**) & GIOVANNI RUSCIADELLI (*)
(*) Dipartimento di Geotecnologie, Università di Chieti, c.ricci@unich.it;
grusciadelli@unich.it.
(**) Dipartimento di Scienze della Terra “Ardito Desio”, Università di
Milano, alessandro.lanfranchi@unimi.it; flavio.jadoul@unimi.it
502
based, and include a wide range in the observation scales. A
combination of quantitative outcrop-related paleontological and
microfacies data is necessary for the characterization of
multifarious features of reefs (BERNECKER et alii, 1999).
This work focuses on the quantitative analysis of a spectacular
outcrop of a reef system portion belonging to the Mt. Bardia
formation (Late Tithonian-Berriasian, JADOUL et alii, 2007;
JADOUL et alii, 2009). The outcrop is located at Cala Gonone,
Dorgali (East Sardinia, Italy) and consists of a sawed quarry wall,
quite polished surface, that appears as a huge slab, ~48 m 2 in size
(H: ~5,5 m x L: ~9 m), offering a complete and high resolution
2D image of the reef unit (fig. 1). The quarry encompasses a great
variability of biocalcifiers (most of coral colony morphology,
stromatoporoids, echinoderms, bivalves, etc.), different degree of
reworking (from in life-position skeleton more than 1 meter in
size to centimetric rubble), the whole pattern of facies texture
(from packstone to rudstone and from bindstone to framestone),
and a complex system of inter- and intra-skeleton cavities that
allows a detailed study of the reef porosity.
The external surface of each component (biotic and abiotic)
has been emphasized using different colours, achieving a
complete, no lacunose, scanning of this portion of the reef unit.
This time-consuming procedure has been able to quantify the real
frequency, density and area occupied by various reef components.
Therefore, this procedure represents, better than other
quantitative methods, the “image” of the pictured reef portion.
The opportunity to archive a high resolution, no lacunose,
quantitative data analysis of the reef allows the different
quantitative data acquisition techniques (plot and plot-less
technique) to be compared. Moreover, this comparison provides a
confident detection of the minimum number of observations that
concur to the actual definition of the reef structure. This
procedure represents a crucial point in order to perform a
quantitative analysis on usual, uncompleted, weathered outcrops
and to compare results among different outcrop conditions.

Fig. 1 – A: Cala Gonne quarry wall recording the Mt. Bardia formation reef facies (Late Tithonian-Early Cretaceous). B: Detail from A, line-drawing method used
to in this work to collect quantitative data. C: Sketch of B: b/e: undifferentiated bivalves, gastropods, echinoderms; cv: inter- and intra-coral cavity; ploc: massive
plocoid coral colony; ram: branching ramose coral colony; sed: bioclastic sediment; st: undifferentiated stromatoporoids.
REFERENCES
BERNECKER M. , WEIDLICH O. & FLÜGEL E. (1999) - Response of
Triassic Reef Coral Communities to Sea-level Fluctuations,
Storms and Sedimentation: Evidence from a Spectacular
Outcrop (Adnet, Austria). Facies, 40, 229-280.
BOSELLINI F. (1994) - The coral fauna of Vitigliano: Qualitative
and quantitative analysis in a backreef environment (Castro
Limestone, Late Oligocene, Salerno Peninsula, S. Italy). Boll.
Soc. Paleont. ltal., 33, 71-181.
BRAUN R., OETKEN S., KONIGSHOF P., KORNDER L. &
WEHRMANN A. (1994) - Development and biofacies of reefinfluenced
carbonates (Central Lahn Syncline, Rheinisches
Schiefergebirge). Cour. Forsch. Senck., 169, 351-386.
CHIAPPONE M. & SULLIVAN K.M. (1991) - A comparison of line
transect versus linear percentage sampling for evaluating
stony coral (Scleractinia and Milleporina) community
similarity and area coverage on reefs of the central Bahamas.
Coral Reefs, 10, 139-154.
DODGE R. E., LOGAN A. & ANTONIUS A. (1982) – Quantitative
reef assessment studies in Bermuda: A comparison of
methods and preliminary results. B. Mar. Sci., 32 (3), 745-
760.
FLÜGEL E. &HÖTZL H. (1976) - Palökologische und statistische
Untersuchungen in mitteldevonischen Schelf-Kalken
503
(Schwelmer Kalk, Givet; Rheinisches Schiefergebirge). Bayer.
Akad. Wiss., Math.-Naturwiss. Kl., Abh., N. F., 156, 70.
JADOUL F., LANFRANCHI A. & BERRA F. (2009) – Evolution of
Late Jurassic to Berriasian carbonate platforms of Eastern
Sardinia. In: Pascucci V. & Andreucci S (Eds.) - Field Trip
Guide Book, Pre-conference trip FT4, 27th IAS Meeting of
Sedimentology, Alghero, 51-72.
JADOUL F., LANFRANCHI A., CASELLATO C.E., BERRA F. &GALLI
M.T. (2007) – Stratigraphic evolution and paleogeographic
setting of the middle Jurassic-Early Cretaceous carbonate
platforms in Eastern Sardinia (Italy). EGU General assembly
2007 April 15-20. Vienna, Austria (Abstract book).
KIESSLING W., FLUGEL E. & GOLONKA J. (2000) - Fluctuations in
the carbonate production of the Phanerozoic reefs. In:
Insalaco E., Skeleton P.W. & Palmer T.J. (Eds) - Carbonate
Platform Systems: components and interactions. Geological
Society, London, Special publication, 178, 191-215.
KIESSLING W., FLÜGEL E. & GOLONKA J. (2002) - Phanerozoic
Reef Patterns. SEPM Special Publication no. 72, 775 pp.
Tulsa: Society for Sedimentary Geology (SEPM)
WEILDLICH O., BERNECKER M. & FLÜGEL E. (1993) –Combined
quantitative analysis and microfacies studies of ancient reefs:
an integrated approach to Upper Permian and Upper
Triassic reef carbonates (Sultanate of Oman), Facies, 28,
115-144.
SESSIONE 15

SESSIONE 15
Quaternary calcareous tufa and travertine in Tuscany (central
Italy): paleoenvironmental and paleoclimatic reconstructions
MARIANNA RICCI (*), ADELE BERTINI (*), ENRICO CAPEZZUOLI (**), SEVERINE FAUQUETTE (***),
MARIAELENA FEDI (°), NADA HORVATINCIC (°°) & FABIO SANDRELLI (**)
Key words: Palynology, Quaternary, sedimentology, stable
isotopes, terrestrial carbonates.
A Quaternary travertine and calcareous tufa succession in the
Valdelsa Basin (San Gimignano, central Italy) has been
investigated for paleoenvironmental and paleoclimatic
reconstructions. The presence in this area of some still active
thermal systems is a unique chance to observe and study,
nowadays, the same process of past time.
The opportunity to register and combine different tools such
as dating, sedimentology, isotopic and palynological analyses,
makes this terrestrial carbonates an interesting geological archive.
The southern part of the Valdelsa Basin is characterized by
the presence of a carbonate terraced succession developed in a
limited segment of the fluvial pattern. Sedimentological and
petrographic analysis shows that the succession is formed by a
terrigenous fluvial deposition rapidly replaced by calcareous tufa
deposited in a fluviatile-paludal environment. In the apical
portion of the succession, tufa are alternated to travertine of
thermal origin.
This is evident near San Gimignano, where three different
cycles of tufa and travertine have been recognized; moreover,
close to the fossil deposit a low thermal spring is still active. 43
samples have been collected for palynological and isotopic
analyses (d 18 O, d 13 C) along the 16m thick section.
Oxygen isotope values do not show significant changes in a
range between -6 and -4,5‰ PDB. Carbon isotope values show
strong fluctuations (-4/+4‰ PDB), however, most of the samples
have d 13 C values ranging between 1 and 3‰ PDB. Samples
contain pollen grains and lack vegetal macro-remains. More than
70 different taxa have been detected.
Concentrations vary from 8 to 796 grains/g. Arboreal plants
of temperate forest (e.g. deciduous Quercus) dominate the
assemblage, except for phases of herbaceous taxa increase.
Among shrubs and trees of Mediterranean climate, Olea and
Quercus ilex are well represented. A quantitative paleoclimatic
_________________________
(*) Università di Firenze, marianna.ricci@unifi.it, adele.bertini@unifi.it
(**) Università di Siena, capezzuoli@unisi.it, sandrelli@unisi.it
(***) Université de Montpellier, severine.fauquette@univ-montp2.fr
(°) INFN Firenze, fedi@fi.infn.it
(°°) Rudjer Boskovic Institute Zagreb, Nada.Horvatincic@irb.hr
504
recostruction from pollen data is provided by using the Climatic
Amplitude Method which furnishes the values for the mean
annual temperature, mean temperature of the coldest month, mean
temperature of the warmest month and available moisture.
The palynological record testifies that deposition of carbonate
deposit took place during a dominant warm-humid climate phase.
According to previous stratigraphical correlations, this succession
could be related to a warm stage of the Late glacial.
However, a younger age cannot be excluded. 14 C dating of
both terrigenous (4) and tufa (9) samples is in progress to better
define the chronology of the succession.

Key words: Ellipsactinia limestones, Intra-Tethys reef
complexes, reef zonation, Upper Jurassic.
Upper Jurassic Intra-Tethyan reef complexes represent a
peculiar reef type that differentiate from other Tethyan and extra-
Tethyan examples on the basis of their biotic content, debris
amount and strong zonation.
This study documents the zonation of an Upper Jurassic reef
complex developed on the platform margin of an Intra-Tethystype
isolated carbonate platform, presently exposed in the central
Apennines. The reef zonation is revealed by the distribution of
biota and sedimentary features along the reef complex. Biota are
mainly represented by corals and calcified demosponges (mostly
chaetetids and stromatopores), which are present with different
amounts and aggregating structures, according to their position
along the reef complex. Corals and stromatopores are the
outstanding biota within zones in opposite position along the reef
complex, the innermost and outermost, respectively. Corals form
large aggregates (dense and sparse) only in the inner reef zone,
whereas they are present as isolated colonies in the other reef
zones. Conversely, stromatopores form mound-shaped dense
aggregates in the outer reef zone; they are present as isolated
specimens in the other reef zones. Among secondary biota,
microencrustations represent an important component of the
studied reef complex, as they actively participate to the reef
construction process. Microencrustations (microbialites and
microencrusters) are relatively more abundant in the inner reef
zone, where they are generally associated to coral aggregates.
Microencruster frameworks are generally associated both to
isolated corals colonies and coral aggregates.
Similarly to the biota, sedimentary features display a different
distribution along the reef complex. Grain size, sorting and
reworking degree of sediments, cement crusts and cavities
increase from the inner to the outer reef zones, whereas peloids,
micrite and bioerosion follow an opposite distribution pattern.
Favourable stratigraphic conditions and large exposures
_________________________
The Ellipsactinia limestones of the Marsica area (Central
Apennines): a reference zonation model for Upper Jurassic Intra-
Tethys reef complexes
GIOVANNI RUSCIADELLI (*), CRISTIANO RICCI (*) & BERNARD LATHUILIÉRE (**)
(*) Dipartimento di Geotecnologie, Università di Chieti,
grusciadelli@unich.it; c.ricci@unic.it
(**) UMR CNRS 7566, Géologie et Gestion des Ressources Minérales et
Energétiques (G2R), Université de Nancy I, France,
Bernard.Lathuiliere@g2r.uhp-nancy.fr
505
allowed the reconstruction of the original depositional profile at
the top of the Upper Jurassic reef complex. The reconstructed
depositional profile allowed the biota distribution to be
constrained to the reef complex morphology and favoured the
interpretation of bathymetric and hydrodynamic parameters.
The ensuing environmental interpretation of the reef zones of
the central Apennines example is in stark contrast with models
previously proposed for many Upper Jurassic Intra-Tethyan reefs,
and essentially based on modern reefs. The central Apennines
reef complex indicates that modern reefs are, in many respects,
rather inadequate models for Upper Jurassic Intra-Tethyan reef
complexes.
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Rocce e minerali industriali:
prospezione - estrazione - gestione - uso e
conservazione
CONVENERS
Roberto Cabella (Università di Genova)
Mauro Fornaro (Università di Torino)
Marco Lezzerini (Università di Pisa)
507
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The needs for mineral raw materials for the sustainable production
in the international framework
VANNI BADINO (*), GIAN ANDREA BLENGINI (**), MAURO FORNARO (°) & ANDREA GIULIANI (°)
Key words: Mineral raw materials, mining industry,
sustainability, sustainable development.
Mineral raw materials are fundamental resources for the civil
society and play an important role in the process of Sustainable
Development.
Their contribution to the economic and social development is
strategic, but they must be produced and used in an
environmentally sustainable manner.
The application of Sustainable Development principles to
non-renewable natural resources is complex and characterized by
a high degree of uncertainty, as well as absence of internationally
standardized procedures (Fig. 1).
In such a context, the quantitative assessment of sustainability
is particularly controversial.
A step towards a most acceptable measurement of
sustainability is the extension of the concept of eco-compatibility
of the mineral industries to a broader and more comprehensive
approach.
Fig. 1 – The three spheres of sustainability.
_________________________
(*) Politecnico di Torino (DITAG), giovanni.badino@polito.it
(**) Politecnico di Torino (DISPEA), gianandrea.blengini@polito.it
(°) Università di Torino (DST), mauro.fornaro@unito.it, giuliani@unito.it
508
Such an approach should overcome the physical boundaries of
extractive and mineral processing sites, in order to encompass not
only the environmental impacts of mining/quarrying, but also the
environmental implications of mineral-based products, including
their end-of-life.
The sustainability of the extractive industry is a theme that
was particularly debated in recent years. However, it must be
recognized that the expression “sustainability of the mineral
industries” could be perceived as not straightforward, as it might
suggest an ambiguous question: “how a non-renewable resource
can be produced sustainably?” Much more straightforward and
meaningful is debating on how the mineral industries can
positively contribute to the Sustainable Development as a whole.
In recent years, the general interest of the European Union, as
well as the other industrialized countries, towards mineral
resources has boomed, not only in terms of environmental
sustainability, but also in terms of social and economic
development possibilities.
Such an interest in minerals is emphasized by the growing
demand also in the industrialized countries, and not only in the
emerging economies, which gives raise to serious concern in
terms of future availability of strategic resources for the industrial
systems.
Bearing in mind the international context in which most of the
mineral products are traded, the European Commission is
promoting a Thematic Strategy on the sustainable use of natural
resources where some crucial issues are well emphasized: “The
EU is highly dependent on resources coming from outside Europe
and the environmental impact of resource use by the EU and
other major economies is felt globally”, and again “raw materials
extraction in Europe has decreased while imports have increased,
resulting in a shift of environmental pressures to other regions”
(COM 670, 2005).
This said, an overview on demand and supply of non-energy
minerals will be presented, in order to briefly discuss on
international strategies for sustainable supply and use of mineral
raw materials towards objectives of sustainable development.
In particular, the concept of “dynamic resource” will be
discussed. What is currently considered a resource, and that
consequently must be used for the economic and social
development, might cease to be a resource in the future, as it
happened several times in history. Although non-renewable,

mineral raw materials are fundamental in sustainable
development (COM 699, 2008; SEC 2741, 2008).
For instance, oil is “sustainable” if it is used to promote a shift
towards renewable energies. Similarly, metals are “sustainable” if
produced and used to promote the change towards a society based
on recycling and efficient use of natural resources.
REFERENCES
COM 670 (2005) – Thematic Strategy on the sustainable use of
natural resources; Communication from the Commission to
the Council, the European Parliament, the European
Economic and Social Committee and the Committee of the
Regions. 22 pp.
COM 699 (2008) – The raw materials initiative. Meeting our
critical needs for growth and jobs in Europe; Communication
from the Commission to the European Parliament and the
Council. 13 pp.
SEC 2741 (2008) – Commission Staff Working Document;
accompanying the COM 699 (2008) - Communication from
the Commission to the European Parliament and the Council.
18 pp.
509
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Difficult coexistence of extractive planning of dimensional stones in
the quarrying activity and territorial planning in Apulia
Key words: Apulia, dimensional stone, quarrying activity, urban
and territorial planning.
GIUSEPPE BALDASSARRE (*) & NICOLA PALUMBO (**)
Quarrying activity of dimensional stones represents since long
time an important field of the Apulia economy. This favorable
condition, due to the geologic and geomorphological context of
the Apulian territory, if on one side has brought remarkable
economic and social benefits, on the other hand, mostly due to
the insufficient coordination of the laws concerning extractive
planning and the environmental protection of the extractive areas,
has determined impacts negatives on the territory and it's natural
resources.
The short examination which this paper show, concerning
detailed situations in some Apulian quarrying basins, has
exemplified the widespread today existing cases of conflict
between the need of planning and development of the extractive
activities in Apulia and those of protection and safeguard of the
territory and its natural resources. This problematic deserves a
necessary deepening of scientific and legal character.
_________________________
(*) Dipartimento di Geologia e Geofisica, Università di Bari,
gbaldassarre@geo.uniba.it
(**) Autorità di Bacino della Puglia, nicola.palumbo@adb.puglia.it
510

Key words: Ligurian ophiolites, Naturally Occurring Asbestos.
INTRODUCTION
Fibrous minerals of Naturally Occurring Asbestos (NOA) are
present in Ligurian ophiolites both as polymorphs of serpentine
and as amphiboles. The tectono-metamorphic units have different
stages of metamorphic facies, due to the rebalancing of pressure
and temperature conditions. This way, in the same outcrop
different mineral assemblages can coexist, conditioning the
appearance or absence of different fibrous minerals.
Currently, the Italian legislation refers to analytical techniques
that favour a relative simplicity of execution, but can present a
variety of criticises, especially in the presence of natural
materials.
The proposed method, which applies only to natural materials,
through an integrated series of observations, is able to take into
account the different lithological and structural conditions of rock
masses, often crucial in assessing the degree of dangerousness of
the natural material.
METHODS
Among the activities held in ARPAL, there’s the control of
asbestos in a state of natural outcrop and mining sites. The type
of checks will vary depending on the circumstances; in general,
however, it will present two typical situations:
a) complete study of the site;
b) control of the quarry site, aimed to the verification of legal
requirements.
The determination of asbestos in a rock is the result of a
complex procedure, which includes both on-site activities and in
laboratory. ARPAL chose the multidisciplinary approach that will
be described.
The first phase consists in the collection of existing
documentation (e.g. the description of the geomorphological,
geological and hydrogeological detailed mapping of outcrops,
_________________________
Asbestos control in Ligurian ophiolites
GIANLUCA BECCARIS (*),EMANUELE SCOTTI (*), FRANCESCO DI CEGLIA (*) & SONJA PRANDI (*)
(*)Agenzia Regionale per la Protezione dell'Ambiente Ligure ARPAL,
scotti.emanuele65@gmail.com
511
geological sections, etc..) and, in the case of a quarry site, as set
out in Annex A paragraph 4 of the DM 14/05/1996.
The structural-geological survey is the key stage through
which the rock mass is classified at the level of tectonic units,
characterized in lithological and structural terms, as well as being
the essential reference for sampling operations (Fig. 1). The
investigation includes the identification of the rock outcropping
in natural conditions and/or exposed on the quarry face, the
description of lithotype in genetic terms, the mineralogical
composition and analysis of the general geological structure, with
particular attention to layout and to the characteristics of
discontinuity. In this regard, it is expected to fill out a form,
derived from the UNI EN ISO 14689-1, for each station for
geostructural analysis, which generally includes the sampling of
rock under consideration.
Fig. 1 Quarry of ‘Rosso Levanto’ (eastern Liguria)
Macroscopic and microscopic study of samples from the
extraction surface or outcrop in natural conditions occurs in the
laboratory using a specific form. The examination is performed
with the aid of a stereomicroscope in order to identify more
precisely crystalline aggregates which may be elongated on the
surface of fractures of the sample. The recognition of any fibres
on the surface of the sample, or debris that may spontaneously
released from the sample, is an important indication of the
tendency of the rock to the release of fibres.
The qualitative and quantitative determination of asbestos
content (“qualitative and quantitative controls", as defined by the
DCR 105/96) is normally conducted by ARPAL through
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Fig. 2 – Microphotograph of a fiber of asbestos obtained wit a Scansion Electron Microscope (SEM).
chemical-mineralogical analysis (e.g. SEM, Fig. 2), according to
the procedures and methods adopted by the “Laboratorio di
Genova – Settore Analisi strumentale”.
Finally, the results of the analyses among diversified
lithologies are presented, in a frame of control of the quarries,
monitoring of excavations for buildings purposes, mining, and
environmental rehabilitation.
512

Preliminary results for the characterization of the radiological levels
of rocks in Tuscany Region
Key words: Airborne measures, gamma-ray spectrometry,
isotopic abundance, MCA_Rad system, natural radioactivity,
potential natural radioactivity content map, ZaNaI system.
INTRODUCTION
The environmental background levels of natural radiation due
to the nuclides in rocks vary in significant amounts that depend
on the geological and geomorphological features of a territory.
The main source of terrestrial gamma-ray radiation exposure to
humans is from 238 U, 232 Th decay chains and 40 K decay.
This paper reports a part of the results of the Research Project
“Measurement of natural radioactivity and mapping of the
radioisotope abundances of Tuscany Region”, which started at
August 2008 and it is supported by founds of Tuscany Region.
The aim of this project is to realize the thematic maps of
radioactivity content and in particular of the abundances of 40 K,
eU and eTh (these concentrations by weight are determined
indirectly from 238 U and 232 Th daughter products, 214 Bi and 208 Tl
respectively, that are assumed to be in equilibrium with their
parent isotope). These goals will be achieved by integrating the
information from measurements on samples in laboratory with insitu
investigations and airborne surveys. The Legnaro National
Laboratory (LNL) is the national leader for the design and
realization of high-resolution gamma-ray spectrometers, portable
and massive NaI(Tl) detectors.
The MCA_Rad gamma-ray spectrometry system (BEZZON et
alii, 2009) was designed and built up at LNL for measuring large
amount of samples with a minimum attendance: these features fit
_________________________
GIANPIETRO BEZZON (*), GIANPAOLO BUSO (*), IVAN CALLEGARI (**), TOMMASO COLONNA (**),
ENRICO GUASTALDI (**), FABIO MANTOVANI (°) (°°), SARA MARIANI (*) (°°), GIOVANNI MASSA (**),
CARLOS ROSSI ALVAREZ (§), MANJOLA SHYTI (°) (°°) & GERTI XHIXHA (°) (°°)
(*) INFN, Legnaro National Laboratories, Legnaro (PD),
gianpietro.bezzon@lnl.infn.it
(**) Center for GeoTechnologies, San Giovanni Valdarno (AR),
mariani12@unisi.it
(°) Physics Department, University of Ferrara, mantovani@fe.infn.it
(°°) INFN, Ferrara Section, Ferrara, mantovani@fe.infn.it
(§) INFN, Padova Section, Padova, carlos.rossialvarez@pd.infn.it
513
perfectly with the requirements of this project. This system is able
to measure any type of materials (solid, liquid, gas), and due to
the high efficiency and its geometric symmetry, absolute activity
measurements are possible with systematic errors below 5%.
MATERIALS AND METHODS
The Tuscany Region occupies an area of about
23 10 3 km 2 and it includes 15 paleogeographic domains (Fig. 1).
The sedimentary rocks constitute the main reservoir covering the
large part of the Region, the igneous rocks are mainly present in
the south part, while in the north-west part of the Region (i.e.
Apuane succession) we meet metamorphic rocks: in this region
are located the main marble caves of Italy.
The sampling strategy was planed on geological arguments:
the homogeneous units are recognized by low density of samples,
permitting to focus an high density of samples on the
heterogeneous areas. Excluding the quaternary deposits when one
sample per 25 km 2 was collected.
The information collected during the sampling was organized
in a geo-database (GeoDB). The two operators working on field
fill the GeoDB with GPS coordinates and the main information
about the state of outcropping, the weather conditions and the
geological features (unit, formation, lithology).
The 491 samples collected were crushed, sieved and then
placed in a drying oven at temperature 60°C in order to remove
the moisture. The 200cc cylindrical polycarbonate containers
filled with the ground rock were weighted and labeled with a
barcode. Finally they were stored and kept sealed for 38 days in
order to reach the radioactive secular equilibrium between 226 Ra
and 222 Rn (10 half- lives of 222 Rn).
The MCA_Rad output (counts, specific activity and
abundance) it is adapted in order to easily fill the GeoDB
permitting an user-friendly management of the data. This
procedure is designed to minimized the human errors and
optimize the manpower.
The specific activity of 238 U and 232 Th was calculated under
the assumption of secular equilibrium, using the gamma
transitions of energy, 609.3 keV for 214 Bi (eU) and 583.2 keV for
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208 Tl (eTh), while for 40 K was calculated through the gamma
transition of energy 1460.8 keV. The achieved minimum
detection activity (MDA) calculated following CURIE (1968)
were 0.2 Bq/kg for 214 Bi, 0.3 Bq/kg for 208 Tl and 1.8 Bq/kg for
40 K. A preliminary screening for 3600 s of spectrum acquisition
reported only 10% of samples below the MDA value, which were
further measured for 14400 s.
Fig. 1 – The paleographic domains of Tuscany Region and the sampling sites.
RESULTS AND CONCLUSIONS
In the current report it was successfully achieved the
measurement of 491 sample of rocks by using the MCA_Rad
system. The Falterona-Cervarola unit (FCU) and the Macigno
formation (MF) revealed an homogeneous radioactive content,
767 ± 187 Bq/kg and 830 ± 182 Bq/kg respectively. Covering
about 20% of the territory, mainly in the north and east part of the
region, FCU and MF are characterized by sandstone flysch: the
homogeneous content of radioisotope is supported by the
presence of an homogeneous lithology.
In Tuscany Region we find the main types of rocks
characterizing the Earth’s crust: sedimentary, igneous and
metamorphic rocks. Concerning the sedimentary rock, the
carbonate rocks (lime, dolomite, travertine) are characterized by a
radioactivity content lower than the clastic rocks (clay, sandstone,
514
sand): 125 ± 134 Bq/kg and 725 ± 240 Bq/kg respectively. In
some neogenic deposits (marine and evaporitic) we find an
alternation of sandstone, conglomerate, limestone, marl,
mudstone, clay and silty-marly clay: the large spread of specific
radioactivity values (317 ± 230 Bq/kg) reveals this alternation.
The igneous rocks coming from Tuscan Magmatic Province
show elevated levels of radioactivity (1738 ± 886 Bq/kg). In
more details the acid igneous rocks (volcanic ash, tuff, lapillus)
and basic igneous rocks (basalts) are characterized by two
opposite levels of radioactivity: 2015 ± 611 Bq/kg and 80 ± 85
Bq/kg respectively.
The metamorphic rocks are the result of alteration of existing
rocks by either excessive heat and pressure, or through the
chemical action of fluids. Although in general this alteration can
cause chemical changes and/or structural modification to the
minerals making up the rock, the radioactivity content in the
samples of the metamorphic rocks can be related to those of the
lithology of origin. On the other hand the perturbation from
metamorphic processes increase the spread of the radioactivity
values. In Table 1 we summarize the 40 K, eqU and eqTh
abundances organized in the classes of rocks described above.
This classification is a key of the interpretation of the natural
radioactivity content of the region.
Lithology N.
40 K
(%)
The environmental and geological information collected in the
GeoDB will permit to refine this framework and to build thematic
maps by using geostatistical methods. Finally the GeoDB will be
updated to the server database (MySQL) and then will be
published on line by using Web-GIS service based on Google
Earth ® platform.
REFERENCES
eU
(ppm)
eTh
(ppm)
Sedimentary Rocks
Clastic 198 2.1 ± 0.7 2.6 ± 1.1 10.6 ± 4.6
Carbonatic 80 0.3 ± 0.4 1.3 ± 1.4 2.0 ± 1.9
Lime-Clay
Igneous Rocks
49 0.9 ± 0.7 1.5 ± 0.9 4.6 ± 3.2
Basic 9 0.2 ± 0.2 0.9 ± 1.6 3.0 ± 7.2
Acid
Metamorphic Rocks
54 5.3 ± 1.6 11.3 ± 5.8 56.6 ± 26.3
MetaClastic 63 2.5 ± 1.1 2.5 ± 1.1 11.5 ± 4.4
MetaCarbonatic 34 0.5 ± 0.6 0.8 ± 0.8 2.4 ± 3.2
MetaMagmatic 4 3.3 ± 1.7 2.6 ± 1.3 14.3 ± 8.3
Tab. 1 – Average of the 40 K, eU and eTh abundance for different lithologies.
The standard deviation is calculated on N samples.
BEZZON G.P., BUSO G.P & ROSSI ALVAREZ C. (2009) A fully
automatic system for general-purpose radioactive analysis.
LNL Annual Report.

Mutlidisciplinary procedure for estimating the amount of asbestos in
the environment and natural hazard assessment by fiber release;
case study in the south of the Arno river, Tuscany
FILIPPO BONCIANI (*), IVAN CALLEGARI (*), LUIGI CARMIGNANI (*), ALICE FARINELLI (*), LUCA GRAZZINI (*),
ENRICO GUASTALDI (*), MARCO IANNINI (*), ASSUNTA SFALANGA (*) & CECILIA VITI (**)
Key words: Asbestos, Index Release, serpentinites.
INTRODUCTION
The topics related to the presence of asbestiform minerals in
nature in rocks excavated have become of particular social
sensitivity and the many confirmations of the risks to human
health from exposure and inhalation of fibers, had led the
promulgation of environmental regulations governing the
management of earth and rocks excavated potentially
contaminated by asbestiform minerals, their disposal and reuse.
The present study aims to estimate the amount of asbestos in
serpentinitic rocks and the characterization of these in terms of
hazard. In this respect it has been developing a specific regional
survey methodology, type tested in an area in the southern part of
Florence (ophiolitic area of Impruneta) which led to estimate the
percentage of the total volume of rock asbestos material with the
determination of the Index Release (IR) and the classification of
the material in terms of hazard of asbestos minerals, according to
the parameters set by law.
SURVEY METHODOLOGY
To achieve the above objectives, we had to split the search in
different and consequently phases, this in order to address various
issues related to territory, geological and geomorphological
conditions, then to operate at different levels of analytical
resolution necessary for mineralogical characterization of the
rock and the quantization of fibrous minerals.
The disciplinary procedure consists of five main phases:
1) Geological and geomorphologica survey (Fig.1);
2) Quality sampling and laboratory analysis (analysis in
optical microscopy and SEM analysis);
3) Geomechanical analysis of the rock with stereonet
_________________________
(*) Centro di Geotecnologie dell’Università degli Studi di Siena,
bonciani@unisi.it
(**) Dipartimento di Scienze della Terra – Università degli Studi di Siena
515
implementation (Fig.2);
4) Geostatistical analysis to determine the amount of
asbestos in the rock (Fig.3);
5) Sampling and determination of I.R. in the rock mass
(Fig.4).
Fig. 1 – Field work into the outcrop.
Fig. 2 – Stereonet representative of the rock fractures.
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CONCLUSION
During this work we developed a multidisciplinary procedure
between the detection integrated from geological-structural
survey, geomechanical detection, analysis and geostatistics
determination of (IR) as a basis for future in environmental
applications. Requirement resulted from the complexity of
interpretation of law on earth and rocks excavated with
potentially contain of natural asbestiform fibers The methodology
aims to be a first input to the necessary and desirable
standardization and technical-normative study to compare
analytical results from different experiences.
Fig. 4 – Determination of I.R. boundary.
516
Fig. 3 – Geostatistical analysis of fractures fibrous filling.

Key words: Concrete, gypsum, limes, national production.
INTRODUCTION
The importance of the industrial minerals in domestic
quarrying activity depends on the great number of products and
various technological properties related both to mineralogical and
chemical features of the raw materials, geological characteristics
and location of the ore bodies.
The industrial minerals category includes many quarry
materials, each of them has various applications, for example in
the pottery and glass manufacturing, paper and plastic industry,
agro-zootechnical uses, paints industry, building products (as for
example lime, concrete, coverings, gypsum plaster and mortar).
In some case, natural raw materials should be replaced by
synthetics products or mixing of other materials.
In particular, this paper focus on limestone, dolostone and
gypsum due to the variety of their applications and the wide trade
of the their products, particularly for the buildings ones.
LIMESTONE AND DOLOSTONE
Limestone is considered pure when calcium carbonate content
is higher than 95%; commonly, natural limestone includes
various amount of dolomite, clay, silica, organic material, oxides,
hydroxides, fluorides.
According to the uses, raw materials have to respect fixed
composition and some mineralogical components must be present
in limited percentages.
Limestone plays a leading role in the economical market of
the industrial minerals, as demonstrated by statistics based on the
production and consumption data which will be furnished in this
paper. Even if the most common use of the limestone (but not the
most important) is represented by buildings products, as for
_________________________
Raw materials for lime, concrete and gypsum production in Italy
(*) Università degli Studi di Torino, sabrina.bonetto@unito.it
(**) CAGEMA, rricci@cagema.it
(°) AITEC, isacerdote@aitecweb.com
SABRINA BONETTO (*), RICCARDO RICCI (**) & IRENE SACERDOTE (°)
517
example lime and concrete, many other industrial sectors require
limestone use.
This work focus particularly on lime and concrete production
and trade, due to the large distribution of this products.
Limes are commonly distinguished in “aerial” and
“hydraulic”. Hydraulic lime is obtained with limestone that
contains more than 6% of clay and it represented the main
building component since the Roman period up to the past
century, when it was replaced by the modern concrete. Nowadays
it get in most of the plasters production, slaked lime and
refractory materials mixed with other components in variable
ratios (BADINO et alii, 1990).
Aerial lime results from the crushing, riddling and
calcinations over 900°C of the raw material (quick lime); it is
mainly employed in iron and steel industry as a scorifier reactant
in the steel and cast iron production and in iron minerals
agglomeration.
In the chemical industry, lime plays an important role in
catalysis and neutralization processes and in pH regulation; lime
is also used for environmental applications as industrial ash
treatment (for example in case of thermal plants and incinerators),
drinkable and industrial water treatment, organic and inorganic
slurries treatment, food and agricultural industry, pharmaceutical
industry, refining of sugar, paper and glass manufacturing and
clay stabilizer in civil engineering) (BADINO et alii, 1989).
Natural raw materials for concrete production are principally
represented by limestone, marls, clays and schists: they must
contain calcium carbonate and oxide of iron, aluminium and
silicon in fixed ratios. Some marls contain naturally all this
elements in right proportions; they are called “concrete marls” if
the hydraulic index is 0.3 – 0.7. Otherwise, concrete is obtained
by mixing different raw materials and, in particular, limestone
and clay or limestone and marly clay or calcareous marls and
clay/schists or limestone and schists (SACERDOTE, 2001).
Other elements are used as additives in the raw mixture, as for
example quartzitic sands, crashed quartzite and marble, ashes,
iron minerals, bauxites.
Quality requests of limestone for concrete production are
particularly restrictive, so that suitable calcareous ore bodies are
no so common. The presence of alkali, free silica, magnesium
oxides and sulfates should determine problems for hardening
process, unexpected swelling or chemical reaction whit other
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component, so they have to be avoid.
Mineralogical features requested for the clay components are
less restrictive, but magnesium, alkali and sulfates content has to
be very small as well as for limestone (FORNARO et alii, 2002).
GYPSUM
In the last few years the gypsum quarrying activity has been
even developed due to the high request of gypsum for different
industrial sectors.
According to the uses, burnt or raw gypsum has been used for
many applications since to the Egyptian period. For thousands of
years it has been employed as building material, dimensional
stone, decoration plaster and base for polychrome paintings. The
improvement of the processing techniques and equipments has
recently determined a large use of gypsum in many products with
particularly regard to building manufactures (as for example
plasterboard, high quality plaster, concrete additive) with
different technological features requested for each applications.
In the last few decades, it has been commonly employed for
other applications as for example in the fertilizers production, in
plastic and paint industry, in pharmaceutical chemistry and for
medical and artistic uses.
Usually, primary quarried gypsum has an evaporitc origin and
its mineralogical and technological properties depend on
conditions and age of deposition, geological and structural
evolution.
Most of the natural ore bodies have a good gypsum quality
and medium-high degree of pureness in respect to the
technological requirements: usually a few points of percentages
of calcium carbonate have accepted, as well as small quantity of
clay minerals and organic material. The presence of marls, in
limited amount, should improve the workability of the raw
material; chlorates, magnesium, sodium or potassium salts should
be cause of wall efflorescence and problems in hardening. Iron
oxides and hydroxides must be avoid principally in case of at
sight plasters and valuable product for sanitary or artistic uses
(BONETTO, 2006).
In some cases, natural gypsum should be replaced by
synthetic gypsum obtained by chemical processes as ashes
desulphurization of power and thermal plants or oil treatment in
refinery.
With respect to the economical importance of the industrial
minerals quarrying activity and to the influence of their
production on the national and international trade, this paper will
propose to furnish a trend of both domestic production of raw
material and the common products obtained (BADINO et alii,
1989).
518
REFERENCES
BADINO V., FORNARO M., MANCINI R. & MANCINI A. (1989) -
Italian quicklime. Trends of the sector, with a particular
attention paid to the extractive aspects. Atti XIV World
Mineral. Conf. WMC, Beijing, 143-147.
BADINO V., FORNARO M., MANCINI R. & MANCINI A. (1990) -
L’industria italiana della calce: situazione e prospettive con
particolare riferimento agli aspetti estrattivi. GEAM, Torino,
dicembre 1990, 725 -731.
BONETTO S. (2006) - Il gesso: da risorsa economica a
patrimonio culturale del Monferrato. Aggiornamento tecnico,
metodologie operative e ipotesi di riuso dei siti di cava
dismessi. Tesi di dottorato, Politecnico di Torino, inedita.
FORNARO M., LOVERA E. & SACERDOTE I. (2002) - La
coltivazione delle cave ed il recupero ambientale. Politeko,
Torino, 259 pp.
SACERDOTE I. (2001) - La produzione della materia prima
calcarea per l’industria del cemento: sviluppo tecnologico e
metodi estrattivi. Tesi di dottorato, Politecnico di Torino,
inedita.

Technological innovations and secondary raw materials obtained
from a virtuous management of wastes connected to mining
activities: the examples of Gruppo Minerali Maffei S.p.A
Key words: Ceramic industries, dressing plants, feldspar and
quartz, glasses wastes treatment, granite, quarry wastes
valorization, secondary raw material.
INTRODUCTION
The industry connected to mining activity is one of the most
important for Italian economy, both for the raw materials
production and for the new technologies connected to
exploitation and dressing plants. It is linked not only to mines as
such but also, in few cases, to ancient quarry dumps valorisation.
The volumes of quarry wastes are a clear example of the
problems connected to mining activities: the exploitation works
can cause an evident hazard for the population, as well as an
important environmental and landscape impacts for touristic
areas.
For those reasons a systematic reuse of the rock wastes, as
secondary raw materials, should be essential: it is important to
guarantee a sufficient quantity of wastes/resources to justify the
construction of a new treatment plant, the constancy of the
wastes/resources supply and the convenience of the transport
system.
Mining activities and wastes management is also complicated
by “quarry wastes” Italian regulation (artt. 183 and 186 D.Lgs.
152/06, D.Lgs. 117/08 e L. 13/09): to guarantee a correct
management of exploited materials we have to distinguish
“wastes” from “by products”, “associated products”, “secondary
raw materials”. The new Italian regulations, which are complex
and, sometimes, conflicting, do not help people involved in
“wastes management”, such as Public Administrations, mines and
dressing plants owners, etc… (BOZZOLA et alii., 2008).
_________________________
GIORGIO BOZZOLA (*), GIOVANNA ANTONELLA DINO (**), MAURO FORNARO (**) & ALESSIO LORENZI (*)
(*) Gruppo Minerali Maffei S.p.A., gbozzola@g-m-m.it, alorenzi@g-m-m.it
(**) Università di Torino (DST), giovanna.dino@unito.it,
mauro.fornaro@unito.it
519
GRANITE WASTES VALORIZATION: ECOMIN
SAMPLES
An interesting example, connected to quarry wastes
valorisation as secondary raw materials, is the one of Montorfano
and Baveno coarse granites heaps (Lake District, VCO mine
basin – NW Piedmont; Fig. 1). The primary granites pertain to a
series of plutonic bodies, characterized by medium - medium fine
grain. This excavation technique produced, during the past, a
huge amount of wastes, stocked on the lower hill side of the
massifs (Montorfano and Baveno), shaping different “waste”
dumps (“ravaneti”).
Fig. 1 – Southern side of Montorfano Massif.
In 1995 a primary Italian company (Gruppo Minerali Maffei
Spa) decided to invest in granite quarry wastes valorisation as
secondary raw material. The technical principle and the project
planning for such a recovery is based on physical-chemical
characteristics of the rock and on the quantity of wastes to be
treated and valorised: these parameters influence heavily the
dressing plant project (BOZZOLA et alii, 1995).
The new exploitation of the dumped materials is useful for the
production, by specific mineral dressing treatment, of secondary
raw material for industry (mainly for the production of GP – Grès
Porcelain stoneware). The raw materials for the GP stoneware
included, according to the rule, pure quartz and feldspar; for this
reason the price of the final product was very high. Secondary
SESSIONE 16

SESSIONE 16
raw materials, coming from Montorfano and Baveno granites
wastes, are composed by 33% quartz and 62% feldspar: this is
quite similar to the desired mixture for GP.
Nowadays, this is an interesting economic reality with a
subsequent save in the raw material costs. The domestic market
of feldspars, as industrial minerals, is increasing year after year in
Italy: from 200,000 t in 1975 to 2.5 Mt in the following twenty
years; moreover, imported natural resources (about 2,0 Mt) have
to be added to these amounts. It has to be noticed that in 2009
there was an important decrease in feldspar production and
utilization (- 30%), caused by the global economic crisis.
The dressing plant (Ecomin S.p.A. in Verbania, now formed
into the Gruppo Minerali Industriali), described in this paper, is
active since 1995; it has got the concession to exploit three
granite quarry wastes dumps: Sengio and Ciana Tane-Pilastretto
areas, for white granite recovering in Montorfano massif, and
Braghini area, for the pink granite exploitation in Mt. Camoscio.
In order to guarantee the highest safety in the superposed
yards and the stability of the quarry fronts, the material layer is
exploited from the top to the base of the whole volume: the
quarried material is then loaded in dumper and transported to the
dressing plant. The total recovery of the granite wastes exposes
the underlying bedrock, to the purpose of minimize the
conclusive hydro-geologic hazard of the areas. The ore, conveyed
from the quarry wastes areas to the plant, is successfully treated
by crushers, roller mills, etc… in order to reduce each grain size
class and to obtain 1.25 mm as maximal grain size dimension.
Subsequently it is selected, by means of sieves, to obtain different
grain size materials and to separate the raw powder granite from
the other products. Finally this material passes through
electromagnetic separators to select ferromagnetic minerals from
the final product, in order to obtain an excellent product,
characterized by the correct physical-chemical properties (Tab.1).
The wastes produced during the enrichment phase (powder
Table 1 – Chemical composition of the products and by-products coming
from Ecomin plant.
granite, ferromagnetic minerals, filler powder < 100μm) are also
treated to obtain by-products which are used in other
applications. In particular, the main product, output from the
plant, is a mixture of quartz and feldspar, commercially known as
F60P (quartz feldspar mixture: 60% of feldspar, mostly K-
520
feldspar). The production of F60P is about 140,000 t/year. To
that, different by-products, commercially known as: SNS - sand
(as pre-mix for building uses), NGA - coarse black sand (used for
industrial sandblast), SF - wet feldspar (for ceramic industry) and
SF100 and SF200 (used as filler in cement industries) have to be
added. The total amount of the by-products is about 70,000
t/year.
CONCLUSIONS
The importance of such a treatment is that, at first, it is
possible to valorise quarry wastes as secondary raw material, but,
secondary, it is possible to achieve the goal of a zero waste
volume production, with a consequential cost decrease for quarry
enterprises and indisputable environmental advantages for the
territory. It is important to underline that it is possible to ensure
sustainable development for mining activities, guaranteeing, at
the same time, the profit for the virtuous companies involved in
the exploitation, valorisation and recovery of the “new ore-body”.
The granite quarry wastes represent, therefore, an important
alternative (integrating) source, vicarious to the exploitation of
“virgin” material from the primary mines of quartz and feldspar.
As already mentioned, the exploitation of the quarry wastes
ensures often a correct environment recovery and the safety of
slopes affected by the dumps.
Furthermore, the hard recovery of the glass scraps is another
important technical development and that it’s applicable not only
in the potting but also for the sanitary fittings production, with the
aim to subrogate natural melting agents (as feldspar or
nepheline). Mineralurgical methods are useful applied to handle
200,000 t/year of glass scraps; last but not least, this recovery
process allows to reduce the consumption of soda and
consequently the un-ecological production of CO2. At present,
last topic is on a preliminary stage, but with a certain interesting
development. Among many industrial innovative activities, it
must be recalled the recovering of the abrasive garnet-sand
(coming from India), that it is picked up after the washing of
residual tailings. The treatment method is mainly gravimetric by
means of a vibratory sieve, combined with air classification and
magnetic separation in order to obtain a still an useful grain size.
REFERENCES
BOZZOLA G., GARRONE L., RAMON L. & SAVOCA D. (1995) – Un
esempio concreto di riutilizzo di prodotti di scarto: da granito da
discarica a materia prima per ceramica e vetreria. GEAM, 4, 17-19.
BOZZOLA G., DINO G.A., FORNARO M., LORENZI A., MESTRINER T. &
SANDRIN D. (2008) – I residui dell’attività estrattiva: scarti da
deposito o neominiere da valorizzare? Atti del Conv. Naz. ANIM “I
rifiuti di cave e miniere: Decreto Legislativo 117/08; Problemi Tecnici
ed Amministrativi”. Roma, 19 dicembre 2008. 16 pp.

Key words: Alpi Apuane, marble, quarry.
INTRODUCTION
Marble quarrying activities throughout the Alpi Apuane area
in the northern Apennines are famous and worldwide known, and
nowdays during the technical-economic planning must also be
considered the environmental impact of the quarrying. Keeping
this in mind the Centro di GeoTecnologie and Soc Henraux S.p.a.
are putting forward a feasibility study of underground marble
quarrying near the M. Altissimo in the central Alpi Apuane.
The major advantage of this quarrying method it is the
possibilitiy to reach underground large volumes of white marble
without large modification of landscape.
GEOLOGICAL SETTING
The Alpi Apuane are a tectonic window located in the Italian
Northern Apennines, a fold-and-thurst chain formed during the
Tertiary due to the collision of the paleo-Europe and the paleo-
Africa continental margins. The deepest part of the inner northern
Apennines consists of the so-called Apuane Metamorphic
Complex (AMC) that comprises the metamorphic sequence
(Massa Unit and underlying “Autochthonous Auct.). Up wards
the AMC is followed by unmetamorphosed cover units. During
Tertiary continental deformation the rocks of the AMC suffered
severe deformation through development of a penetrative
foliation (S1) and millimetric to plurikilometric isoclinal folds
coeval with green schists facies metamorphism. Later
deformation (D2, tectonic phase) led to uplift and tectonic
exumathion characterized by a complicated internal geometry.
The Alpi Apuane are a known region because of large
outcrops of ornamental stones, among which the whitish and
_________________________
Underground marble quarrying in the Alpi Apuane, M.te Altissimo
LUIGI CARMIGNANI (*), PAOLO CONTI (*), GIOVANNI MASSA (*), LEONARDO DISPERATI (*),
RICCARDO SALVINI (*), SERGIO MANCINI (*), VINICIO LORENZONI (**), TOMMASO COLONNA (*),
ENRICO GUASTALDI (*), MARILENA TROTTA (*), SILVIA RICCUCCI (*),
MIRKO FRANCIONI (*) & LORENZO MARTINELLI (*)
(*) Centro di GeoTecnologie e Dip. Sc. Terra, Università degli Studi di Siena,
luigi.carmignani@unisi.it
(**) Soc. Henraux SpA
Work supported by the Regione Toscana project POR CREO FESR 2007/2013
521
variously decorated marbles are the most famous. The marbles of
the M. Altissimo region form an important district in the central
Apuane Alps and were exploited in many quarries active up to
some decades ago. The marble varieties are characterized by high
quality physical-mechanical properties often joined with very
appreciated ornamental features. The marbles crop out at the core
of the Altissimo Syncline, one of the major km-scale structures of
the “Autochthonous Auct.” unit, formed during the D1
compressional tectonics of the Tertiary orogenesis, and were
severely affected by the D2 tectonic phase.
EXPLOITATION PLAN
Aim of this study is to consider an area, in the properties of
the Henraux society in the M. Altissimo area, from which a tunnel
can be realized, to conduct an underground quarrying of marbles.
The approach consists in a multidisciplinary study. A detailed
structural geological field survey will be put forward and it will
be produced a geological map of the marble type occurrence and
their three-dimensional occurrence in the underground.
Digital Terrestrial Photogrammetry and Laser Scanning
techniques will be integrated with geological-engineering survey
in order to collect data necessary for the stability analysis of the
slope and the portal tunnel; this analysis will be performed using
the distinct elements numerical modelling
The phases of the projects includes the realization of two “in
situ” approaches by high-resolution geophysical surveys: a first
study of external rocks quality by seismic refraction technology
and a subsequent study of the main discontinuities and cavities by
geoelectrical surveys. The first goal of geophysical surveys is to
perform a preliminary study of potential seismic zone, in
relationships with the problems of tunnel construction and the
possible scenarios following a seismic event.
Furthermore we will delineate the hydrogeological knowledge
of the area, the characteristics of the hydrostructures, and the
aquifer state, by evaluating the relationships among water springs,
groundwater flow and underground infrastructures.
SESSIONE 16

SESSIONE 16
Key words: Alpi Apuane, marble, quarry.
INTRODUCTION
The marbles from the Alpi Apuane are well known geological
materials due to their extensive use as building stones. In this
abstract we present a syntesis of the results obtained in a field
study of the commercial marble varieties in the Alpi Apuane
basins of marbles.
This project was carried out by the "Centro di Geotecnologie"
of the Siena University and founded by the Geological Survey of
the “Regione Toscana”. Main goal of the project was to update
geological and quarrying activity informations from the Alpi
Apuane area in northern Tuscany.
GEOLOGICAL SETTING
The Alpi Apuane are a tectonic window located in the Italian
Northern Apennines, a fold-and-thurst chain formed during the
Tertiary due to the collision of the paleo-Europe and the paleo-
Africa continental margins.
The deepest part of the inner northern Apennines consists of
the so-called Apuane Metamorphic Complex (AMC) that
comprises the metamorphic sequence (Massa Unit and underlying
“Autochthonous Auct.).
Up wards the AMC is followed by unmetamorphosed cover
units. During Tertiary continental deformation the rocks of the
AMC suffered severe deformation through development of a
penetrative foliation (S1) and millimetric to plurikilometric
isoclinal folds coeval with green schists facies metamorphism.
Later deformation (D2, tectonic phase) led to uplift and tectonic
exumathion characterized by a complicated internal geometry.
_________________________
Maps and database of marble and quarry activities of the
Alpi Apuane (Tuscany)
LUIGI CARMIGNANI (*), PAOLO CONTI (*), GIOVANNI MASSA (*), LUCA VASELLI (*), SERGIO MANCINI (*)
ASSUNTA SFALANGA (*), ALICE FARINELLI (*) & MARCO IANNINI (*)
(*) Centro di GeoTecnologie e Dip. Sc. Terra, Università degli Studi di
Siena, luigi.carmignani@unisi.it
522
MAPS AND DATABASE OF MARBLE AND QUARRY
ACTIVITIES OF THE ALPI APUANE
The project consisted of three phases:
1. Initial gathering of geological informations by means of
field mapping and structural geologic investigations; this led to
production of thematic maps at 1:10.000 scale.
2. Realization of databases and a Geographic Information
System (GIS) to manage all the informations collected in the
previous phase.
Three types of maps are completed.
The Giacimentological Map is a geological map where all the
marble types outcropping in the area are mapped (white marble,
grey marble, marble breccia, etc.). In this maps all the Quaternary
deposits are also indicated (alluvium, slope deposits, landslides,
etc.) as the location of all the quarry, active and inactive.
The Map of the Quarry Debris ("ravaneti") are maps where
are reported all the anthropic deposits resulting from quarry
activity. This deposits are of great economic value as marble
blocks not suitable for cutting and production of facing stones are
now widely used in chemical industries because the elevated
content (>99%) of CaCO3 of this rocks. In this maps is reported
the extension of the quarry debris, the color of the marble blocks,
size of the blocks, etc.
The Structural Map is a structural geologic map where, with
information on marble types bedding and foliation attitudes, fold
axis, stretching and mineralogical lineations, etc…, are reported
A Geographic Information System is realized, with topologic
and relationship rules such to be fully integrated with GIS
produced by the Italian Geological Survey for the realization of
the 1.50.000 Geological Map of Italy ("Progetto CARG") and
with GIS produced by Tuscany Region for its geological mapping
project at 1:10.000 scale. The companion database contains all
the information of the maps, and furthermore photographs,
technical documentation of the present quarrying activity,
historical information on quarrying and exploited marbles.
All the information produced from the project are intended to
be useful for a more rational use of the marble natural resource,
for a three dimensional evaluation of the exploitable marble
bodies and for a more efficient environmental protection
planning.

THE LABORATORY
Together with geological investigations to better planning
quarrying activities, nowadays emphasis is on safe, permanent,
low maintenance products, of which the Alpi Apuane marbles
leads the list in the minds of architects, designers, and consumers
worldwide.
Without a consistent, realistic set of standards and testing
procedures for marble products, the stone industry as a whole
would be in disarray. The standards that have been developed and
set in place for these products are important tools to help protect
end users, individual companies, and the industry from negative
effects related to product failures. Materials standards help to
prevent the use of stone products for unsuitable applications.
The Soil Mechanics Testing Laboratory of the Centre for
GeoTechnologies of the Siena University (San Giovanni
Valdarno, Arezzo) has increased its testing equipment in order to
contribute to this research. The principal tests, according CE
marking standards for slabs, kerbs and setts of natural stone are:
Petrographic examination (EN 12407); Apparent density and
open porosity (EN 1936); Real density by helium pycnometer
(ASTM - D5550); Water absorption (EN 13755); Flexural
strength under concentrated load (EN 12372); Freeze-thaw
resistance (EN 12371); Abrasion resistance (EN 1341); Slip
resistance (EN 1341, 1342, 14231).
These tests also serve also to deliver benchmarks for quality
limits of products. If a stone with a below-minimum flexural
strength is used for a lintel, then it may be more likely to fail, thus
causing damage and possible injury. Interior or exterior flooring
or paving with an inadequate slip resistance level will more likely
cause slipping accidents in public or private projects.
523
SESSIONE 16

SESSIONE 16
Key words: Campiglia ridge, dislocation’s pattern, karst caves,
mining archaeology, preindustrial mines, skarn deposits,
speleothems.
This work represents an interdisciplinary speleological,
mining archaeological and geomorphological survey over the
Mesozoic Campiglia Ridge, in southern Tuscany. This is a typical
karst area (CASCONE G., 1993) but also a very important mining
district, well known for Cu-Pb-Zn (Fe, Ag) skarn deposits
(CORSINI et alii, 1980).
This area belongs to the Northern Apennines’ chain, and
several karst formations of the Tuscan Units crop out here,
ranging from the Liassic Calcare massiccio to the eocenicoligocenic
Scaglia Toscana. The prevalently outcrop is
represented by the Liassic massive limestone, characterized by
widespread karst phenomena; few important natural caves open
also in the Rosso ammonitico limestone formation, and secondly
in all the other formations: these natural drillings show wery well
the lithological control over the cave’s morphology. The
morphological profile of the Calcare massiccio caves is a
verticalness, which is due to the fault and fracture structural
setting, dipping from 60° to 85°, and NW-SE, NE-SW, N-S, E-W
trending. As a matter of fact the most caves have a prevalent
tectonic origin and belong to the percolation zones, while only a
few caves have been formed in the transition zone. At the actual
state of knowledge the karst carbonatic acquifer, with static level
25-30m asl (GRASSI et alii, 1990), is only intercepted by a few
caves that present an anomalous air temperature (>20°C). To
understand the karst evolution in this area, besides the structural
setting, it’s necessary to refer to the regional stratigraphy that
indicates that the maximum thickness of sediments over Calcare
massiccio formation, built during the Pliocene, was about 1500-
2000m (BARTHOLOMÈ & EVRARD, 1970). Only after the
progressive erosion of the covering sediments, due to the horst
raising, the underlying karst limestone has been interested by a lot
of decompressive fractures; in addition, the progressive onset of
an important hydraulic gradient (respect to the local sea level)
allowed the karst process evolution. Moreover in this area we can
_________________________
(*) Studio di Geologia, Livorno, giannacascone@tiscali.it
(**) Parco Minerario Naturalistico di Gavorrano,
parcominerario@comune.gavorrano.gr.it
The karst area and the preindustrial mines of the
Campiglia Marittima Ridge (LI -Tuscany)
GIOVANNA CASCONE (*) & ALESSANDRA CASINI (**)
524
face a lot of artificial caves, so-called preindustrial mining sites.
As a matter of fact, an important magmatic activity connected
to the post collisional phase, during from late Miocene to lower
Pliocene, lead up to emplacement of several intrusive anatectic
magmatic bodies with an acid to intermediate composition: at
first the granite outcrops of Botro ai Marmi (5.7 Ma, BORSI et alii
1967), than, between 5 an 4 Ma, several other porphyry dikes
intruded the eastern part (PECCERILLO et alii, 1987), producing
contact metamorphism (white marble) and metasomatism
processes (skarn deposits; TANELLI, 1977) inner the host rock, the
Calcare massiccio formation. Not all skarn bodies crop out: karst
phenomena exploration sometimes allowed the discovery of
depth skarn bodies excavated by preindustrial mining activity:
more than two hundred of preindustrial sites has been discovered.
The morphological setting of this mines is prevalently vertical
(Fig. 1) along all their extension (the deepest explorated mine is
120m depth), which is the same structure as in the carsic caves.
Fig. 1 – Biserno preindustrial mine (-120 m depth): shaft inner the altered
skarn.
It’s therefore evident the control of the local structural setting
over the ore deposits. In addition, because during the
preindustrial period the ore deposit has been only drawed along
the vein, the mine’s trend shows the ore deposit trending.
Therefore the cave’s mapping plane plot suggests the
dislocation’s pattern; these analyses can contribute to confirm or
deny the new hypotesys about the spatial and chronologic
relationship between the tectonic structures and the hydrotermal
fluids circulation.

The observed skarn complexes, frequently alterated, have
developed substantial radiating and concentring aggregates of
clinopiroxene with fibres long from 1 cm to more than 30 cm.
The macroscopic analyses of the skarn mine walls show it is free
from metal ores.
The skarn is visible completely enclosed in white marble and
the contact surface is often corroded. The skarn deposits inner the
ancient mines have been never observed in contact with porphyry
dikes.
To understand the frequent underground coesistence of
natural and artificial emptyness, it must be remembered that skarn
deposits represent a permeability boundary to the karst process
inside of the permeable limestone host rock.
Both natural caves, as well as the ancient mines, present
various carbonate speleothem types formed by flowing water,
dripping water and seeping water. The mine’s speleothems often
show green-blue and red-brown colour, due to impurity copper
metal ions and to several pigmenting substances as oxides and
hydroxides of iron and manganese.
The study of the pre-industrial mining system brought to light
and documented the ancient mining techniques and their
evolution. It was possible to recognize four major historical
periods of intensive mining, alternated with other phases,
distinguished by an apparently total lack of interest for these
metal sources. These periods may be defined as follows: 7 th – 1 st
Century BC; 10 th – 14 th Century AD; 16 th Century; 19 th – 20 th
Century AD (CASINI, 1993; CASCONE & CASINI, 1998). The
settlements of this area (from the Etruscan Period to the 16 th
Century AD) were specifically centered on mining.
The size of the shaft and the galleries depends from the
relevance of the deposit but also from its interaction with preexisting
karst caves. Sometimes, in the calcite deposits, which
coat the floor of some oblique galleries, we could identify the
imprints of wooden elements (CASCONE &CASINI, 1998). Mining
techniques, marks left by digging, filled cavities by selected
material, free from metal bearing ores, show traces of the
technical evolution and organization of workmanship (CASCONE
&CASINI, 1997; CASINI, 1993, 2007).
The strategy of this interdisciplinary survey is based on three
key points: the new findings of the research; the integrated
development of the cultural and natural resources; the measures
for the protection of the heritage and the historical landscape.
REFERENCES
ACOCELLA V., ROSETTI F., FACCENNA C., FUNICIELLO R. &
LAZZAROTTO A. (2000) - Strike-slip faulting and pluton
emplacement in Southern Tuscany: the Campiglia Marittima
case. Boll. Soc. Geol. It, 119, 517-528.
BARTHOLOMÈ P. & EVRARD P. (1970) - On The genesis of zoned
skarn at Temperino, Tuscany. Inter. Union. Geol. Sci., Ser. 2:
525
Problems of hydrothermal ore deposition. Schweerbart
Stuttgart, 53-57.
BORSI F., FERRARA G. & TONGIORGI E. (1967). Determinazione
con il metodo del K/Ar dell’età delle rocce magmatiche della
Toscana. Boll. Soc. Geol. It., 86, 403-410.
CASCONE G. (1993) – La zona speleologica del Massiccio del
Monte Calvi. Primo contributo alla sua conoscenza. In:R.
Mazzanti (Ed.) - La scienza della terra nell'area della
Provincia di Livorno a sud del fiume Cecina. Suppl. n.2
Quad. Mus. Stor. Nat. di Livorno, 13, 183-212.
CASCONE G. & CASINI A. (1997) - Le miniere antiche di
Campiglia M.ma (LI). Atti del IV Conv. Naz. sulle Cavità
Artificiali, Osoppo 30 May -1 June 1997, Trieste, 29-50.
CASCONE G. & CASINI A (1998) - Pre-Industrial Mining
Techniques in the Mountains of Campiglia Marittima
(Livorno). In: S. Milliken and M. Vidale (Eds.) - Craft
Specialization: Operational Sequences and Beyond. EAA
Third Annual Meeting at Ravenna 1997, Volume IV, British
Archaeological Reports International Serie 720, 149-151.
CASINI A. (1993) - Archeologia di un territorio minerario: i
Monti di Campiglia. In R. Mazzanti (Ed.) - La scienza della
terra nell'area della Provincia di Livorno a sud del fiume
Cecina. Suppl. n.2 Quad. Mus. Stor. Nat. di Livorno, 13, 303-
314.
CASINI A. (2007) - L’extraction du cuivre et de l’argent dans les
Monts de Campiglia Marittima (Toscane) de l’époque
étrusque au XVIe siècle, in M.C Bailly-Maitre and J.M.
Poisson (Eds.) - Mines et Pouvoir au moyen age, Le contrôle
seigneurial de l'exploitation minière au Moyen Âge. PUL,
Lyon.
CORSINI F., CORTECCI G., LEONE G. & TANELLI G. (1980) -
Sulfur isotope study ok skarn (Cu-Pb-Zn) sulfide depositi of
Valle del Temperino, Campiglia Marittima, Tuscany, Italy.
Econ. Geol., 75, 83-96.
GRASSI S., SQUARCI P., CELATI R., CALORE C., PERUSINI P. &
TAFFI L., (1990) – Nuove conoscenze sul sistema idrotermale
di Campiglia Marittima (Livorno). Boll. Soc. Geol. It, 109,
693-706.
PECCERILLO A., PONTICELLI S. & MANETTI P. (1987) –
Petrological characteristics and genesis of recent magmatism
of Southern Tuscany and Northern Latium. Per. Mineral., 56,
157-172.
TANELLI G. (1977) - I giacimenti a skarn della Toscana. Rend.
Soc. It. Min e Petrol., 33 (2), 875-903.
SESSIONE 16

SESSIONE 16
The archaeological area of San Gaetano di Vada (LI): lithological
and petrographic characterization of marble artefacts from
HORREA and thermal baths
Key words: Archaeological site, marble artefacts, petrography,
greco scritto, provenance determination, San Gaetano.
This work represents the preliminary study of marble artefact
samples coming from the archaeological site of San Gaetano,
Vada (Rosignano Marittimo - LI). The Department of Historical
Sciences of the Ancient World of Pisa University has been
responsible for the excavation of the archaeological site since
1982 and the works are still in progress. A coastal plain village
dating back to the Roman period has been dug out: it includes
remains of baths, storerooms and other structures; the
archaeologists think it was near the harbour of ancient Vada
Volaterrana. The results of this interdisciplinary study are about
to be published in the following collection of scientific essays:
“Vada Volaterrana. Area archeologica in località S. Gaetano.
Gli Horrea. Stratigrafie, strutture, materiali”, edited by M.
Pasquinucci, S. Menchelli and P. Sangriso.
The main purpose of this study is to outline a preliminary
frame for the samples coming from the storerooms (Horrea) and
then for the ones coming from the little thermal bath. The aim
was to find a realistic reference frame in order to detect where the
lithoid manufacts may come from. The numerous restrictions due
both to the sample shape and size, and to their preservation, do
not allow to use integrated investigations methods (MARIOTTINI,
1998; LAPUENTE et alii, 1995) such as mineralogical,
geochemical, diffrattometric, spectroscopic and
cathodoluminescence analyses. This research is, therefore, a first
lithological and petrographical characterization. The unknown
orientation of the samples as to their original position in the
quarry and the paving stone samples shape, did not permit the
application of MGS and QFA methods to the polarized
microscopic examination of the thin sections.
The lithological characterization is related to 39
representative samples, while the petrographical study is related
to 25 thin sections. 20 of the thin sections concern white, grey
and veined marbles, the remaining ones the coloured “marbles”:
by “marbles” archaeologists mean all the ornamental rocks.
_________________________
(*) Studio di Geologia, Livorno, giannacascone@tiscali.it,
barbara.ghiribelli@yahoo.it
GIOVANNA CASCONE (*) & BARBARA GHIRIBELLI (*)
526
Fig. 1 – Paving stone in the little thermal bath floor (A group) - scale 1: 10.
In the main white, grey and veined marble group we have
detected 3 further similar groups.
A Group: white, predominantly medium-coarse grain marble
with fine grey-black-bluish veined and spotted, found in situ in
the little thermal bath floor called vestibulum (Fig. 1); the A
group presents a grano-xenoblastic heteroblastic texture and it is
characterized by abundant presence of opaque minerals both
concentrated in irregular veins along the intercrystalline
boundaries and dispersed in the carbonatic mass.
B Group: white medium grain marble characterized by a
strong dynamic intercrystalline (grain boundary migration) and
intracrystalline (sub-grain boundary) recrystallization due to
mylonitic deformation (Fig. 2).
C Group: white fine grain marble, also visible in situ, was
used as building material for two frames in the thermal bath
frigidarium and in a capital, in a column and in a pillar. It shows
grano-omeoblastic texture characterized by triple junctions that
indicate an annealing process (CARMIGNANI et alii, 2007)
In the second smaller coloured “marble” group, a wide
lithological range referred to sedimentary, magmatic and
metamorphic rocks are observed. The size and the uniqueness of
these samples did not allow to produce a lot of thin sections;
therefore, only 5 samples have been observed under the polarized
microscope: 1 red porphyry, 1 green porphyry, 2 metalimestones
and 1 micaschist.
In the range of the grey and veined marbles, the predominant

Fig. 2 – Photomicrograph of the thin section of sample n.13 (B group)
showing recrystallization along an axial plane. Crossed Nicols 125x.
artefacts are probably identifiable with the so-called greco scritto,
a North African lithotype (ANTONELLI et alii, 2009), while in the
range of the white fine grain marbles their provenance may be
both from the Greek and/or Anatolian area, or the Italian Apuan
quarries. In the range of the medium-coarse grain marbles the
origin both from Italian Apuan quarries and Italian Campiglia
Marittima (MANNONI et alii, 1995) quarries are macroscopically
and petrographically ruled out; finally the observed mylonitic
marbles (LAZZARINI et alii, 1980; AMADORI et alii, 1998) could
probably belong to a particular geostructural domain and
therefore they need further and specific analyses. On the other
hand, in the range of the coloured “marble” group, many of them
are lithotypes coming from this archeological site related to the
more common marble used in the ancient times and in particular
they are: Lapis porphirites (Egypt), Marmor numidicum and its
breccia (Egypt), Marmor carystium (Greece), Marmor tenarium
(Greece), Lapis lacedaemonius (Greece), Pietra bekhen (Egypt),
Marmor sagarium (Turkey), Marmor iassense (Turkey), Marmor
sagarium (Turkey), Lapis hecatonthalitos (Egypt), Marmor
scyrium (Greece), Lapis alabastrites (Egypt), Marmor phrygium
(Turkey), Granito della colonna (Egypt) and Marmor
Thessalicum (Greece).
This work allowed a realistic correlation between the
examined coloured “marble” samples and the commercial
typology used during the Roman Empire (GNOLI, 1988;
LAZZARINI, 2002). Most of the white, grey and veined marbles
need additional integrated analyses to try to identify their
geographical origin.
REFERENCES
AMADORI M.L., LAZZARINI L., MARIOTTINI M., PECORAIO M. &
PENSABENE P. (1998) - Determinazione della provenienza dei
marmi usati per alcuni monumenti antichi di Roma. In: P.
527
Pensabene (Ed.) - Marmi antichi II. Studi Miscellanei, 31, 45-
56.
ANTONELLI F., LAZZARINI L. & CANCELLIERE S. (2009) - Mineropetrographic
and geochemical charaterization of “Greco
Scritto” marble from Cap de Garde, near Hippo Regius
(Annaba, Algeria). Archeometry, 51 (3), 351-365.
CARMIGNANI L., CONTI P., FANTOZZI P., MANCINI S., MASSA G.,
MOLLI G. & VASELLI L. (2007) - I marmi delle Alpi Apuane.
Geoitalia, 21, 19-30.
GNOLI R. (1998) - Marmora Romana. Dell'Elefante, Roma, pp.
298.
LAZZARINI L., PENSABENE P. & TURI B. (1995) - Isotopic and
petrographic charaterization of Marmor Lesbium, island of
Lesbos, Greece. Actes de la IV éme Conf. Intern. Ass. Étude
Marbres et autres Roches Utlisés dans le Passé, Bordeaux,
125-129.
LAPUENTE P., TURI B., LAZZARINI L. & NOGALES T. (1995) -
Provenance investigation of white marble sculptures from
Augusta Emerita, Hispani. Actes de la IV éme Conf. Intern.
Ass. Étude Marbres et autres Roches Utlisés dans le Passé,
Bordeaux, 111-116.
LAZZARINI L. (2002) - La determinazione della provenienza delle
pietre decorative usate dai Romani. In L. Ungano and M. De
Nuccio (Eds.) - I marmi colorati della Roma imperiale
(catalogo mostra), Roma, 223-262.
LAZZARINI L., MOSCHINI G. & STIEVANO B.M. (1980) - A
contribution to the identification of Italian, Greek an
Anatolian marbles through a petrological study and the
evaluation of Ca/Sr ratio. Archeometry, 22 (2), 173-183.
MANNONI T., CASINI A. & PARENTI R. (1995) - Il marmo pario
dell’Etruria. In: G. Cavalieri Manasse and E. Roffia (Eds.) -
Splendida Civitas Nostra. Studi archeologici in onore di
Antonio Frova. Quasar, Roma, 343-359.
MARIOTTINI M. (1998) - La provenienza dei marmi cristallini
usati in antico: un problema aperto. In: P. Pensabene (Ed.) -
Marmi antichi II. Studi Miscellanei, 31, 23-35.
SCHMID J., RAMSEYER K&DECROUEZ D. (1995) - A new
element for the provenance determination of white marbles:
quantitative fabric analysis. Actes de la IV éme Conf. Intern.
Ass. Étude Marbres et autres Roches Utlisés dans le Passé,
Bordeaux, 171-175.
TRISCARI M., SABATINO G. & LANZA S. (2002) - Identification of
ancient marbles from the straits of Messina area. Plinius, 28,
278-280.
REGIONE TOSCANA, GIUNTA REGIONALE & ERTAG (1980) -
Marmi apuani: schede merceologiche. Nuova Grafica
Fiorentina, Firenze.
SESSIONE 16

SESSIONE 16
The classification of igneous, sedimentary and metamorphic rocks
and the UNI/CEN terminology of natural stones
DANIELE CASTELLI (*), LAURA GAGGERO (**), PAOLO MAZZOLENI (°) & SERGIO ROCCHI (°°)
Key words: IUGS recommendations, rock classification and
nomenclature schemes, UNI/CEN standards.
The scientific classification of rocks has been the subject of
frequent debate and voluminous literature for ages, because
decades of field and laboratory studies have resulted in a vast,
and sometimes overwhelming, array of nomenclature and
terminology.
In recent years, the use of databases for storing geological
information has grown considerably, and there has been a
remarkable increase in the degree of collaboration between
universities, scientific to cultural institutions, and industries. To
maximise efficiency in the use of geological information and to
facilitate collaborative work, a common approach to classifying
and naming rocks is essential (e.g. GILLESPIE &STYLES, 1999;
MIBAC-ICCD, 2007).
After some pioneering works (e.g. STRECKEISEN, 1967, 1976),
the International Union of Geological Sciences (IUGS)
Subcommission on the Systematics of Igneous Rocks (SSIR: a
branch of the IUGS Commission on the Systematics in
Petrology), eventually proposed a complete classification of
igneous rocks (LE MAITRE, 1989) that most geologists have
increasingly accepted as the standard when studying igneous
rocks, either in the field or the laboratory. In addition to the
classification rules, it comprised a glossary of terms that has been
updated in the second edition (LE MAITRE, 2002) to include more
than 1600 entries, of which 316 are recommended, with a
comprehensive bibliography of source references for all the terms
included in the glossary.
Because many common terms in metamorphic petrology also
vary in their usage and meaning between countries, a companion
IUGS Subcommission (the Subcommission on the Systematics of
Metamorphic Rocks: SCMR) started operating in 1985 in order
to provide a scheme for naming and describing metamorphic
rocks that could be used worldwide. Following the scheme of
_________________________
(*) Dipartimento di Scienze Mineralogiche e Petrologiche, Università di
Torino, daniele.castelli@unito.it
(**) Dipartimento per lo Studio del Territorio e sue Risorse, Università di
Genova, gaggero@dipteris.unige.it
(°) Dipartimento di Scienze Geologiche, Università di Catania,
pmazzol@unict.it
528
SSIR products, provisional recommendations were published and
critical comment encouraged. The SCMR has recently presented
a recommended nomenclature of metamorphic rocks, with an
inclusive glossary of definitions, sources and etymology of over
1200 terms (FETTES &DESMONS, 2007). This text also includes
multi-authored sections (dealing with rocks from high- to lowand
very-low-grade) that explain how to derive the correct names
for metamorphic rocks and processes.
The task of a unified scheme for classifying sedimentary rocks
and their unlithified equivalents has not yet been accomplished by
the IUGS Subcommission on the Systematics of Sedimentary
Rocks (SSR), and natural groups of sediments and sedimentary
rocks have been classified separately by different authors (e.g.
FOLK, 1959; PETTIJOHN et alii, 1987). Many institutions and/or
research teams have therefore developed their own
recommendations (e.g. HALLSWORTH & KNOX, 1999). The
SEDimentary dataBAse (SEDBA), a system for storing,
retrieving and utilizing petrological data pertaining to
sedimentary rocks (http://www.ige.csic.es/sdbp/sedba.htm) was
also developed as IGCP Project 269, funded by UNESCO and
IUGS, for broad geological use by both geoscientists and
prospective users dealing with sedimentary rocks as building and
decorative materials or as materials in chemical and industrial
manufacturing processes (e.g. HARGBAUGH, 1989).
The classification of rocks has been also an important subject
in the frame of standardisation developed by UNI (Italian
Organization for Standardization) and CEN (Comité Européen de
Normalisation). For example, the UNI 8458:1983 document
(“Building - Natural building stones - Terminology and
classification”) defined, in addition to technical properties of
quarried natural stone materials (such as size, fissility, defects,
working techniques, etc.), the long-used commercial terms:
marmo, granito, travertino and pietra applied to the building
industry.
In 1991, a Technical Committee (CEN/TC 246 - Natural
Stones) began to work on a simplified classification of rocks and
minerals (e.g. KRAEFT, 1997, with refs.), and the European
standards EN 12440:2000 (“Natural stone – Denomination
criteria”), EN 12670:2001 (“Natural stone – Terminology”), and
EN 12407:2007 (“Natural stone test methods – Petrographic
examination”) were published by CEN.
Main objective of the EN 12440:2000 standard was to unify
the designation criteria of natural stone varieties, maintaining the

traditional names used by the international marketing, with an
informative annex providing a non-exhaustive list of the names
under which most stones from each contributing European
country were known. This document has been recently upgraded
by CEN, with the later endorsement of UNI (UNI EN
12440:2008 standard).
The EN 12407:2007 standard (and its Italian version: UNI
EN 12407:2007) focus on the petrographic description of natural
stone not only for the purposes of petrographic classification, but
also in order to highlight features influencing its chemical,
physical and mechanical behaviour, and the importance of the
stone’s origin in the case of restoration of historical monuments
and cultural heritages. The EN 12670 and EN 12440 are stated as
indispensable for the application of this document.
The EN 12670:2001 (“Natural stone – Terminology”)
standard has been translated and approved by the UNI Technical
Commission “Products, processes and systems for building” (i.e.
the UNI EN 12670:2003 standard, replacing the aforementioned
UNI 8458:1983). This document is important because, in
addition to the recommended technical terminology covering test
methods, products, and classification of natural stones, it also
claims at defining the scientific terminology of minerals and
rocks. Definitions of some 450 geological terms and schemes for
the scientific classification of igneous, sedimentary and
metamorphic rocks are included. Classification of igneous rocks
follows LE MAITRE (1989); limestones and siliciclastic rocks are
classified according to FOLK (1959, 1962) and FOLK et alii
(1970), respectively. Classifications of metamorphic and other
sedimentary rocks do not follow any rule commonly used by
geoscientists, and part of the glossary needs some polishing. In
view of the role of EN 12670:2001 and UNI EN 12670:2003
standards in interdisciplinary, collaborative work, the Società
Italiana di Mineralogia e Petrologia has recently set a
Committee in order to address these problems and to provide
suggestions and comments for a revision of the document.
REFERENCES
FETTES D. & DESMONS J. (EDS.) (2007) – Metamorphic rocks : a
classification and glossary of terms: recommendations of the
International Union of Geological Sciences Subcommission
on the Systematics of Metamorphic Rocks. Cambridge
University Press, 244 p.
FOLK R.L. (1959) – Practical petrographic classification of
limestones. Am. Ass. Petroleum Geol. Bull., 43, 1-38.
FOLK R.L. (1962) – Spectral subdivision of limestone types. In:
W.E. Ham (Ed.) - Classification of Carbonate Rocks-A
Symposium. Am. Ass. Petroleum Geol. Memoir, 1, p. 62-84.
529
FOLK R.L., ANDREWS P.B. & LEWIS D.W. (1970) – Detrital
sedimentary rock classification and nomenclature for use in
New Zealand. New Zeal. J. Geol. Geoph., 13, 937-968.
GILLESPIE M.R. & STYLES M.T. (1999) – BGS Rock
Classification Scheme. Volume 1 – Classification of igneous
rocks. British Geol. Survey Res. Report, (2 nd edition), RR 99-
06, 54 p.
HALLSWORTH C.R. & KNOX R.W.O’B. (1999) – BGS Rock
Classification Scheme. Volume 3 – Classification of
sediments and sedimentary rocks. British Geol. Survey Res.
Report, RR 99-03, 46 p.
HARGBAUGH J.W. (1989) – International Geological Correlation
Project (IGCP) 269 - SEDBAS: Global Data Base for
Sedimentary Petrology. Carbonates and Evaporites, 4(1),
128-129.
KRAEFT U. (1997) – Classifications of rocks and minerals.
European Geologist, 6, 52-54.
LE MAITRE R. W. (Ed.) (1989) – A classification of igneous rocks
and glossary of terms: Recommendations of the International
Union of Geological Sciences Subcommission on the
Systematics of Igneous rocks. Blackwell, 193 pp.
LE MAITRE R. W. (Ed.) (2002) – Igneous Rocks: a Classification
and Glossary of Terms: Recommendations of the
International Union of Geological Sciences Subcommission
on the Systematics of Igneous Rocks - 2nd Edition.
Cambridge University Press, 236 pp.
MIBAC-ICCD (2007) – Strutturazione dei dati delle schede di
catalogo. Scheda BNPE: Beni Naturalistici - Petrologia.
Ministero per i Beni e le Attività Culturali – Istituto Centrale
per il Catalogo e la Documentazione. 116 pp.
PETTIJOHN F.J., POTTER P.E. & SIEVER R. (1987) – Sand and
sandstone. 2nd Edition. Springer-Verlag, 553 pp.
STRECKEISEN A. L. (1967) – Classification and nomenclature of
igneous rocks. N. Jb. Miner. Abh., 107, 144-240.
STRECKEISEN A. L. (1976) – To each plutonic rocks its proper
name. Earth Sc. Rev., 12, 1-33.
SESSIONE 16

SESSIONE 16
Building materials of the prehistoric altar of Monte d’Accoddi (Sassari-Italy)
Key words: Monte d’Accoddi, mortars, ornamental stones,
physico-mechanical characterization.
INTRODUCTION
This work deals with archaeometric investigations carried out,
in view of a future restoration and consolidation, on the
prehistoric altar of Monte d’Accoddi (Sassari, Italy; Fig. 1). This
is a ziqqurat shaped monument discovered in the 1954 close to
the Sassari town (Sardinia, Italy). The monument, exclusive for
its characteristics in the Mediterranean basin, was part of a
prenuragic complex (aged 4000 years B.C), where performed the
function of religious altar (CONTU, 2000).
BULDING STONES CHARACTERIZATION
Fig.1 –Theziqqurat shaped altar of Monte d’Accoddi.
The monument is made up of two limestones (called
respectively CA and CO) belonging to the Miocene carbonate
succession of the Porto Torres basin (THOMAS &GENNESAUX,
1986), where the altar lies. CA facies is a fine grained calcarenite
characterized by a pitting decay while CO facies is a rhodolitesrich
grainstone. In the ashlars interstices of the masonries also an
original mortar is present.
In the past similar rocks were largely utilized as building
stones in all neighborhood, particularly in the edification of Porto
Torres (the ancient Roman colony of Turris Libisonis) and
Sassari (CARTA et alii, 2005).
_________________________
(*) Dipartimento di Scienze Botaniche, Ecologiche e Geologiche,
Università di Sassari, scuccuru@uniss.it.
STEFANO CUCCURU (*), PAOLA MAMELI (*) & ANTONIO BRUNDU (*)
530
An exhaustive physico-mechanical characterization of these
stones has been performed carring out the following tests:
- Dry density (UNI EN 9724/2);
- Water absorption at atmospheric pressure (UNI EN
13755:2002);
- Open porosity;
- Capillarity water absorption (UNI EN 1925:2000);
- Ultrasonic velocity;
- Uniaxial compressive strength – UCS - (UNI EN
1926:2000)
- Compressive strength measures with the Schmidt hammer.
All tests show different physico-mechanical behaviors (Table
1) of the two limestone facies.
The CO sample, which macroscopically seems the tougher,
once cut for the realization of the specimens, showed numerous
karstified cavities filled by soil. The CA sample instead, despite
some pitting evidence in the surface, was relatively homogeneous
and devoid of karstic cavities. Due to the karstic cavities, CO
showed a dry density value less than CA. The highest value of
open porosity in the CA instead is due to the occurrence of
numerous intergranular cracks. In the CO facies, the cavities have
a close macroporosity and the rhodolitic portions, very abundant
in this rock, are not porous.
As for water absorption, the values at atmospheric pressure
are almost similar. Conversely the capillarity absorption values in
the CO facies is almost double than CA facies. Probably this
behavior is due to the large amount of karstic cavities filled with
soil which tend to absorb large amounts of water by capillarity.
Finally in the CA facies higher UCS values has been obtained
owing to the lack of karstic voids. Also ultrasonic velocity
highlighted this physico-mechanical feature.
MORTARS CHARACTERIZATION
Drew mortar samples were subjected to optical microscopy
(OM) minero-petrographical analyses on thin section and
diffractometer X-ray (XRD) mineralogical analyses on powders.
The analyses in thin section showed that the mortars are made
of a marly binder with quartz grains, feldspars, oxides of various
composition and fragments of calcitic fossils as inert. Wasted
bivalves and bones are also common. These data are confirmed
by the XRPD analyses which indicate also the presence of
phyllosilicate minerals (particularly illite and kaolinite).

CO Facies CA Facies Average value
Dry density (g/cm 3 ) 2,14 2,39 2,26
Water absorption at
atmospheric pressure (%)
6,59 8,58 7,59
Open porosity (%) 14,08 19,40 16,74
Capillarity water
absorption –C- (g/m 2 s 0,5 )
11,96 6,61 9,29
Uniaxial compressive
strength (MPa)
21,40 23,49 22,45
Ultrasonic velocity (m/s) 4190,6 4365,32 4277,96
Tab.1 – Physical and mechanical properties analyzed.
All these data indicate that the mortars are made with
products of the decay of the surrounding rocks with the constant
presence of bones and shells.
CONCLUSIONS
Two main suggestions issue from the investigations:
- CO facies, due its poor physic-mechanical quality and
high value of capillarity water absorption, is not suitable
for the replacement of basal ashlars;
- The mortar was made with local raw materials similar to
the muddy soil stretching around the site. The occurrence
of edible bivalves and bones suggest that the mortar
derives from earthy material plenty of wastes from life
activity.
REFERENCES
CARTA L., CALCATERRA D., CAPPELLETTI P., LANGELLA A. &
DE’ GENNARO M. (2005) – The stone materials in the
historical archietcture of the ancient center of Sassari:
distribution and state of conservation. J. Cult. Herit., 6, (3)
277-286.
CONTU E. (2000) – L’altare preistorico di Monte d’Accoddi. -
Sardegna Archeologica. Carlo Delfino Editore, Sassari.
THOMAS B. & GENNESSEAUX M. (1986) – A two stage rifting in
the basin of the Corsica-Sardinia strait. Mar. Geol., 72, 225-
239.
531
SESSIONE 16

SESSIONE 16
Effect of thermal stress on hydric dilatation of clay-bearing stone materials:
preliminary experiments on some “Macigno” sandstones
Key words: Macigno sandstone, physical properties, hydric
dilatation.
INTRODUCTION
The role of hydric dilatation (i.e. the deformation of a rock in
response to water absorption) in the decay of sandstones, and the
relationship between this property and the presence of expansible
clay minerals have been recently discussed by several authors
(FRANZINI et alii, 2007a, 2007b, 2008; BENAVENTE et alii, 2008;
SEBASTIAN et alii, 2008). How this property changes in
degradated stones is, instead, poorly investigated. In this
framework, this work presents the results of preliminary
experiments carried out to investigate how the hydric properties
of “Macigno” sandstone are modified by thermal stress.
THE “MACIGNO” SANDSTONE
The “Macigno” Formation (Upper Oligocene-Lower
Miocene) belongs to the stratigraphic sequence of the Tuscan
Nappe Unit. This formation outcrops extensively in the northwestern
Tuscany, with some occurrences also in the south of this
region. Since Middle Age, these sandstones have been widely
employed in buildings of several Tuscan villages and towns. The
homogeneous very fine-grained variety characterized by a dark
bluish grey colour is known as “Pietra Serena”. It consists of fine
to medium, sometimes coarse grain-size siliciclastic sandstones,
of turbiditic origin, mainly composed of quartz, feldspars and
micas. The colour is grey to light-bluish grey when unweathered.
These sandstones are appreciated for their good technical
properties even though, when used outdoor, they undergo a
typical process of decay consisting prevalently in flaking of the
stone surface with detachment of rock fragments.
_________________________
GIULIA DA PRATO (*), ANNA GIONCADA (*), LEONARDO LEONI (*) & MARCO LEZZERINI (*)
(*) Dip. Scienze della Terra, University of Pisa, gioncada@dst.unipi.it,
leoni@dst.unipi.it, lezzerini@dst.unipi.it
532
RESULTS
Samples of “Macigno” sandstone were taken from active
(Greve in Chianti, FI) and historical (Gonfolina, FI) quarries. The
samples had similar grain-size and were devoid of apparent
weathering. Prismatic specimens, 20×20×60 mm 3 in size,
underwent several cycles of heating from room temperature
(20°C) to 110 ± 5°C; cooling was carried out without quenching,
to avoid the mechanical decay effect of thermal shocks. The same
experiments were carried out on a series of specimens of other
Tuscan sandstones and metasandstones, to compare the behaviour
of rocks with different mineralogical compositions. Some hydric
properties such as hydric dilatation, water absorption after water
immersion and water absorption by capillarity were measured
before and after the heating/cooling experiments.
The results indicate that the “Macigno” sandstones maintain
the capability to dilate after heating to 110°C. The amount of
dilatation (α, mm/m) is, however, 20 to 40% lower in the
measured specimens. In samples showing anisotropy of this
property, the dilatation is higher when measured orthogonally to
bedding also after the thermal treatments. Water saturation by
total immersion is similar or slightly higher, but the capillarity
coefficients are lower, suggesting that the open porous network of
the rocks was irreversibly modified by the thermal treatments.
Also the sandstones and metasandstones without expansible clays
in the matrix showed lower hydric dilatation values after heating
to 110°C, indicating that the decrease in dilatation is related to
modifications in the porous network and not only to the presence
of expansible clay minerals.
REFERENCES
BENAVENTE D., CULTRONE G. & GOMEZ-HERAS M. (2008) The
combined influence of mineralogical, hygric and thermal
properties on the durability of porous building stones. Eur. J.
Mineral., 20, 673-685.
FRANZINI M., LEONI L., LEZZERINI M. & CARDELLI R. (2007a) -
Relationships between mineralogical composition, water
absorption and hydric dilatation in the "Macigno" sandstones
from Lunigiana (Massa, Tuscany). Eur. J. Mineral., 19, 113-
123.

FRANZINI M., LEONI L., LEZZERINI M., GIONCADA A. & BAGLINI
P. (2007b) - Relazioni fra composizione mineralogica e
proprietà fisiche nell’arenaria “Macigno” dei Monti d’oltre
Serchio (Toscana Occidentale). Atti IV Congresso Nazionale
AIAR, pp. 291-305.
FRANZINI M., GIONCADA A., LEONI L. & LEZZERINI M. (2008) -
Uno strumento per la misura della dilatazione idrica lineare
delle rocce. Atti Soc. Tosc. Sci. Nat., 113, 57-62.
SEBASTIAN E., CULTRONE G., BENAVENTE D., LINARES L., ELERT
K. & RODRIGUEZ-NAVARRO C. (2008) - Swelling damage in
clay-rich sandstones used in the church of San Mateo in
Tarifa (Spain). J. Cult. Herit., 9, 66-76.
533
SESSIONE 16

SESSIONE 16
Key words: Brick clay, ceramic raw materials, clay deposits.
Italy is traditionally one of the major clay brick and roof tile
manufacturers in Europe, with 155 operating brickworks for a
current output around 18 million tons per year. Approximately
1,200 brickworks have been operating in the period from 1960 to
2010, utilizing on the whole about 750 million tons of clay
materials extracted from about 1,600 quarries (DONDI &
MARSIGLI, 1998) distributed all over the Italian territory (Fig. 1).
The industrial requirements have been fed exploiting a wide
range of clay resources: recent alluvial, eluvial and colluvial
deposits; Quaternary fluvio-glacial blankets; lacustrine to marine
Plio-Pleistocene sediments; and a plethora of Tertiary to
Cretaceous formations, including continental to deepsea deposits
and tectonic mélanges (FABBRI &DONDI, 1995a; DONDI et alii,
1999).
A survey of clay sources – including how their use has been
changing in the last decades – is drawn for different areas:
Piemonte and Liguria; Lombardia; Veneto, Trentino-Alto Adige
and Friuli-Venezia Giulia; Emilia-Romagna; Toscana and
Umbria; Marche, Abruzzo and Molise; Lazio and Campania;
Puglia, Basilicata and Calabria; Sicilia; Sardegna.
A picture of clay brick manufacturing trends over the last 50
years is presented as number of brickworks, yearly output,
production capacity, mean brickwork size and average clay
tonnage extracted from quarries.
Statistical trends are discussed in function of clay reserves;
geographical distribution of deposits; excavation procedures;
environmental impact and remediation; technological onnovation
in the brickwork; clay properties and technical requirements for
bricks and roof tiles (FABBRI &DONDI, 1995b).
REFERENCES
DONDI M. & MARSIGLI M. (1998) Argille per l’industria italiana
dei laterizi: giacimenti e tendenze nel periodo 1960-1996.
Ceramurgia, 28(3), 163-171.
DONDI M., ERCOLANI G., FABBRI B., GUARINI G., MARSIGLI M. &
MINGAZZINI C. (1999a) -Major deposits of brick clays in
Italy. Part 1: Geology and composition. Tile & Brick Int.,
15(4), 230-237.
_________________________
(*) ISTEC CNR Faenza, michele.dondi@istec.cnr.it
Brick clays in Italy: deposits and trends 1960-2010
MICHELE DONDI (*)
534
Fig. 1 – Number of brick clay quarries in operation from 1960 to 2010.
DONDI M., ERCOLANI G., FABBRI B., GUARINI G., MARSIGLI M. &
MINGAZZINI C. (1999b) -Major deposits of brick clays in
Italy. Part 2: Technological properties and uses. Tile & Brick
Int., 15(5), 360-370.
FABBRI B. & DONDI M. (1995a) -La produzione del laterizio in
Italia. Gruppo Editoriale Faenza Editrice 160 pp.
FABBRI B. & DONDI M. (1995b) -Caratteristiche e difetti del
laterizio. Gruppo Editoriale Faenza Editrice 144 pp.

The restoration of the stone between theory and needs
Key words: Architecture, natural stones, restoration,
substitution.
The vicissitude of stone’s restoration is discussed for a long
time on two opposite positions.
According to the theory of restoration, prevailing today in the
western culture, interventions on degraded stone are made with
products and materials different from the original ones, but
compatible with its physical characteristics and feature behaviors.
At the beginning, the possibility of replacing a stone element,
even if degraded, with one of the same petrographic, it was not
admitted because we would have made a false.
This approach, in the conservation of original material, is
looking for the main objective of the intervention (Fig. 1).
This attitude contrasts with an ancient tradition, which
contemplates the possibility of replacing a degraded element with
Fig. 1 – The cathedral of Milan during the recent restoration of facade made
by Candoglia marble.
_________________________
(*) Politecnico di Torino, II Facoltà di Architettura (DITAG),
maurizio.gomez@polito.it
MAURIZIO GOMEZ SERITO (*)
535
one of the same origin and nature, possibly wrought and installed
with the same unchanged and traditional techniques.
In this case the concept of restoration is indistinguishable
from that of maintenance, and the meaning of this is maintaining
the object in perfect efficiency (Fig. 2).
Fig. 2 – The Turin’s cathedral facade is made by Foresto white marble.
These philosophies are obviously so different but they both
take care of the same important question: the conservation of the
artwork. In the first case the safeguard of the work is obtained
through the preservation of original material which was made,
even if we can maintain just an approximate or partial image; in
the second case, the safeguard passes through the idea of
preserving the image obtained by the renewing of the material it
is made.
We touch in this opposition one of the deeper meanings
compared to the nature of stone and particularly for the
architectural stone. From one side the idea of design and
composition is represented by a drawing and a form; on the other
hand physical aspect of the work which consists of stone material.
Better and longer you keep the material, longer be keep the
artwork as a model. In western civilization these concepts are
often exchanged and reversed. When we think that Medieval and
Renaissance architects began their training working as
stonecutters, we can imagine how important was the material with
its specific processes and how important was the stone when they
required the use.
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Architects today, they have an approach less idealized than
once, just because they do not know really and directly the stone.
It's probably that the current dominant thought in relation to
conservation has a common cultural roots with contemporary
designers: the lack of direct knowledge of the stone material
creates a detachment that makes it more difficult to accept the
sacrifice and then the replacement of even one small piece of
stone or marble.
The examples to compare these concepts are many, but we
observe the importance of latest developments in which the two
philosophies have found points of contact to get better results
mediating between theory and needs.
536

Geomechanical monitoring and stress measurements in open pit and
underground marble quarries
Key words: Open pit quarry, displacement monitoring, stress
measurement, stability evaluation .
The mechanization of marble cutting operations thrusts the
enlargement of quarry exploitations. This trend makes necessary
the geomechanical control and computations of the static
condition both at the exploitation workplaces and of the residual
rock structures (HOEK &BRAY, 1981; HOEK &BROWN, 1982;
BRADY &BROWN, 1985; BIENIAWSKI, 1989). Planning of the
investigations is driven by the specific geostructural and
mechanical rock mass characteristics of the quarry sites in respect
to the natural morphology and the excavation geometries. For
instance in open pit quarrying, the monitoring of the structurally
controlled deformation of high excavated rock faces is relevant
for safety and planning of further quarry developments.
The paper reports an experience of monitoring and
computations at an open pit quarry. The quarry site belongs to the
Alpi Apuane marble basin (Carrara marble), where past
exploitation operations left in place a parallelepiped marble spur
≈90 m high, horizontal section ≈ 30×20 m and hosting old drifts
(Fig. 1a). This residual rock structure is intersected by different
rock joints and a sub-vertical large fault located on the back side
of the spur. Evident joint traces appear on the excavation and
drift surfaces, and a monitoring plan was defined which allows to
detect the influence of rock fractures on the deformation
behaviour of the marble spur. Groups of different measuring
devices (1D or 3D crack gages, MPBX extensometers, load cells
and piezometer) were arranged on the surface and in the old drifts
(Fig. 1b) while a wireless transmission system conveys the
measured data to the quarry technical office (DUNNICLIFF, 1993).
Hydraulic fracturing was furthermore applied in two vertical
boreholes located on the two opposite sides of the big fault to
detect the stress condition (HAIMSON, 1993, AMADEI &
STEPHANSSON, 1997).
Computations were made to estimate the influence of the rock
mass structure and of the environmental condition on the static
behaviour of the rock spur. The Block Theory (BT) technique
(GOODMAN & SHI, 1985). was applied to detect potentially
unstable rock blocks defined by rock joint intersections in the
_________________________
(*) Istituto di Geologia Ambientale e Geoingegneria, CNR
giorgio.iabichino@polito.it, masantonio.cravero@polito.it
GIORGIO IABICHINO (*) & MASANTONIO CRAVERO (*)
537
Fault bounding the
mountain side of
the excavated spur
Fig. 1 – (a) The excavated quarry spur; (b) a sketch of the East side.
(a)
(b)
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marble spur (Fig. 2a). FEM modelling, made by using the
commercial software Phase, allowed to clarify the possible role
played by the fault and by different stress or water load
conditions on the deformation mechanism shown by the spur
(Fig. 2b).
The experimental control along with the analysis of unwanted
deformation and rock block instabilities was motivated not only
by the need of controlling the evolution of the displacements, but
also suggested setting up remediation countermeasures against a
possible unstable trend of the marble spur.
REFERENCES
AMADEI B. & STEPHANSSON O. (1997) Rock stress and its
measurement. Chapman & Hall, London, 490 pp.
BIENIAWSKI Z.T. (1989) Engineering rock mass classifications.
Wiley, New York, 251 pp.
BRADY B.H.G. & BROWN E.T. (1985) Rock Mechanics for
Underground Mining. George Allen & Unwin (1 st Ed),
London, 527 pp.
CRAVERO M., IABICHINO G. & GULLÌ D. (2003) Comparative
mechanical characterization of marble by means of
laboratory testing. In: Proc. 12 th Panamerican Conf. Soil
(a) (b)
Fig. 2 (a) Potentially unstable rock block along the edge of the spur; (b) trend of the displacements suggested by a 2D FEM model.
538
Mech. and Geotechn. Eng. & 39 th U.S. Rock Mech. Symp.
MIT – Cambridge (Mass), 473-478.
DUNNICLIFF J. (1993) Geotechnical instrumentation for
monitoring field performance. John Wiley & Sons Inc., New
York, 577 pp.
GOODMAN R.E. & SHI, G.H. (1985) Block theory and its
application to rock engineering. Prentice Hall Inc., London,
338 pp.
HAIMSON B. C. (1993) The hydraulic fracturing method of stress
measurement: Theory and Practice. In: J.A. Hudson (Ed.) –
Comprehensive Rock Engineering Vol. 3. Pergamon Press,
Oxford, 395-412.
HOEK, E.&BRAY, J.W. (1981) Rock Slope Engineering. The
Inst. Min. Metall., London, 381 pp.
HOEK E. & BROWN E.T. (1997) Practical estimates of rock mass
strength, Int. J. Rock Mech. Min. Sci., 34 (8), 1165-1186.

Key words: CaO, dilatometry, limestone, sintering.
INTRODUCTION
The presence of impurities, even in small percentages (1-3%),
plays an important role either on the structure and properties of
limestones or on the process of decomposition-sintering and
consequently on the characteristics of CaO produced.
Owing to the complexity of the system, where many are the
variables involved, as temperature, CO2 pressure (BERUTO et alii
1979), porosity and particle size of the rock (CRIADO &ORTEGA,
1992), is difficult to assess the evolution of the microstructure
using the traditional methods of analysis (TG, XRD SEM). For
this reason it was developed a dilatometric method (BERUTO et
alii, 2010) by which we can get an overall picture of the
decomposition-sinterig process, including the action played by
the impurities.
MATERIALS AND METHOD
Cylindrical samples (6 mm in diameter and 3 mm in length)
were obtained by a block of high-pure Carrara marble and by
blocks of two kind of limestone, using a water-cooled diamondcore
drill. The samples were inserted in thermobalance (Netzch
STA 409, ± 0.1 mg) and heated until 1200 °C (10 °C/min).
Similar cylindrical samples were inserted into dilatometer
(Netzch DIL 402 E) and heated in static air with the same thermal
program of TG. The A limestone is fine-grained (grain-size of 1-
15 μm), slightly recrystallized with opaque minerals in stilolites
(Fig. 1A), instead the B limestone show a coarser texture (grain
size of 50-75 μm) with strong recrystallization (Fig.1B) and the
presence of fluorite and fluorapatite as accessory minerals. Tab. 1
shows the chemical composition of A and B limestones.
_________________________
Decomposition-sintering dilatometer method to study the effect of
limestone impurities on lime microstructure
ALBERTO LAGAZZO (*), RODOLFO BOTTER (*), ROBERTO CABELLA (**) & MARCO LEZZERINI (°)
(*) DiCheP, University of Genoa, Alberto.Lagazzo@unige.it,
Rodolfo.Botter@unige.it
(**) DIPTERIS, University of Genoa, Cabella@dipteris.unige.it
(°) DST, University of Pisa, Lezzerini@dst.unipi.it
539
RESULTS DISCUSSION
The comparison between the thermogravimeter and
dilatometer traces of sample B (Fig. 2), shows three sections: a)
no weight loss and only thermal expansion of the sample, b)
decomposition and loss weight, c) CaO sintering, evidenced by a
change of the dilatometric curve slope, no weight variations.
Fig. 1. – Polarized light micrographs (NX). Photo A evidence the presence of
opaque minerals in stilolites and authigenic albite in sample A; photo B
shows the coarser texture of sample B.
Fig.2 – Thermogravimetric and dilatometric traces of two identical samples
of limestone B.
From the analysis of dilatometric traces of A and B limestone
into the sintering section (Fig. 3), we can observe a higher slope
( β& B=0.0013 ΔL/L0 min) at starting of the process and a larger
shrinkage (ΣB=10.6 ΔL/L0%) of the B sample. (Sample A:
β& A=0.0003 ΔL/L0 min, ΣA=2.2 ΔL/L0%). The presence of
impurities, also if in low quantity, can influence the
decomposition process and then modify the microstructure and
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Tab.1 – Composition of limestones A and B
Sample
CaCO3
(%)
MgO
(%)
SiO2
(%)
Al2O3
(%)
S
(%)
Fe2O3
(%)
A 97.79 0.55 0.58 0.14 0.033 0.062 0.0017 0.0047 0.041 0.144 0.10 0.0052 0.03
B 99.34 0.15 0.05 0.01 0.005 0.029 0.0245 0.0021 0.002 0.124 0.06 0.0052 0.054
the porosity of the lime. Because the degree of porosity is
responsible of sintering rate (RAMHAN et alii, 1991), it is possible
to assume a relationship between the degree of purity and the
sintering rate.
Due to the complexity of the process, it is difficult to
understand all the phenomena that occur, however we can try to
explain the difference in the starting rate considering the packing
of CaO. Indeed, although the particles of lime A are smaller than
the particles of lime B, the lower packing in A slows the sintering
process, because of longer diffusion paths. This starting density is
preserved in the final product (A porosity = 0.30 ml/g, B porosity
= 0.15 ml/g).
The higher sintering rate of lime B is reached as a
consequence of the action of liquid phase due to presence of
Fig. 3 – Comparison of the dilatometer decomposition-sintering curves of A
and B limestones and of high pure Carrara marble.
Fig. 4 – Typical SEM observations on fractured surfaces of the lime A and of
the lime B obtained through an equal decomposition-sintering process:
1200°C for 150 minutes.
540
MnO
(%)
Na2O
(%)
K2O
(%)
SrO
(%)
fluorites, which give rise to eutectics at decomposition
temperature. The solid-liquid mechanism explains the formation
of high-density aggregates, due to dissolution and ricrystallization
of CaO (BERUTO et alii, 1977; Fig. 4). In good agreement with
these hypothesis is the dilatometric curve of pure Carrara marble:
in fact the absence of impurities is symptomatic of slow sintering
rate ( β& Marble=0.0005 ΔL/L0 min), and little shrinkage (ΣMarble=1.5
ΔL/L0%).
REFERENCES
P2O5
(%)
Cl
(%)
F
(%)
BERUTO D.T., SEARCY A.W., FULRATH R.M. & BASU T. (1977) -
Effects of carbon dioxide and sodium chloride on the
sintering of calcium oxide. Lawrence Berkeley Laboratory,
76, 101.
BERUTO D., ERWING J. & SEARCY AW. (1979) - The effect of CO2
pressure on the rate of decomposition of CaCO3 powders.
Lawrence Berkeley Laboratory, 78, 112.
BERUTO D.T., BOTTER R., CABELLA R. & LAGAZZO A. (2010) - A
consecutive decomposition–sintering dilatometer method to
study the effect of limestone impurities on lime microstructure
and its water reactivity. J. Eur. Ceram. Soc., 30, 1267-1286.
CRIADO J.M. & ORTEGA A. (1992) - A study of the influence of
particle size on the thermal decomposition of CaCO3 by
means of constant rate thermal analysis. Thermochim. Acta,
195, 163-167.
RAHAMAN M.N., DE JONGHE L.C. & CHU M-Y. (1991) - Effect of
green density on densification and creep during sintering. J.
Am. Ceram. Soc., 74, 514-519.

The historical marbles in Tuscany:
a proposal of a new method of classification
Key words: Historical marbles, ornamental stones, Tuscany.
This study is a report regarding the Tuscan ornamental stones,
their quality control and commercial opportunities. It is also a
general proposal about the application of a new method to
classify the “historical stones” based on both professional
documents and regional laws concerning the excavation
activities.
Nowadays, according to regional study, the adopted
classification (PRAER – TUSCANY REGION, 2007) is about the
quality and the quantity of historical stone materials. The authors
of this last research confirm that their studies are mostly about the
main lithotypes without considering a specific historic time.
The geologic and petrographic research of BASTOGI et alii
(2004) is a detailed description of the quarries of marbles and
stones used for the main monuments in Florence.
CARMIGNANI et alii (2007) research for the classification of
the different kinds of marble of the Apuan Alps (called “Marble
Project”) defines three classes of historic marbles, even dated of
different geological period of time. These Authors give the
definition of historical marble as those materials with particular
characteristics in colours and drawing that today are not subject
to cultivation like in the past when the materials were quarried
and widely used for decoration and ornamental purposes.
The research activity of the Regional Board of the PARCO
DELLE ALPI APUANE (2002) seems to be an exhaustive and
careful examination of historical stone materials of the Apuan
Alps area, also including the stones that today are quarried in a
very low quantity. It is also a proposal for extending their use in
historical or new buildings.
These studies suggest that the definition of PRAER (2007)
can have a large use and that of the “Marble Project” of the
Tuscany Region is more restrictive. A different definition of
“historical marbles” can be found in the studies mentioned above,
considering also the differences between the periods before and
after the industrial revolution.
The more recent research of the Regional Board of the
_________________________
(*) Centro di Geotecnologie dell’Università di Siena San Giovanni
Valdarno (AR)
SERGIO MANCINI (*)
541
PARCO DELLE ALPI APUANE (2002) includes in the definition of
“historical marbles” the following four elements: 1) ancient
quarrying methods, 2) consolidated fame, 3) cultural renown and
4) low quantity of material.
In the period between 1995 and 2007, a classification of
quarries of ornamental stones and marbles was adopted in
Tuscany. Such classification is valid still today.
There are some researchers in Italy such as BADINO et alii
(2001) and FILIPELLO et alii (2008) that take in large
consideration the historical period of excavation, the activity and
the kind of materials/marbles.
Table 1 – The proposal of a new method of classification.
Kind of quarry Quarrying method Quarrying period
Ancient quarry Manual excavation Roman era
until the year 1000
Historical quarry
(type A)
Manual excavation 1000 - 1600
Historical quarry Manual excavation - 1600 -1847(°)
(type B) explosive excavation
Historical quarry Explosive charge
(type C) without helical wire
Modern Quarry Explosive charge
with helical wire
Contemporary quarry Diamond wire
and chain cutter
1847 – 1895(*)
1895 - 1980
After 1980
(°) referring to the first usage of black powder and other kind of explosive
charge like the nitroglycerin in the quarring;
(*) referring to the first usage of the helical wire in the quarries of Carrara.
The new method of classification is based on the theories of
these researches and work out a detailed analysis of different
elements.
a) The geological reserve is an analysis of the quantity of
blocks, which can be used. To cultivate ornamental stones
according to contemporary industrial criteria, we have to consider
the necessary average dimensions of blocks for their
transformation during the cycle by the multiblade gangsaw, with a
range of the bench minimum height from 1.70 to 3.00 meters and
with commercial block dimension of 2.50 × 1.30 × 1.50 m 3 .
b) The so-called “block recovery” is the percentage of
ornamental stone quarried and still rough. Nowadays, this
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parameter is adopted for a classification of the quarry’s
excavation with a minimum percentage of “block recovery” of
25%, according to PRAER 2007 of the Tuscany Region.
c) The historical classification of quarries.
This proposal of classification (Table 1) should give the
opportunity to realize a detailed and complete research either of
quarries, historical marbles (starting from the “geological
reserve” and its cultivation) or in general of other stone materials,
particularly worthy, whose cultivation is planned in order to
quarry the quality amount and not the quantity one.
REFERENCES
BADINO V., BOTTINO G., BOTTINO I., FORNARO M., FRISA
MORANDINI A., GOMEZ SERITO M. & MARINI P. (2001) –
Valorizzazione delle risorse lapidee del bacino estrattivo dei
marmi del Monregalese – Geam Ed., 38, 97-108.
PARCO DELLE ALPI APUANE (2002) – Piano per il Parco.
Allegato Attività Estrattive – relazione illustrativa, 38 pp.
BASTOGI M. & FRATINI F. (2004) – Geologia, litologia, cave e
deterioramento delle pietre fiorentine, Mem. Descr. Carta
Geol. d’It., 66, 27-42.
FILIPELLO A., FORNARO M. & GIULIANI A. (2008) – Nuova
metodologia di analisi per la valutazione speditiva della
qualità dei giacimenti di pietra ornamentale e dei blocchi
estraibili. Giorn. Geol. Appl., 8, 67-74.
CARMIGNANI L., CONTI P., FANTOZZI P., MANCINI S., MASSA G.,
MOLLI G. & VASELLI L. (2007) – I marmi delle Alpi Apuane –
Geoitalia, 21, 19-30.
PRAER – TUSCANY REGION (2007) – Piano regionale delle
attività estrattive di recupero delle aree escavate e di
riutilizzo dei residui recuperabili – Allegato F, Settore II -
Materiali Storici, 108 pp.
542

Mineral resources and economic availability of Industrial Minerals
and Rocks in Italy
Key words: Industrial Minerals and Rocks deposits, geology,
Italy, economic availability.
INTRODUCTION
The established trend towards a general retreat of the mining
industry in Western Europe is accentuated by the present phase of
worldwide suffering of markets. Nevertheless, Italy remains a
significant player in the global mineral economy, occupying an
important role as supplier and major consumer of numerous
mineral commodities. In particular, the country is a leading
European and world producer of Industrial Minerals and Rocks
(IM) as feldspar (Italy is the 2 nd world producer, with about 25%
of the world output), bentonite (4% of world output), silica sands,
pumice, lime, cement (U.S. GEOLOGICAL SURVEY, 2007). Other
commodities, like olivine, dolomite, talc, rock salt, fluorspar,
ceramic clays, kaolin, perlite, zeolites, also are considerable as
productions or reserves. Therefore, IM resources still play an
important role in the national industry, while their exploitation is
focused to supply selected productive sectors, as those of
ceramics and glass industries (feldspar, talc/steatite, clays, silica
sands), clay minerals applications, metallurgical uses (olivine,
dolomite, refractory clays, bentonite, silica sands), paper, plastics
and paints industries (talc, kaolin, GCC), chemicals (fluorite),
constructions. In the following review, unless otherwise specified,
all production data come from WILSON (2007).
ITALIAN GEOLOGY AND IM DEPOSITS
The Italian territory is characterised by great geological variety,
hosting several IM resources. However, due to the geology and
size of the deposits or to the quality of the ores, a limited number
of them are economic and really suitable to mining. In the Italian
districts, the age of different IM deposits ranges from Palaeozoic
to Holocene: Western and Southern Alps, the Northern
_________________________
(*) Dipartimento di Scienze della Terra - Università di Cagliari,
marinic@unica.it
(**) Dipartimento di Geoingegneria e Tecnologie Ambientali – Università
di Cagliari, snaitza@unica.it
(°) Gruppo Minerali Maffei , Novara
CARLO MARINI (*), STEFANO NAITZA (**) & FABIO GRANITZIO (°)
543
Appennine, the Magmatic Provinces of Central Italy, the
Southern Appennine, the Paleozoic basement and the Cenozoic
volcanic province of Sardinia, are the most important geotectonic
settings, in terms of quantity and quality of deposits and
occurrences.
Western Alps. The Western Alps include several significant IM
deposits, mainly hosted in metamorphic Penninic units and in
Permian volcanic covers. The Boca mine (100000 tpa of
capacity) and the mine of Alagna Valsesia (50000 tpa) are
relevant sources of feldspars for ceramics and cement. The
Alagna mine exploits the Mud di Mezzo oligoclase-quartz-mica
aplitic gneiss of the Monte Rosa; the Boca mine exploits the Boca
rhyolite, a quartz-feldspatic volcanite part of the Early Permian
Biellese quartz-porphyry volcanic complex. In Lozzolo, SW from
Boca, altered pyroclastics of the same complex host ball and
ceramic clays deposits, exploited by the ACDAL mine (200000
tpa) and destined to tile production. In Western Piedmont, the
only active mine in the Val Chisone/Valle Germanasca talc
district of the Dora Maira cristalline massiff is Rodoretto (30000
tpa of high quality talc; http://www.talcovalchisone.com); the
deposit consists of several talc lenses at the contact between
calceschists and gneiss/micaschists units. Talc production is
mostly finalised to cosmetics, fillers and ceramics markets. The
Valmalenco talc/steatite deposits (grey talc), in the Penninic
nappes of Lombardy (55000 tpa of talc-chlorite in the Brusada-
Ponticelli mine), belongs to a different geological setting,
including a sequence of Mesozoic anfibolites, serpentinites, and
metamorphosed dolomitic limestones. In the San Lorenzo quarry
in Valdieri ground calcium carbonate (GCC) for fillers (30000
tpa) is produced from the Cretaceous marbles of the autochtonous
sedimentary complex of the Argentera massiff. Gypsum is
quarried in deposits from Messinian evaporites of the Monferrato
tertiary basins, as in the Moncalvo area (90000 tpa).
Central and Southern Alps. The southern part of the Alpine belt
hosts a relatively short number of IM active mines. The Vidracco
mine, in Piedmont, (250000 tpa) is the primary source in Italy of
olivine for refractories and abrasives. It exploits the Bric Carlevà
peridotite, which belongs to the Ivrea Zone. An important source
of raw materials for glass and ceramics is the ECOMIN plant in
Verbania, which treats about 300000 tpa of granite scraps
deriving from ornamental stone quarrying in Baveno and
Montorfano, to obtain a quartz-feldspathic sand concentrate. In
the Central Alps (upper Valtellina Valley), the Sondalo
underground quarry exploits hydrothermal quartz in a quartzdiorite
part of the Sondalo gabbroic complex; the production is
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60000 tpa. Near Marone, East of the Iseo Lake, 400000 tpa of
dolomite for refractories are extracted in the Calarusso quarry,
which exploits Late Triassic dolostones. The main GCC
producers of the area operate near Vipiteno (50000 tpa,),
extracting and processing Permian marbles from Val Racines.
Northern Appennines. This composite geotectonic region hosts a
limited number of IM resources, even though in the area are
present several first-order raw materials consumers, as the
Sassuolo ceramics district. Amongst the most important resources
are the Liassic marbles of the “Autoctono” metamorphic unit of
the Alpi Apuane. GCC is obtained from marble scraps processed
in the Massa and Carrara ornamental stone district; the
production capacity is very high, reaching 2000000 tpa, mainly
addressed to fillers markets. Important feldspatic rocks are near
Campiglia Marittima (Botro ai Marmi mine) and in the Elba
island (La Crocetta mine), where sericitised porphyritic aplites of
Miocene-Pleistocene Tuscan Magmatic Province are mined.
Productions in Campiglia Marittima are 150000 tpa, while in La
Crocetta assessed reserves are >10Mt
(http://www.euritonline.com/). Also in southern Tuscany, a
primary kaolin deposit, hosted in Tertiary hydrothermalized
rhyolites, is mined in the Piloni mine, near Roccastrada; the
mineable ore is estimated >15Mt (http://www.euritonline.com/).
Magmatic Provinces of Central Italy, Southern Appennines and
Sicily. Feldspars, GCC, rock salt, kaolin, silica sands, pumice,
zeolites, are the main exploited IM resources in this large area. In
the Paleozoic of the Calabrian arc, feldspars are mined from
Paleozoic basement in the Sila region: sodic-potassic feldspars
from aplites hosted by gneiss and Variscan granites in the Sorbo
San Basile area (175000 tpa; http://www.gruppofimed.it), sodic
and sodic-magnesic feldspars in Variscan pegmatites in Acri
(100000 tpa; http://www.gruppofimed.it). After the recent closure
of the Lipari island quarries in Sicily, the Italian pumice
production is focused in Central Italy, close to the Bolsena lake,
with quarries that operate in the Pleistocenic pyroclastic
sequences of the Vulsini volcanic complex; other pumice,
lapilli/scoriae, and chabazite zeolitite deposits are quarried in
Tessennano and Monte Cellere (Viterbo). Total production from
this area is >200000 tpa. Kaolin is extracted from
hydothermalised pyroclastics of the Bracciano volcanic complex
in the Santa Severa Nord mine; production is 55000 tpa. Central
and Southern Italy main GCC productors are located in Gualdo
Tadino, Nocera, Avezzano, Caserta; each plant processes
limestones or marbles, with capacities >100000 tpa. Silica sands
are quarried from quaternary deposits in the Priverno/ Fossanova
area, East of Latina (300000 tpa). Rock salt is at the present the
most important IM resource of Sicily: huge salt deposits are part
of the Late Miocene evaporites of the “serie gessoso-solfifera”
and are exploited in the Racalmuto, Petralia and Realmonte
underground mines, with a total production of the district of
about 1500000 tpa (http://www.italkali.com).
Sardinian block. Sardinia IM productions are the largest in Italy,
including feldspars, silica sands, talc, ceramic clays, bentonite,
fluorite, perlite (MARCELLO ET ALII, 2008). In the Paleozoic
basement of Central Sardinia, the Orani-Ottana district is the first
544
source of feldspars for the ceramic and glass industries of Italy.
Sodic and sodic-magnesic feldpars are extracted from albitised
Variscan granitoids and pegmatites, being part of the 30-km long
Central Sardinia albitite belt. The Ispaduleddas mine reach a
capacity > 600000 tpa. Other feldspar resources are the plant in
Buddusò (30000 tpa), which processes leucocratic monzogranite
scraps, and the San Simplicio mine in Siniscola (45000 tpa), that
exploits Ordovician porphyroids. In the Orani area, talc/chlorite
deposits are hosted at granitoids-metamorphic basement
(phyllades, marbles) contact; the deposits are exploited in the Sa
Matta mine (30000 tpa). In Southeastern Sardinia basement, the
Silius mine exploits late Variscan fluorspar veins hosted by lowgrade
metamorphites; production capacity is 80000 tpa. In the
Central Sardinia Sarcidano district, secondary ceramic clay
deposits hosted in Jurassic sequences are exploited (about
100000 tpa) only in the Funtana Piroi mine (Escalaplano).
Several large bentonite deposits are included in Cenozoic
pyroclastic sequences of Western Sardinia; the most relevant
deposit is S’Aliderru, East of Alghero, that produces 200000 tpa
of Ca-bentonite. Several other deposits are located in Busachi
area (100000 tpa) and in Southern Sulcis (Giba). The largest
deposits of silica-feldspatic sands in Italy are located in NW
Sardinia, in the Late Miocene sedimentary sequence of Logudoro.
The Florinas mine has a capacity >750000 tpa of quartz and
feldspar concentrates; kaolinitic clays are also recovered. Perlite
is mined in the Plio-Pleistocenic rhyolites of the Monte Arci
volcanic complex.
ISSUES AND CONCLUSIONS
If the current economic downturn seems to prefigure, in Europe, a
period of declining demand for raw materials, there is always a
strong dependency of entire sectors of the national and European
industry from the supply coming from the Italian poles of IM
extraction. Reserves in the Italian IM deposits are in general, in
the key sectors (feldspars, silica sands, GCC, etc. ), very good
and certainly enough to feed the needs of industry for many years,
however a major effort must be done in the research of new
technological applications for known mineral resources, in the
rationalization and improvement of mining and processing, and in
the definition of the economic potential of new resources .
REFERENCES
TOCCO S., MARCELLO A., MAZZELLA A., NAITZA S., PRETTI S.,
VALERA P. & VALERA R. (2008) La Carta Metallogenica e
delle Georisorse della Sardegna in Scala 1: 250.000. LAC,
Firenze.
U.S. GEOLOGICAL SURVEY (2007). Minerals Yearbook – Italy 7
pp. , http://minerals.usgs.gov/minerals/pubs/country/2007/
WILSON, I (2007). Minerals of Italy: built to last. Industrial
Minerals 479, 32-42.

Key words: Dimension stone, Egypt, geo-mechanical analysis,
structural geology, Tunisia.
The detailed geological study is fundamental as a preparatory
phase in order to assess the volume of the deposit and correctly
address the future exploitation of a dimension stone quarry. In the
same way, detailed geological and geo-mechanical analyses in
already active quarries represent an essential tool to delineate
deposit extensions, to drawn up the exploitation front direction,
to locate new varieties and to define the geological situation and
the possible features that impedes the correct exploitation of the
material giving the hints to increase productivity.
Detailed geological-structural survey consists of ductile and
fragile structural studies, stratigraphic and tectonic analyses. All
the data coming from these studies are acquired with several
technologies and allow to fully describe the geological setting of
the quarry area through a geological model. The geological
model must reproduce the three-dimensional geometry of a
terrain portion giving the spatial relationships between
lithologies, faults, bedding surfaces, etc. These techniques are
crucial especially in the dimension stone quarrying for defining
the discontinuities framework in the rock mass and for knowing
which is the medium dimension of the blocks that could be
exploited in a certain area. Moreover, using this kind of study it is
possible to optimize further detailed investigations such as
drilling campaigns and geophysical surveys.
The data collected on the field are transferred in a
computerized database and then elaborated through geo-spatial
software and documented as maps (2D and 3D) and with geostatistical
diagrams. The definition of the geological model is the
basis for any project concerning the interaction with the territory
and quarry activities, and if properly built could guarantee the
success in terms of production and economic savings.
Here we want to show the potentialities of the detailed
geological field analysis through the case studies of some
dimension stone quarries from Egypt and Tunisia. These areas
_________________________
(*) Geofield srl, www.geofield.it
The detailed geological field analysis as a powerful tool
for deposit evaluation and quarry development:
case studies from Tunisia and Egypt
SERGIO MATTEOLI (*), GIUSEPPE NIRTA (*) & ELISA LIVI (*)
545
represents different geological situations and, as a consequence,
different ways to approach the construction of the geological
model. As a main rule: the more complicated is the geological
situation, the more detailed must be the description of the
geological features.
As proved in this study, the transposition of the requirements
of the geological study in quarrying activities results in a more
correct excavation of the material with the proper technology and,
in the short to medium term, in a lowering of the production costs
and an increasing of the productivity.
SESSIONE 16

SESSIONE 16
Key words: Ammonia removal, chabazite, ionic exchange,
phillipsite, zeolites.
INTRODUCTION
In the last decades experimental studies for ammonia removal
from water increasingly improved.
In Italy, the limit value for NH4 + concentration in sewage
waters is 15 mg/l (L. 319/76). Higher concentration values might
be detected in natural superficial waters, mainly due to the
agricultural use of the land. Ammonium compounds are
characterised by an extreme solubility in the presence of water;
for this reason their removal requires complex treatments:
biologic treatments (nitrification and denitrification,
biodegradation), chemical treatments (oxidation, chlorination),
chemical-physical treatments (ionic exchange) (POLLICE et alii,
2002; SPRYNSKYY et alii, 2005).
The most common option for ammonia removal is represented
by the break point chlorination. Even if effective, it must be
observed that water treatment with this method led to the
formation of organic-halogen compounds characterised by
cancerous effects.
As far as chemical-physical treatments are concerned, zeolites
are nowadays referred as ideal materials (BARRER, 1987).
Application of zeolites in water purification processes is based on
the high affinity of these minerals towards cations which are
substituted into their structure by means of ionic exchange
processes. This property, known as selectivity in ionic exchange,
is well testified for clinoptilolite, phillipsite and chabazite and
other zeolites, showing these minerals a high affinity for the NH4 +
ion (PARK et alii, 2002; SARIOGLU, 2005; WEATHERLEY et alii,
2004). For this reason zeolites are nowadays preferred above
synthetic resins, for which ionic exchange is instead not a
selective property.
_________________________
Experimental results from a pilot plant for the ammonia removal
from superficial waste waters by the use of an
Italian volcanic zeolitite
DANIELA NOVEMBRE (*), DOMINGO GIMENO (**) & BRUNO DI SABATINO (*)
(*) Dipartimento di Geotecnologie per l’Ambiente ed il Territorio,
Università D’Annunzio, Chieti, dnovembre@unich.it.
(**) Departamento de Geoquimica, Petrologia i Prospeccio Geologica,
Universitat de Barcelona, (Spain), domingo.gimeno@ub.edu.
546
Italian pyroclastic rocks, like the “Tufo Giallo Napoletano”
and “Tufo Rosso a Scorie Nere”, containing chabazite and
phillipsite, are usually been tested for the ammonia removal from
sewage urban waters, leather industry waters, zootechnical
farming, aquaculture and water purifying (CIAMBELLI et alii,
1988a; CIAMBELLI et alii, 1988b; COLELLA &AIELLO, 1988; LIN
et alii, 1986).
In this paper we test the efficacy of an italian tuff zeolitized at
chabazite (and secondarily phillipsite), i.e. the “Tufo Rosso a
Scorie Nere”, coming from the Latial Province (Italy), in the
ammonia removal from sewage waters. Preliminary experiments
based on continuous column process were performed in
laboratory to test the efficacy of the zeolitite in the pollutant
removal and indicated a real CEC (cation exchange capacity) of
1.5 mg/l (Fig.1).
Fig. 1 – Characteristics of the zeolitite.
AMMONIA REMOVAL AT FOSSO SAN GIUSTINO
Pollution at the Fosso San Giustino (Chieti, Central Italy)
course is mainly due to unauthorised dumping of waste waters by
the neighbouring built-up areas which spill pollutants in this
course even if a purification plant is present at a very short
distance. The main pollution is represented by the accumulation
over the law limit of ammonia.
A ten months long campaign started at Fosso San Giustino
during which the effluent undergone periodical controls and
measures of lot of chemical parameters such as concentration of

ammonia, nitrates, nitrites, clorures, calcium, sodium, potassium
and magnesium. Also physical parameters, such as pH,
conductivity and temperature, were periodically monitored. The
mean value of flow rate along the water course has been
calculated in 0.4 l/sec and the NH4 + input values ranging between
5 and 120 mg/l.
A laboratory preliminary study finalised to determine the
efficacy of a Latial zeolitite in the ammonia removal was
NH4+ (mg/l)
130
120
110
100
90
80
70
60
50
40
30
20
10
0
sept-2
sept-16
clear dirty law limit
conducted and resulted in a column system test. The induced flow
rate was of 0.4 l/sec, being this the mean flow rate value
measured at Fosso San Giustino over a ten long period. By
analysing the results of the breakthrough curve, it results that the
system saturates in a long period, about 110 h, which correspond
to the passage of about 80 l of water. Taking into account these
findings and the geometry of the Fosso San Giustino water
course, a total amount of 25 m 3 of zeolitite was preventivated to
be necessary to guarantee ammonia removal under the limit laws
over a ten months long period. According to these preliminary
evaluations, a pilot plant was established at Fosso San Giustino
effluent; a zeolitite bed 20 cm in height was positioned on a
portion of 70 m in length and 70 cm in width of the effluent and
seven zeolitic beds were positioned along the effluent and
intercalated by decantation and homogenization baths. The
results of the ammonia removal campaign indicated an effective
efficacy of the zeolitite and a positive ammonia reduction of
about 80/90%. NH4 + concentration values always resting under
the law limit (Fig.2).
Results for clear water indicate NH4 + values under 10 mg/l,
very often ranging between 1 and 5 mg/l.
REFERENCES
sept-30
oct-14
oct-28
nov-11
nov-27
dec-09
dec-24
dec-29
gen-14
gen-28
feb-13
feb-27
mar-13
mar-26
may-12
june-01
july-11
Fig. 2 – Ammonia removal expressed as variation in Nh4 + (mg/l) during the
period September-July.
BARRER R.M. (1987) Zeolites and clay minerals as sorbent and
molevcular sieves. Academic Press, New York, 497 pp.
547
CIAMBELLI P., CORBO P., LIBERTI L. & LOPEZ A.. (1988a) -
Ammonium recovery from urban sewage by natural zeolites.
In: B. Drzay, Hocevar and Pejonic (Eds.) - Zeolites: synthesis,
structure, technology and application. Elsevier, 501-509.
CIAMBELLI P., CORBO P., LIBERTI L., & LOPEZ A. (1988b) -
Ammonia removal from municipal water by phillipsite. In: B.
Drzay, S. Hocevar and S. Pejovnik (Eds.) - Zeolites:
synthesis, structure, technology and application. Elsevier,
539-546.
COLELLA C.& AIELLO R. (1988) Ammonia removal from tannery
sewage by selective ion exchange using natural phillipsite. In:
D. Kallo and H.S. Sherry (Eds.) - Occurrence, properties and
utilization of natural zeolites. Akademiai Kiado, 491-500.
LIN S.H. & VU C.L. (1996) Electrochemical removal of nitrite
and ammonia for aquaculture. Water Res., 30, 715-721.
PARK J.-B., LEE S.-H., LEE J.-W., & LEE C.-Y. (2002) Lab scale
experiments for permeable reactive barriers against
contaminated groundwater with ammonium and heavy metals
using clinoptilolite. J. Hazard. Mater., 95, 65–79.
POLLICE A., TANDOI V. & LESTINGI C. (2002) Influence of
aeration and sludge retention time on ammonium oxidation to
nitrite and nitrate. Water Res., 36, 2541–2546.
SARIOGLU M. (2005) Removal of ammonium from municipal
wastewater using natural Turkish (Dogantepe) zeolite. Sep.
Pur. Tech., 41, 1–11.
SPRYNSKYY M., LEBEDYNETS M., TERZYK A.P., KOWALCZYK P.,
NAMIES´NIK J. & BUSZEWSKI B. (2005) Ammonium sorption
from aqueous solutions by the natural zeolite
Transcarpathian clinoptilolite studied under dynamic
conditions. J. Coll. Interf. Sci., 284, 408–415.
WEATHERLEY L.R. & MILADINOVIC N.D. (2004) Comparison of
the ion exchange uptake of ammonium ion onto New Zealand
clinoptilolite and mordenite. Water Res., 38, 4305–4312.
SESSIONE 16

SESSIONE 16
Synthesis of sodalite from natural kaolinite:
a way to simulate the loss in weight of chlorine during the synthesis
process by an analytical and mathematical modeling
Key words: Kaolinite, infrared analysis, mathematical modeling,
sodalite.
SODALITE SYNTHESIS
Sodalite, [Na4(AlSiO4)3Cl]2, can be defined as a crystalline
microporous material whose structure is characterized by a
tetrahedral network displaying enclosing voids of at least 2.5 Å in
diameter. The extreme similarity of sodalite with low silica
zeolitic minerals (i.e., Na-X, Na-P, Na-A zeolites) justifies the
great interest in sodalite synthesis processes, carried out at
industrial scale not only to investigate the crystal structure of the
mineral, but especially to explore its properties in environmental
fields like waste water purification through cationic exchange
processes, molecules absorption etc.
Kaolinite has just been attested in the past as the preferred
material for sodalite synthesis (DE-CHANG et alii, 2004). Reports
of sodalite synthesis from metakaolin under high temperature and
in absence of water are extremely rare (TOMISAKA &EUGSTER,
1968).
Transformation of metakaolinite to basic sodalite in presence
of NaCl was here investigated. Experimental synthesis was
performed in alumina crucibles at 850°C and ambient pressure.
Reaction progress was monitored by X-ray powder diffraction
from 1 h to 400 h. During the crystallization of sodalite, the
presence of reacting residual halite was testified throughout the
run synthesis; intermediate-phase carnegieite was detected in the
initial stage of the synthesis run (1 h 24 h). Both sodalite and
residual halite were evidenced between 24 and 101 h, where
sodalite reaches a climax in the crystallization degree.
Progressive replacement of sodalite by nepheline was testified
_________________________
(*) Dipartimento di Geotecnologie per l’Ambiente ed il Territorio,
Università D’Annunzio Chieti (Italy), dnovembre@unich.it.
(**) Dipartimento di Scienze, Università D’Annunzio Chieti (Italy),
apasculli@unich.it.
(°) Departament de Geoquímica, Petrologia i Prospecció Geològica,
Universitat de Barcelona, (Spain), domingo.gimeno@ub.edu.
DANIELA NOVEMBRE (*), ANTONIO PASCULLI (**), CARLA PACE (*),
DOMINGO GIMENO (°) & BRUNO DI SABATINO (*)
548
starting from 171 h. Synthesized sodalite was submitted to
chemical-crystallographical and mineralogical-textural studies
and Infra-Red Spectrometry (IR), providing values comparable to
the ones available in the literature on this mineral. A continuous
loss in weigth of the NaCl plus metakaolinite starting matrix
contained in the alumina crucible heated in oven was testified and
attributed to Cl vaporization.
LOSS IN WEIGHT OF CHLORINE
An analytical mathematical model to solve the parabolic
differential equation related to the chlorine diffusion processes
occurring within the crucible is proposed.
Lost in weight of the initial mixture was measured over time
taking into account the contribute given to this process by
systematic samplings. As initial and simplifying hypothesized
model, it was assumed that all the Cl atoms were free to diffuse
through the NaCl plus kaolinite matrix mixture contained in the
crucible. This hypothesis also implies a second assumption: the
entire matrix of NaCl molecules was at a temperature over that of
Cl ionization since from the time the transient (and the
consequent set of experimental measures) started.
Bearing in mind these considerations, we applied the
following diffusion equation:
weight lost (g)
2,5
2,0
1,5
1,0
0,5
experimental data and analytical results
experimental data
numerical results:
[D] =m 2 /s
D =1.1x10 -9
D =1.5x10 -9
D =2.0x10 -9
D =2.5x10 -9
0,0
0 100 200
time (hour)
300 400
Fig. 1 – Mathematical modeling of the chlorine loss.

∂C
= ∇ ⋅ ( D: ∇C)
+ q&
( r,
τ)
(1)
∂τ
where C is the mass concentration of Cl inside the crucible; τ is
the transient time, D is the diffusion coefficient tensor; q& ( r,
τ)
is
the mass source depending, in general, on the position r and on
transient time τ . In order to apply an analytical approach, we
assumed the following simplified statements:
instead of the diffusion tensor D, a constant scalar D is
considered;
cylindrical coordinates are selected around the crucible axes;
as a first step the totality of the diffusing material (Cl) is
considered available from the start of the transient, so q & = 0.
From the previous assumption it yields:
where ( , , x)
2
2 2
∂C
⎛ ∂ C 1 ∂C
1 ∂ C ∂ C ⎞
= D⎜
⎟
⎜
+ + +
2
2 2 2
∂τ
⎟
⎝ ∂r
r ∂r
r ∂φ
∂x
⎠
(2)
r φ are the cylindrical coordinates ( x = h is the
height of the crucible). The Cl atoms are assumed to diffuse only
through the interface between the NaCl plus kaolinite mixture and
the oven environment. The counter-pressure due to the Cl atom
gas in the oven environment is supposed to be negligible:
C ( x = h,
τ)
= 0.
Furthermore the base ( x = 0.
) and lateral
surfaces are supposed to be impermeable; thus, in particular it
∂C
yields: = 0.
Other important assumptions, related to the
∂x
x=
0
previous discussion, were then introduced. During the entire
transient, an uniform concentration of Cl atoms on surfaces
orthogonal to x axis and a radial symmetry are supposed. Thus
the following 1D simplified initial-boundary problem yields:
The solution of (3) is:
C(
x,
τ)
=
∑ ∞
n=
0
( 2n
+ 1)
2
⎧ ∂C
∂ C
⎪ = D 2
⎪
∂τ
∂x
⎪ ⎛ ∂C
⎞
⎨ ⎜ ⎟ = 0.
⎪ ⎝ ∂x
⎠x
= 0
⎪ C(
x = h,
τ)
= 0.
⎪
⎩C(
x,
τ = 0)
= C0
e
⎡
( −1)
⎤
(3)
n
2
−λ
n Dτ
⎢2
⎥ ⋅C
0 ⋅cos(
λn
x)
(4)
L ⋅λ
n
⎢⎣
where λ n =
2L
π
, n = 0,
1,
2,
3...
are the Eigen values
associated to Eigen functions λ x)
. In order to evaluate the
cos( n
mass of Cl released from the system during the transient, the
integration of concentration C( x,
τ) into the volume of the
⎥⎦
549
crucible, whose shape was assumed as a truncated cone, was
performed. Fig. 1 shows the comparison between experimental
data and the results obtained by varying values of diffusion
coefficient D in the expression of the integration of
concentration C( x,
τ ) . After about 120 hours, the best results
−9
2
were obtained with D = 2.
5 × 10 m / s . Before that time,
however, lower diffusion coefficient values are more
suitable to match experimental measures (work in progress). For
example, the complete availability of all Cl mass is not guaranteed
as the temperature inside the crucible is probably not
homogeneous, i.e. each point does not simultaneously reach
temperature values over the critical temperature to allow the
ionization of Cl in NaCl molecules.
REFERENCES
DE-CHANG,L.,XIAO-WHEN,X.,FENG,Z.&YING-CAI L. (2004)-
Crystallization of JBW, CAN, SOD and ABW type zeolite
from transformation of meta-kaolin. Micropor. Mesopor.
Mater., 70, 63-70.
TOMISAKA T. & EUGSTER H.P. (1968)- Synthesis of the sodalite
group and subsolidus equilibria in the sodalite-noselite
system. Mineral. J., 5, 249-75.
SESSIONE 16

SESSIONE 16
State of the art of the dimension stones sector in Italy. A synopsis
Key words: Installation, processing, quarrying, standards.
The note provides a synthetic overview on the current “state
of the art” in the dimension stone sector. The following main
themes are dealt with:
- quarrying technologies;
- processing technologies;
- installation and application tendencies;
- standards.
QUARRYING TECHNOLOGIES
Increasing application of the dry cut, both with diamond wire
and chain saw machines. No relevant technological advances,
with the exception of the adoption of safety, automation and
environmental devices. Chain saw, in particular, is available in
many different versions, for primary cuts (arms up to 8,2 m) and
squaring phase. The traditional pneumatic perforation is being
progressively replaced by the hydraulic system. Expansive mortar
is also increasing as detachment system. Less and less used the
water-jet, flame-jet and multidrill technologies.
PROCESSING TECHNOLOGIES
As a general remark, there is an increasing adoption of the
NC, even on the simplest machines and equipments. Numerically
controlled machines are more and more accessible, more
intuitive, thanks to the philosophy “entry-level”
adopted by many machineries constructors.
- Primary cutting: stabilization of the gang-saw size (up to
7,50 m for granites) with the hypothesis to introduce the titanium
grit as abrasive. Relatively slow, but constant, growth of the
multiwire plants (up to 85 wires); not yet a technology replacing
the traditional gang-saw, but a complementary one.
- Secondary cutting: worth mentioning the diversification and
development of the bridge cutting machine, with its evolution
from simply trimming unit to a multipurpose machine
- Surface finishings: to be underlined the impressive growth
_________________________
(*) Dimension Stone International Consultant – Docente incaricato Facoltà
di Ingegneria, Università di Bergamo, pieprima@gmail.com
PIERO PRIMAVORI (*)
550
(conceptual and productive) of the plants for resin application but
also the relevant diffusion of the water-jet surfaces (very
welcome in the new design applications of the stone). Significant
development are registered also in the equipments for semiindustrial
and industrial mosaics manufacture, as well as in the
brushing process.
- Special jobs: the borderline among the “traditional”
contouring, shaping, profiling machines and the so-called
“working centres” is less and less clear and many machines can
nowadays perform a relevant amount of tasks. “Mixed” machines,
units capable to do two, at most three, specific jobs, are
increasing their diffusion. New water-jet equipments are being
introduced in the market with pressure-system up to 6.200 bar
and 5 controlled axis..
- A new concept of surface finishing has been created, far
enough from the traditional ones: introduction of the terms
“texture” and/or “skin” to define something no longer created
solely as a cortical modification of a previously cut surface, but
generated from the start as form and volume as well as surface.
Nanotechnologies applications are starting (e.g.: nano-silica;
nano-titanium dioxide; nano-montmorillonite), mostly for surface
treatments (e.g.: consolidation; water-proofing; anti-bacteria
surfaces; elimination of polluting substances etc.) and
amelioration of stone’s technical properties, but also for
production of industrial super-abrasives (CVD, Chemical Vapour
Deposition).
INSTALLATION AND APPLICATION TENDENCIES
Progressive reduction of the slabs thickness.
Composite materials: the stone combined with other materials
(2.5 ÷ 6 mm) for indoor applications, such as internal
diaphragms, suspended roofs, illuminated elements, interior
elements for vessels and yacht, but also for (less common)
outdoor application. Different types of support, such as
honeycomb, “birdwing”, polystyrene, polycarbonate, glass.
Translucency.
“Re-discovery” of the structural use of the stone, with
examples of pre-stressed and pre-compressed granite elements.
Application of industrial mosaics and elements with (quite)
complex forms.
Recent introduction of PCM (Phase Change Materials – latent
heat storage) as a coating of the stone, to improve its thermal
properties.

A brief mention will also be dedicated to the increasing
application of the ventilated façades, to the green building
movement and related adoption of certification protocols, and to
the overall position of the natural stone in terms of sustainability
both as an industry and as a building material.
STANDARDS
Besides the norms and standards regulating the quarrying
activities, the safety + hygiene aspects in the working places and
in machineries’ production (recent introduction of the Machines
Directive 2006/42/CE), it is worth mentioning the future new
structure of the Directive CPD-89/106/EEC “Construction
Products” which will become a CPR (Construction Products
Regulation). Its new status implies two crucial points:
- it will be effective in each EU-Member State without
requiring the decrees of incorporation;
- it will contain one additional Essential Requirement (the 7th,
besides the existing six), related to sustainability (“sustainable use
of the natural resources”).
As far as the CE marking application is concerned, the note
examines the current position of the Italian companies, showing a
permanent conflictual attitude and a relevant lack of
responsibility.
The undervaluation of the aggressive commercial policy
carried on by the producers of alternative materials is also
discussed.
551
SESSIONE 16

SESSIONE 16
Key words: Dimension stones, gamma-ray portable
spectrometer, granites, radioactivity, Sardinia-Corsica
batholith.
INTRODUCTION
About 6000 km 2 of Sardinia consist of the Sardinia-Corsica
batholith made up of several plutons emplaced between 311 and
286 Ma (OGGIANO et alii, 2005; GAGGERO et alii, 2007). The
wide emplacement time-span allowed large compositional
variability of these intrusions, which range from quarzodioritestonalites
to leucomonzogranites. These stones represent a
considerable economic resource; the first evidence of its
exploitation dating back to the 15 th century BC in the building of
nuraghi. Moreover the Roman quarries, active during the Roman
Empire and still visible on the north eastern coast (POGGI &
LAZZARINI, 2005).
Nowadays, granite quarrying activity is located in the centralnorth
Sardinia, mainly in Gallura and Goceano regions, where
several commercial varieties are exploited.
All these stones are widely exploited and represented the main
building materials in the past. Besides, these granites have been
widely exported around the world as tiles, flooring, columns or
other architectonic element. Moreover the north-eastern Sardinia
granite was largely employed for ashlars used in the building of
dwellings until the sixties. Taking into account the large diffusion
of the Sardinian granites, the knowledge of their natural
radioactivity is basic for the evaluation of the amount of public
exposure because people spend most of their time (about 80%)
indoor (NGACHIN et alii, 2007 and their references).
The aim of this work is therefore to determine the K, U and
Th isotopic concentration in these materials.
_________________________
Natural radioactivity in Sardinian granite dimension stones
ANTONIO PUCCINI (*), STEFANO CUCCURU (*), DANIELE SECHI (*), GIACOMO OGGIANO (*),
FABIO MANTOVANI (°), GERTI XHIXHA (°) & SARA MARIANI (**)
(*) Dipartimento di Scienze Botaniche, Ecologiche e Geologiche –
Università di Sassari, apuccini@uniss.it
(°) Dipartimento di Fisica – Università di Ferrara
(**) Centro di Geotecnologie – Università di Siena
552
METHODS
For this purpose a portable gamma-ray spectrometer at the
National Lab of Legnaro (INFN) was developed (Fig. 1).
Fig. 1 – Portable gamma-ray spectrometer in a quarry during the
acquisition of K-U-Th isotopic concentration.
The equipment consists of one liter thallium-activated sodium
iodide scintillator [NaI(Tl)], digiBASE by Ortec and a netbook
which manages also humidity and temperature sensors. By using
the Jradview software is possible to process the data in real time
and to determine uranium and thorium (in ppm), expressed as
equivalent units, and potassium concentration (in %) as well as
total activity expressed in Bq kg -1 . Following the IAEA guideline
(IAEA-TECDOC-1363, 2003), the gamma-ray spectroscopic
analysis is performed by monitoring three spectral windows:
1.37-1.57 MeV for 40 K, 1.66-1.86 MeV for 214 Bi and 2.41-2.81
MeV for 208 Tl.
The concentrations of U/Th are estimated by 214 Bi/ 208 Tl
decays, under the assumption that the U and Th decay series are
in secular equilibrium. This occurs when the parent half life is
much longer than the daughter half life and then the number of
atoms of a daughter isotope essentially becomes constant after
some time. Two conditions are necessary for secular equilibrium.
First, the parent radionuclide ( 238 U/ 232 Th) must have a half-life
much longer than that of any other radionuclide in the series.
Second, a sufficiently long period of time must have elapsed, to
allow for ingrowth of the decay products. The state of secular

Commercial
varieties
Measures
number
Activity 40 K
(Bq/kg)
equilibrium in natural U and Th ores is significantly altered when
they are processed to extract specific radionuclides, in particular
Ra and Rn.
Assuming secular equilibrium, in order to evaluate the
external gamma-radiation dose from building materials, the
following model (HAYAMBU et alii, 1995) was used as criterion.
This model uses the External Hazard Index (Hex) defined as:
Hex= AU/370 + ATh/259+AK/4810
where AU, ATh and AK are the activity concentration of 238 U,
232 Th and 40 K, respectively, in Bq kg -1 in building materials. To
limit the external gamma radiation dose from building materials
to 1.5 mSv year -1 ,Hex must be less than unity in order to maintain
the radiation hazard negligible (XINWEI, 2004).
The average radioactivities of 238 U, 232 Th and 40 K and Hex
measured in different commercial varieties of Sardinian granites
are given in Table 1.
RESULTS AND CONCLUSIONS
Activity 238 U
(Bq/kg)
The data acquires show that the 40 K average activities vary
from 925±110 Bq kg -1 in Grigio Malaga to 1501 Bq kg -1 in Rosa
Cinzia. The 238 U, average activities range from 38±8 Bq kg -1 in
Grigio Perla to 77±18 Bq kg - 1 in the San Giacomo. The highest
average activity of 232 Th was 91±15 Bq kg -1 in Ghiandone and the
lowest average was 59±5 Bq kKg -1 in Rosa Beta.
About the Hex, the commercial varieties showed the highest
values were, in order, Ghiandone (0.83±0.11), Rosa Cinzia (0.82)
and San Giacomo (0.79±0.13).
Finally, all commercial investigated varieties have Hex value
below 1, hence, generally, the corresponding rocks can be safely
used as building materials for dwelling construction also in
indoor conditions.
553
Activity 232 Th
(Bq/kg)
Total Activity
(Bq/kg) Hex
Rosa Cinzia 1 1501 75 79 1655 0.82
Ghiandone 7 1361±106 74±14 91±15 1526±108 0.83±0.11
San Giacomo 2 1473±108 77±18 71±14 1621±111 0.79±0.13
Grigio Malaga 4 925±110 39±6 68±2 1032±110 0.56±0.04
Grigio Perla 10 1288±133 38±8 67±11 1393±133 0.63±0.06
Bianco Sardo 3 1351±72 49±12 60±7 1460±73 0.64±0.06
Rosa Beta 4 1183±110 43±11 59±5 1285±110 0.59±0.07
Tab.1 – Commercial varieties considered and mean values of A 40 K , A 238 U, A 232 Th, Total Activity and Hex (About Rosa Cinzia, was not calculated the uncertainty
because we performed only a single measure)
REFERENCES
GAGGERO L., OGGIANO G., BUZZI L., SLEJKO F. & CORTESOGNO
L. (2007) - Post-Variscan mafic dykes from the late orogenic
collapse to the Tethyan rift: evidence from Sardinia. Ofioliti
32, 15-37.
HAYAMBU P., ZAMAN M.B., LUBABA N.C.H., MUNSANJE S.S.,
MULEYA D. (1995) – Natural radioactivity in Zambian
building materials collected from Lusaka. J. Radioanal. Nucl.
Ch., 199 (3), 229-238.
IAEA-TECDOC-1363 (2003) - Guidelines for radioelement
mapping using gamma ray spectrometry data.
NGACHIN M., GARAVAGLIA M., GIOVANI C., KWATO NJOCK M.G.
NOUREDDINE A. (2007) – Assessment of natural radioactivity
and associated radiation hazards in some Cameroonian
building materials. Radiat. Meas., 42, 61-67.
OGGIANO G, CHERCHI G.P., AVERSANO A., DI PISA A., ULZEGA
A., ORRÙ P. & PINTUS C. (2005) – Note illustrative della
Carta Geologia d’Italia. Foglio 428 Arzachena, S.EL.CA,
Firenze.
POGGI D. & LAZZARINI L. (2005) – Il granito sardo: cave e
cavatura. Usi, diffusione e aspetti archeometrici. Marmora, 1,
49-68.
XINWEI L. (2004) – Natural radioactivity in some building
materials and by-products of Shaanxi, China. J. Radioanal.
Nucl. Ch., 262, 775-777.
SESSIONE 16

SESSIONE 16
Key words: Policy, raw materials, resources, supply.
All nations continually face decisions involving the supply
and utilization of raw materials, substitution of one resource for
another, competing land uses, and the environmental
consequences of resource development.
A nation’s economic security depends on maintaining
adequate mineral resources supplies from a variety of domestic
and international sources emphasizing those with the least
environmental impact.
According to the definition of the EU non-energy raw
materials policy by the European Commission, in Italy it is
necessary to implement a national initiative for planning and
developing the utilization of natural resources (COM 699, 2008).
Informed planning and decisions concerning suitable
resources development require a long-term national perspective
and an integrated approach to land-use, resource and
environmental management.
The availability and efficient use of raw materials is a key
factor for sustainable growth in industrialized countries (COM
670, 2005).
Based on extensive consultation with relevant stakeholders
and in agreement with Ministry of Economical Development, a
Raw Materials Laboratory is starting, with the aim of proposing a
suitable polity in agreement with the raw materials of EU.
As regards domestic supply there is also a question of how to
improve sustainable access to raw material from Italian and
European sources.
This raises specific challenges in the area of exploration for
new resources, the permitting process, research and innovation
and health and safety performance of the extractive industry.
REFERENCES
COM 670 (2005) – Thematic Strategy on the sustainable use of
natural resources. Communication from the Commission to
_________________________
Strategic proposals for the implementation of a national
non-energy raw-materials policy
(*) ANIM (National Association of Mining Engineers), anim@minerari.it
DOMENICO SAVOCA (*)
554
the Council, the European Parliament, the European
Economic and Social Committee and the Committee of the
Regions. 22 pp.
COM 699 (2008) – The raw materials initiative. Meeting our
critical needs for growth and jobs in Europe. Communication
from the Commission to the European Parliament and the
Council. 13 pp.

Key words: Dimension stone, land planning, mining basin,
sustainable development.
INTRODUCTION
The Provincia Autonoma di Trento is situated in the north of
Italy in the eastern part of the Alps. The remarkable lithological
heterogeneity and the geomorphological peculiarities which
characterise Trentino have led to the presence of a wide range of
lithologies, among which Porphyry and carbonatic types of stone.
In the last two decades the presence on the market of
competitive stone materials also coming from abroad has led to
the closure of many of the ornamental stone quarries, however the
quarrying of porphyry is still of considerable importance
(AA.VV., 2005).
THE PORPHYRY INDUSTRY
The porphyry represents nowadays, in Trentino, the most
important extractive sector by a social-economic point of view.
The quarries are about a hundred, the direct employees are about
1300, considering also the linked activities, about 2000. Every
year it is extracted a rock volume of about 1,500,000 cubic
metres.
The term “porphyry” is traditionally used to indicate various
types of volcanic rock belonging to the so-called Adige Valley
Porphyry Shelf, namely an extensive expanse of effusive rocks
which in our region stretches out over an area of around 7,500
km² with a thickness which can reach up to 2,000 metres.
In geological terms “porphyry” corresponds with rhyolitic
ignimbrite and is characterised by its reddish or grey-pink colour
and by intense sub-vertical fissuring over a thickness of around
100-200 metres. This characteristic fissuring allows the extraction
of slabs of various thickness, which together with the high
mechanical resistance and low frost susceptibility, make this kind
_________________________
The sustainable development and the administration of the
porphyry quarries in the Province of Trento
(Provincia Autonoma di Trento)
(*) Provincia Autonoma di Trento, Servizio Minerario,
alessandro.tomasi@provincia.tn.it
ALESSANDRO TOMASI (*)
555
of rock one of the most important materials adopted for external
paving and cladding.
The extraction of porphyry for local use has gone on for
centuries, but it was only starting from 1970, that it was
developed industrially, creating also many problems of an
environmental nature.
Since about ten years ago, all the not utilized material (about
70%) was thrown in big landfills. Starting about from 2000 there
was an important change and, also thanks to pubblic researches,
the wastes are now totally utilized for construction and industry.
THE QUARRIES ADMINISTRATION IN THE
PROVINCIA AUTONOMA DI TRENTO
Trentino since 1972 is an independent authority, then it can
make laws about some matters, among which the mining matter.
The Provincia Autonoma di Trento has been probably the first
one in Italy to promulgate a provincial law about quarries and to
approve a territorial planning of the quarries. In 1980 it
promulgated a provincial law that regulated the quarry activity
and stated also that it must be elaborated a planning of the
extractive areas, named “Quarries Plan”. After the passing in
1983 of a plan concerning only the porphyry quarries, in 1987
was approved the “Piano provinciale di utilizzazione delle
sostanze minerali”. The Plan was updated in 1989, in 1992, in
1998 and in 2003 (PROVINCIA AUTONOMA DI TRENTO, 2003a).
The fourth update of the Plan is part of the basic shift
towards sustainable development enshrined in the Provincial
Development Programme (Programma di sviluppo provinciale)
(PROVINCIA AUTONOMA DI TRENTO, 2003b), which means, as far
as mining resources are concerned, measures aimed at
rationalizing exploitation of deposits, increasing recovery of
waste material and alleviating the impact on the environment,
both through low impact intervention and trough rapid
reclamation of areas used.
On that occasion, a “Strategic Evaluation” and a “Strategic
environmental Report” were also drafted, with the aim of making
an overall planning assessment and examining the individual
areas. This report provided useful guidance for the basic choices
of the plan, and will therefore be reflected in the drafting of
individual quarry executive projects (PROVINCIA AUTONOMA DI
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SESSIONE 16
TRENTO, 2003b).
In summary, the Plan defines the connections with the others
provincial and municipal urbanistic plans, the consumption and
the requirements of the quarries products, the areas where it is
allowed to quarry, the leads for the elaboration of the quarry
plans and of the acts of the municipalities and the principles for
the correct exploitation of the quarries and for the environmental
recovery of the areas.
The law provides different kinds of permission procedures as
per the volume of the extractable material in the quarry:
- for volumes greater than cubic metres 500,000, the plan is
subjected to the procedure of environmental effects evaluation
(V.I.A.);
- for volumes between cubic metres 200,000 e 500,000 the
plan is subjected to a screening to evaluate the possible
undergoing to environmental effects evaluation (V.I.A.);
- for volumes lower than cubic metres 200,000 the plan is
subjected to a more simple procedure; anyway all the landscape,
forest, geological and mining technicalities are analysed.
REFERENCES
AA.VV. (2005) –Atlante della pietra trentina. Antichi e nuovi
percorsi - Guida pratica all‘utilizzo. Nicolodi, Trento, 360
pp.
PROVINCIA AUTONOMA DI TRENTO (2003a)–Piano provinciale di
utilizzazione delle sostanze minerali.
http://www.minerario.provincia.tn.it/piano_cave/
PROVINCIA AUTONOMA DI TRENTO (2003b) – Valutazione
strategica” e “Relazione ambientale strategica” del “Piano
provinciale di utilizzazione delle sostanze minerali”.
http://www.minerario.provincia.tn.it/piano_cave/
556

Key words: Bergamascan stones’ mark of origin, building stones,
Zandobbio dolomite, Zandobbio “marble”.
GEOLOGICAL PROVENANCE AND TECHNICAL
CHARACTERIZATION
The Zandobbio “marble” is an historical-contemporaneous
ornamental and building stone from the lower Cavallina Valley,
Bergamo. Actually it is not a marble s.s., but a compact
crystalline dolomite, with saccharine weaving, known in the
geological literature as Zandobbio Dolostone (BERSEZIO &
CALCAGNI, 1994). According to the recent stratigraphic revision,
it’s a 160m thick member of the Albenza Formation, Hettangian
in age, cropping out at the core of the Bergamo-Zandobbio
Anticlinal fold in the Southern Central Orobic Alps (JADOUL &
GALLI, 2008).
As far as the mineralogical-petrographic composition, it’s a
fine-grained, completely recrystallized, dolomite rock, consisting
of rhombohedral dolomite filled with subordinated secondary
sparry calcite, and traces of self-produced albite (VOLA, 2009).
The market varieties indicated by the EN 12440 standard are
“Zandobbio White” and “Zandobbio Pink”. Nevertheless it is
possible to distinguish a third one, named “Zandobbio Pinkish-
White”, which corresponds to an unique production variety
(VOLA, 2009). All the varieties are present in the following types:
grainy, fractured and uniform (PAGANONI, 1987). Historical
varieties no more available on the market are the “Grey Onix”,
used for sculpturing, and the “Brownish” from the village of
Selva di Zandobbio.
As far as the physical-mechanical point of view, it shows
elevated compressive strength (Rm = 217 MPa, under ambient
conditions), and good frost resistance after freezing and thawing
(Rm = 206 MPa). Water absorption, thermal expansion, and
abrasion resistance are comparable with many other commercial
“marbles” (see Tab. 1). Good structural performance and
elevated durability have been demonstrated during its long period
_________________________
Geo-petrographic and lito-applicative characterization of the
Zandobbio “marble” from lower Val Cavallina, Bergamo
(*) Geologist, Bergamo; gabriele.vola@gmail.com
Author acknowledgments to Mrs. R. Facchinetti, SIMA Srl Gruppo Marell,
Gorlago (Bergamo), and to Dr. A. Locati, Bergamo Chamber of Commerce
GABRIELE VOLA (*)
557
of use. Nevertheless, being a carbonate rock, it is affected by
local dissolution, bleaching and sulphuric damage, showing a
characteristic net-like weathering morphology (VOLA, 2009).
ARCHITECTONICAL EMPLOYMENTS
The main use is ornamental, even since the Middle Ages,
examples of structural use do not miss. Vast dimension ashlars
are used in the historical building’s brick-work of the Upper City,
Bergamo (porches of the Basilica di Santa Maria Maggiore), and
also in the neighbouring localities of the extraction area (the
Romanesque church of San Giorgio in Campis at Zandobbio).
This material was exploited for many centuries, since the
ancient Roman era: manufactured products and tombstones with
Latin inscriptions are diffused all over the Cavallina Valley and
in the Upper City, besides the Roman column of Sant’Alessandro
is still preserved in the Lower City. A peak in quarrying output
and employment in Bergamo’s architecture was during the
Renaissance (frames and horizontal elements of the Colleoni
Chapel, masterpiece of the famous architect A. Amadeo, and the
gate of San Giacomo in the Upper City), in the Baroque (San
Michele all’Arco church, restored by G.B. Caniana, and the
Contarini fountain in Piazza Vecchia), in the Neoclassicism
(Palazzo Nuovo, now public library “Angelo Mai”, by E.
Pirovano on the original project of V. Scamozzi), up to the
Rationalism with the co-called “Piacentini style” (elements of the
Sentierone, andTorre dei Caduti; the former Casa del Fascio, in
the Lower City). Some important applications out of the Province
are the WWI Memorial in Bolzano, the Insurances Palace in
Bologna, the United Nations Palace in Geneva (Switzerland), and
the Capitolium in Havana (Cuba).
The artist Tobia Vescovi (1893-1978) from Zandobbio must
be also mentioned, for his works of an intense expressionism.
Recurring themes in his long career are high-relief “suffering”
bodies, pieties, tombstones and war memorials, widespread all
over the Province of Bergamo, and in private collections.
Main current use regards local monuments restoration, but it
is also used for urban furnishings (benches and fountains) and
internal covering (pavements, baths and staircases). In 2008, in
the Lower City, the so-called Porte di Prato were unveiled, in the
same place where the monument found before its removal in
1882. Symbol of historic elegance and splendour, the Zandobbio
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SESSIONE 16
“marble” is nowadays available not only for restoration purposes,
but for many architectural applications in local and international
market.
Tab. 1 – Physical-mechanical and mineralogical characterization of the
Zandobbio “marble” (VOLA, 2009).
Determination UNI EN Amount
Uniaxial compressive strength (MPa) 1926 Rm=217 ±18
Frost-resistance: compressive strength
after freezing and thawing (MPa)
12371 Rm=206 ± 25
Frost-resistance: compressive strength
percentage deterioration (%)
12371 ? R=13,2
Flexural strength under concentrated
load after freezing and thawing (MPa)
12372 Rtfm=15,9±3
Apparent density (kg/m 3 ) 1936 ?b=2795±20
Open porosity (%) 1936 Po=2,1± 0,1
Water absorption at
atmospheric pressure (%)
13755 Ab=0,6 ± 0,1
Water absorption coefficient
by capillarity (g/m 2 *vs)
1925 C=2,3
Linear thermal expansion
coefficient (μm/m*°C)
14581 a=7,80
Resistance to ageing
by thermal shock (%)
14066
? Mm=-0,05
? Edm=-10,7
Knoop hardness (MPa) 14205
Id=1,8;
HKm=2728
solution “A”
Resistance to ageing by SO2 action
in the presence of humidity (%)
13919
? m

Key words: Anhydrite, Bardiglio of Bergamo “marble”,
bergamascan historic stone products, evaporitic sulphates,
Volpinite.
INTRODUCTION
The Volpinite is a massive anhydrite of scaly and granular
structure and bluish tint, originally reported from Costa Volpino,
lower Val Camonica, Bergamo. This ornamental stone, also wellknown
as Bardiglio of Bergamo “marble”, has been historically
quarried and used for the production of small, decorative objects,
but also as building material, since the XIV century.
From a geological viewpoint it is an evaporitic stone,
pertaining to a km-sized member of the “Carniola di Bovegno”
Formation, lower Triassic in age, pertaining to the stratigraphic
succession of the Lombardy basin in the Central Orobic Southern
Alps (JADOUL et alii, 2002).
GEOLOGICAL PROVENANCE AND TECHNICAL
CHARACTERIZATION
Many Authors deal with this building stone until the second
half of the XVIII th century, especially transalpine chemists,
naturalists, and mining engineers, such as Louis Benjamin
Fleuriau de Bellevue (1761-1852), Louis Nicolas Vauquelin
(1763-1829), René Just Haüy (1743-1822), Alexandre Brongniart
(1770-1847) and A.J.M. Brochant de Villiers (1772-1840). The
first in Italy was MAIRONI DA PONTE (1825), followed by
CURIONI (1855), that described this stone as a “coarse-grained
limestone”, and ROSA (1858) that considered just its industrial
applications. The reference formation in stratigraphy, namely
“Carniola di Bovegno”, was formalized by ASSERETO &CASATI
(1965) in Val Camonica, and mapped into the geological map of
_________________________
Geo-petrographic and lito-applicative characterization of the
Volpinite “marble” (Bardiglio of Bergamo),
from lower Val Camonica
GABRIELE VOLA (*), LUCA ALCIATI (**), ELENA DI MAJO (°) & LAURA FIORA (°°)
(*) Geologist, Bergamo, gabriele.vola@gmail.com
(**) Ufficio Cave, Provincia Asti, lu-al@libero.it
(°) Università di Pisa, elena.dimajo@fastwebnet.it
(°°) Dipartimento Scienze Mineralogiche e Petrologiche, Università Torino
559
Breno 1:100.000 (Foglio 34), between the “Servino Formation”
and the “Calcare di Angolo” (COLLECTIVE, 1971).
The depositional paleoenviroment is a tidal flat and restricted
marine platform, with intertidal passing to subtidal shallow water
carbonate-evaporite lithofacies, typical of warm and arid climates
(sabka). The formation, composed of yellowish vacuolar
dolomites associated to tectonic breccias with yellowish
dolomites and green clasts of argillaceous limestone, locally
presents km-sized lens of gypsum (Castefranco, Pisogne) and
anhydrite (Volpino) (JADOUL et alii, 2002).
From the structural point of view all the Triassic evaporites
represent ductile levels, corresponding to the regional
detachments (basal faulting) of the stratigraphic-sequence, upon
which is arranged the tectonic deformation style of the Central
Southern Alps, by the so–called “flat and ramp” geometry.
Fig. 1-2 : macrographs; Fig. 3-4 : micrographs (PPL, XPL).
As far as the mineralogical-petrographic characterization, the
Volpinite is composed of massive anhydrite (anhydrous calciumsulphate)
with secondary minerals of alteration, such as mica and
clay-minerals. The specificity of this stone is that must be used
just for internal applications, because easily weathering in humid
environments, due to hydration suitability and the subsequent
gypsum’s formation. The good workability is linked to the weak
hardness (3 ÷ 3,5 in the Mohs scale). This is the reason why it
was adopted since the antiquity as a decorative stone and for
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sculpturing, especially when alabastrine in aspect.
QUARRY LOCATION, DEPOSIT EXPLOITATION, AND
HYPOTHESIS OF ENVIROMENTAL RECOVERY
The inactive quarry of Volpinite is located at the bottom belt
of the Volpino village (from which the stone name), on the right
side of the lower Val Camonica, Costa Volpino, Bergamo. The
Volpinite deposit is about 150 m thick, with a lateral extension of
1-2 km. Usually the exploitation was carried out by means of
blasting materials using the sub-horizontal layering of the deposit
to facilitate the extraction of slabs for paving and cladding
materials, but also for blocks production (COMPAGNONI, 1976).
Cutting waste materials and fine-aggregates were generally
grinded in millstones, for the production of pulverized anhydrite
to be used as mineral addition for industrial applications. Among
quarries which exploited the evaporites from the “Carniola di
Bovegno”, recently only the Pisogne one is still open. A project
for the environmental recovery of the Volpino quarry is going to
be evaluated from the local administration, maybe with the
support of the Bergamo Province, in order to develop a cultural
and historic tourism, because it’s evenly considered a “placeidentity”.
ARCHITECTONICAL EMPLOYMENTS
Although it may sounds unusual, locally applications of
anhydrite in the architecture don’t miss, such as the columns and
parietal coverings of the Giovanna D’Arco Chapel, in the
Cathedral of Saint Etienne, Toul, Lorraine, France (FIORA, 2010).
As far as the Volpinite, we recall the XIV-XV century porches
of the Basilica di Santa Maria Maggiore in the Upper City of
Bergamo, works of Giovanni da Campione (active between 1340
and 1360). Moreover the Volpinite has been adopted for the
facade of the Colleoni Chapel, masterpiece of the Lombard
Renaissance, built between 1472 and 1476 by the famous
architect Antonio Amedeo (1447-1522). In the XVII century the
Volpinite was also used by the Bergamascan stone-carver Andrea
Fantoni (1659-1734) from Rovetta (PAGANONI, 1987; VOLA et
alii, 2009). Some significant application in altars is also attested
in the Eastern Piedmont during the XVIII century, especially
around 1730 and 1770. Exactly the Volpinite was introduced in
Piedmont by the Lombard stonemasons, such as the Pellagatta
from Viggiù (Varese). In the habit of working these artisans
widely adopted stones from their own local tradition, for the
straight interest in quarrying output too. This is the reason why,
further than Volpinite, we found also other Lombard “marbles”
such as the Orobic “Red” from the Brembana Valley, the “Black”
from Varenna (Lecco), the “Macchiavecchia” and “Biancorosso”
from Arzo (Canton Ticino), and finally the “Occhiadino” from
Val Camonica (Brescia). Examples of bas-relief sculpturing in
Volpinite dating back from the XVIII century, are preserved in
560
the churches of Camagna Monferrato, Lucedio, and Murisengo
(Eastern Piedmont). At the end of the XVIII century the style
changed, so after a short-time of coexistence, Lombard “marbles”
were generally supplanted by those from the Savoia’s area.
Especially the Volpinite and Occhiadino were respectively
replaced by Grey marbles from Valdieri and Frabosa (Cuneo).
Recently typical examples of application are the decorative
architectonical elements of the local constructions, such as
columns, capitals, slabs, tables, bases, door and window frames,
and bas-reliefs, widespread around the extraction area.
MAIRONI DA PONTE (1825) attested its wide marketing during
the first half of the XIX century in Milan, while ROSA (1858)
documented its quarrying, and marketing in Italy as abroad,
together with the gypsum from Lovere and Pisogne. As far as the
production of pulverized mineral addition for cements, paper
mills, farming fertilizer, and colors industry, is attested until the
second half of the Seventies of the last century (TURCO, 1990).
REFERENCES
ASSERETO R. & CASATI P. (1965) – Revisione della stratigrafia
permo-triassica della Val Camonica meridionale
(Lombardia). Riv. It. Pal. Strat., 71, 999-1097.
COLLECTIVE (1971) – Carta geologica d'Italia, Note Illustrative
al Foglio n.34 Breno. Servizio Geologico d'Italia, Roma.
COMPAGNONI M. (1976) – Costa Volpino. F.lli Ferrari, Clusone
Bergamo.
CURIONI G. (1855) – Sulla successione normale dei diversi lembi
del terreno triassico nella Lombardia. Giorn. I. R. Ist. Lomb.
Sc. Lett., 7, 204-236.
FIORA L. (2010) - Rocce evaporitiche e loro utilizzo.
L’Informatore del Marmista, G. Zusi Ed., Verona, 577, 6-14.
JADOUL F., FORCELLA F., BINI A. & FERLIGA C. (2002) - Note
Illustrative della Carta Geologica della Provincia di
Bergamo alla scala 1:50.000. Ditta Grafica Monti, Bergamo,
313 pp.
MAIRONI DA PONTE G. (1825) – Sulla Geologia della provincia
Bergamasca. Tipografia Mazzoleni, Bergamo, 111-115.
PAGANONI A. (1987) – Le pietre ornamentali della Bergamasca.
Atti Ateneo Sci. Lett. Arti di Bergamo, 46 (2), 561-571.
ROSA G. (1858) – Notizie statistiche della Provincia di Bergamo,
in ordine storico. Tipografia Pagnoncelli, Bergamo, 193 pp.
TURCO T. (1990) – Il gesso. Lavorazione, trasformazione,
impieghi. Ulrico Hoepli., Milano, 609 pp.
VOLA G., FIORA L. & ALCIATI L. (2009) – Stones used in
Bergamo architecture. Stud. Univers. Babes-Bolyai,
Geologia, Special Issue, MAEGS-16, 137-139.

Petrographic quantitative analysis of pozzolanic mortars from
ancient Roman marine concrete cores, drilled by Romacons team
(2006-2009)
GABRIELE VOLA (*), CORRADO STANISLAO (**), CONCETTA RISPOLI (**),
VINCENZO MORRA (**) & MAURIZIO DE GENNARO (**)
Key words: Binder/aggregate ratio, petrographic quantitative
analysis, pozzolanic ancient mortars, Romacons project.
This paper deals with preliminary results of petrographic
quantitative analyses performed on pozzolanic mortars, coming
from ancient marine concrete cores, drilled by ROMACONS team
in the 2006-2009 fieldwork (OLESON et alii, 2004; BRANDON et
alii, 2005; HOHLFELDER et alii, 2007). Concretes cores here
considered come from the Roman age harbours of Baia
(BAI.2006) in the Gulf of Naples, Alexandria (ALE.2007) in
Egypt, Chersonisos (CHR.2007) in Crete, Egnazia (EGN.2008)
on the Adriatic cost close to Brindisi, and finally Pompeiopolis
(POM.2009), near Mersin in Turkey. Stereoscopic analysis on
concrete slices, and petrographic examination on 7x5 mm
“panoramic” thin sections, were performed using a digital net for
point-counting, on a representative number of grains (ca. 900 for
each section). Moreover each component of the mortar was
sampled, using a pair of tweezers, and XRD analyses are still in
progress. These data begin clarifying the provenance of raw
materials and the diverse concrete mix-designs of the various
concrete harbours.
PETROGRAPHIC CHARACTERIZATION
In September 2006 ROMACONS team extracted five cores
from the sunken remains of harbour moles at Baia (BAI.2006.01
(BAI.2006.03), and from the submerged remains of Portus Iulius
(BAI.2006.02, 04, 05), mainly from the first century BC (OLESON
et alii, 2004; BRANDON et alii, 2008). A volcanoclastic tuff from
Campi Flegrei volcanic field is the main constituent of the coarseaggregate
along with white, dull cm-sized grains of reacted lime.
XRD mineralogical analysis of tuff-aggregate, shows sanidine,
_________________________
(*) CTG Italcementi Group, Dir. Lab., Bergamo, g.vola@itcgr.net
(**) Dip. Scienze della Terra, Università Federico II di Napoli
Paper deals with the job done by C. Stanislao and C. Rispoli, at the Lab. Dept.
of the CTG Italcementi Group, Bergamo. Research activity was possible
thanks to the collaboration with the Earth Sciences Dept. of the University
“Federico II” of Naples. Authors acknowledgements to the Romacons team.
561
analcime, clay minerals (illite), zeolites (phillipsite and
chabazite), and hydrotalcite. The mortar is composed of fine tuffaggregate
(21÷29%), including pumiceous scoria, phenocrysts
(sanidine, augite), and fine ash-tuff. The cementiceous matrix
(69÷76%) is mostly composed of microcrystalline sparry calcite
cement (62÷69%), with very little amount of amorphous gel-like
C-S-H (3÷5%). Dull microcrystalline grains of reacted lime,
composed of tobermorite, calcite, plus brucite and vaterite, reach
up to 3%. Their textures attest different stages of dissolution.
Unusual submillimeter-sized rounded grains of sparite, containing
muscovite laminas in the core (2%), have been found in
BAI.06.03. Porosity (1÷2%) is lower than the other mortars, and
binder/aggregate ratio ranges from 2.4 (BAI.06.01) up to 3.5
(BAI.2006.05).
In May 2007 ROMACONS team extracted four concrete from
submerged, first century BC, structures in the eastern harbour
basin at Alexandria. The first two (ALE.2007.01 and
ALE.2007.02) were recovered at the base of Antirhodos Island,
and the third one (ALE.2007.03) from a large pilae extending
south from the modern western breakwater. The coarse-size
aggregate is composed of a bioclastic grainstone, probably the
local kurkar eolianite limestone. The tuff-aggregate in the mortar
(19÷24%) is composed of fine ash-tuff, pumiceous scoria,
phenocrysts (sanidine and augite), and zeolite fillings inside
amygdaloidal cavities of the tuff. As far as the fine-aggregate is
considered, local carbonate rock fragments reach the 6%. The
cementiceous matrix is essentially composed of microcrystalline
sparry calcite cement (30÷36%, probably underburned lime
clasts), plus amorphous gel-like C-S-H (32÷35%), and rare dull
grains of reacted lime (1%). Round pores in the mortar are filled
in by zeolites with the so-called “rosette” morphology (up to 4%).
Total porosity (3÷5%) is higher than in Baia, while
binder/aggregate varies from 2.2 (ALE.07.02, and 03) up to 3.3
(ALE.07.01).
In September 2007 two cores were recovered from the first
century BC/AD breakwater at Chersonisos harbour (BRANDON et
alii, 2005). Only the second one (CHR.2007.02), from a quay
wall exposed above waterline, has been analyzed. Macroscopic
observation indicates that the mortar is very porous and granular,
perhaps poor in lime, while the coarse-aggregate, very irregular
in shape, size, and distribution, is composed of porous
SESSIONE 16

SESSIONE 16
dolomicritic fossiliferous limestone.
Petrographic examination shows that amount of tuff-aggregate
in the mortar is very low (15÷17%), and its lack is partially
replaced by red-brick fragments of cocciopesto (up to 4%).
Pumiceous scoria, sanidine phenocrysts, ash-tuff with zeolite
fillings, and carbonate rock fragments form the fine-aggregate.
The cementiceous matrix (71÷73%) is mainly composed of
amorphous gel-like C-S-H (48÷59%), with subordinated sparry
calcite cement (14÷22%), and rare dull grains of reacted lime (up
to 1%). Total porosity (5÷8%) is the highest, binder/aggregate
ratio is high too (3.4).
The ancient port of Egnatia, probably from the Early Imperial
period, first century BC, was drilled by ROMACONS team in May
2008, on the Adriatic Italian coast, close to Brindisi.
Only one of the three cores planned could be recovered
(EGN.2008.01). It was taken from the taller pila near north side
of ancient harbour. The coarse-aggregate is a porous,
fossiliferous grainstone from the local Pleistocene calcarenite
deposit. The mortar is granular, porous, strongly enriched in
pozzolanic material. The tuff-aggregate (31÷32%) consists of
volcanic rock fragments, and ash-tuff with subordinated
pumiceous scoria, sanidine and augite phenocrysts. Local
carbonate rocks fragments are circa 1%. The cementiceous matrix
is mostly composed of amorphous gel-like C-S-H (47÷49%) with
subordinated microcrystalline sparry calcite (10÷11%), and rare
dull grains of reacted lime (1%). The XRD mineralogical analysis
confirms the presence of calcite, ettringite, and tobermorite. The
porosity (5÷7%) is very high as in Chersonisos, but
binder/aggregate ratio is the lowest (1.7).
The last concrete cored by ROMACONS team in 2009 was in
Pompeiopolis harbour, close to Mersin, in Turkey, unknown age.
Two cores were extracted from the west breakwater. The top
surface of the mole is currently above sea level, so it was possible
to drill the complete height of the structure.
Preliminary observations of the first core (POM.2009.01)
showed friable, poorly compacted mortar, and hard, closely
packed, riverbed cobbles up to 20 cm size. Oppositely the second
core (POM.2009.02) showed a very hard, well mixed, pozzolanic
mortar. Petrographic examination shows that the coarse-aggregate
is composed of metamorphic anphibolite (Prg, Pl and Clc), stony
corals, and travertine. Fine tuff-aggregate of the mortar (13÷19%)
is composed of pumiceous scoria, volcanoclasts, sanidine and
augite phenocrysts, and ash-tuff. Few carbonate rock and redbrick
fragments also occur.
The cementiceous matrix is mostly composed of
microcrystalline sparry calcite (40÷61%), subordinated
amorphous gel-like C-S-H (9÷31%), and abundant dull grains of
reacted lime (3÷9%). XRD analysis on dull grains points out
calcite and tobermorite. Total porosity (3÷6%) is high, and
binder/aggregate ratio reaches the highest value (4.5) of all the
cores.
562
PRELIMINARY CONCLUSIONS:
Coarse-aggregate (> 4 mm) is generally composed of dmsized
fragments of dark vitric ash-tuff (caementa), plus cm up to
dm-sized fragments of crushed local carbonate rocks (limestones
or dolomitic limestones). The only exception regards
Pompeiopolis concrete, which was cast using river cobbles. The
tuff-aggregate has sanidine, augite, and zeolite fillings
(phillipsite, chabazite). Mineralogical association, confirmed by
XRD analyses, is consistent with that of the “Neapolitan Yellow
Tuff” from Campi Flegrei volcanic field (DE GENNARO et alii,
2000). Mortars always include pozzolanic volcanic fine-ash, the
pulvis Puteolanus of Vitruvius (OLESON et alii, 2004), pumiceous
scoria, phenocrysts, and volcanoclasts. Crushed aggregates from
local carbonate rocks, and red-bricks amount is little. Dull
residual grains of hydrated lime in seawater show progressive
stages of dissolution. The microcrystalline cementiceous matrix is
often associated to gel-like C-S-H. At the current stage of
knowledge, origin of zeolites “rosettes” found in the mortar could
be interpreted as a consequence of minerogenetic processes
occurring after the concrete setting, which developed at expenses
of the glassy fraction (pozzolana, pumices, etc.) by interaction
with seawater in a in a somewhat less alkaline environment.
In conclusion, petrographic quantitative analysis is a powerful
tool in distinguishing features of pozzolanic mortars, especially
binder/aggregate ratio is an important parameter in evaluating the
progression of the pozzolanic reaction.
REFERENCES
DE GENNARO M., CAPPELLETTI P., LANGELLA A., PERROTTA A.,
SCARPATI C. (2000) – Genesis of zeolites in the Neapolitan
Yellow Tuff: geological, volcanological and mineralogical
evidences. Contrib. Mineral. Petrol., 139 (1), 17–35.
BRANDON C., HOHLFELDER R. L., OLESON J. P. et al. (2005) - The
Roman Maritime Concrete Study (ROMACONS): The Roman
harbour of Chersonisos in Crete and its Italian connection.
Mediterranée, 1, 25-9.
BRANDON C., HOHLFELDER R.L. & OLESON J.P. (2008) - The
Concrete Construction of the Roman Harbours of Baiae and
Portus Iulius: The ROMACONS 2006 field season; Int. Jour.
Naut. Arch., 37, 374-392.
HOHLFELDER R.L., BRANDON C., & OLESON J.P. (2007) -
Constructing the Harbour of Caesarea Palaestina, Israel:
New Evidence From the ROMACONS Field Campaign of
October 2005. Int. J. Naut. Arch., 36, 409-415.
OLESON J. P., BRANDON C., CRAMER S., CUCITORE R., et al.
(2004) - The ROMACONS project: a contribution to the
historical and engineering analysis of hydraulic concrete in
Roman maritime structure. Int. J. Naut. Arch., 33, 199-229.

SESSIONE 17
Pericolosità da eventi geo-idrologici e strategie per la
mitigazione del rischio
CONVENERS
Fausto Guzzetti (CNR Cosenza)
Giulio Iovine (CNR Cosenza)
Alberto Puccinelli (Università di Pisa)
Anna Rosa Scalise (ISPRA)
Piero Farabollini (Università di Camerino)
563
SESSIONE 17

SESSIONE 17
Landslides in urban areas: the eastern slope of the Monteverde hill
in Rome
Key words: Inclinometers, landslides, Monteverde, Roma, urban
areas.
Recent landslides that struck southern Italy have brought the
geological instability of the Italian peninsula again to the
attention of the general public.
The city of Rome was not in the past and is not at the
moment, free from slope instability (AMANTI et alii, 1995, 2008);
we just remember the slide/flow in Via Labriola (Monte Mario)
active since 1960 and reactivated last time at the end of 2008, or
the rockfall occurred in 2007 on the western slope of Monti
Parioli (Viale Tiziano).
Fig. 1 – In the circle you can see the studied area. The heavy line represents
the section of Fig. 2.
_________________________
(*) ISPRA – Servizio geologico d’Italia, marco.amanti@isprambiente.it
(**) libero professionista, catageo@tiscali.it
MARCO AMANTI (*) & GIUSEPPE CATALANO (**)
564
This paper wants to show the evolution in the past and the
present state of activity of one of the "historical" landslides of the
Capital (Fig. 1): the eastern slope of the hill of Monteverde (Via
Ugo Bassi – Via Aurelio Saffi), a natural offshoot of the
Gianicolo hill, and a unique and natural observation point on
Roma downtown.
The whole slope along the NW side of Viale Trastevere
(known as Viale del Re in the first part of ‘900) between Via
Dandolo and C.ne Gianicolense, is an attention area with regard
to ground stability. The steep profile of the slope, whose
urbanization began in the ‘50s of last century, and which connects
the Tiber floodplain with the relief referred to generically as
Monteverde, is subjected to a delicate balance, mainly due to man
actions.
A historical research on the movements occurred in the past
was conducted together with the examination of many aerial
photographs covering a period between the ‘60s and today. These
researches allowed the identification of the area subject to
different types of movements and to draft a list of the damages
occurred in the past and in some cases lasted until today.
Principal movements occurred in the last years of the 19 th
century, during the WWI (FOSSA MANCINI, 1922), between 1925
and 1927, in 1947 and in 1963. The 1963 event was the main one
of the century, destroyed many houses, walls and the sewage
system of the area causing the local streets to be closed to cars for
a long time. After a stop in the main movement followed to works
done in the first half of the ‘80s, some superficial movements
started to appear in the ‘90s and in the last ten years. As a general
information coming from different sources, the main events seem
to be occurred after periods of heavy rainfall.
Fig. 2 – One of the sections used to compare the topographic surfaces
between 1849 and 2008.

Authors were able to find a detailed topographic map of the
area dating back to 1849 and a comparison (Fig. 2) was made
with the present topographic surface, highlighting the differences
occurred over 150 years and assessing a reliable evaluation of the
thickness of removed sediments or, on the contrary, of settled
landfill because of human activities.
However the most important part of the work was the
comparison between data on the stability of the slope measured
specifically during 2008-09 and those dating back to 2004-05,
surveyed during a study commissioned by the Province of Rome
(PROVINCIA DI ROMA, 2006).
In particular, three measurement campaigns were carried out
between the beginning of 2008 and the end of 2009 on 15
inclinometer tubes placed in the area during previous monitoring
campaigns, pointing out, for some of them, movements related to
a possible slip plain located between 10 and 12 m from the
surface as well as other more superficial movements.
In conclusion, while taking into account the difficulty of
comparing data from different measurement campaigns
conducted with different instruments, nevertheless the results
obtained in this work, properly calibrated and processed, can be
considered reliable to evaluate the stability of the slope.
In particular they demonstrate that the existing remedial
works, built in the ‘80s, are still acting well in the upper part of
the slope, while small movements can be measured in the lower
part of the slope.
So the suggestion is not to reduce the attention on the area,
but to start a regular monitoring program in the next years,
especially because of the presence of inhabited buildings at the
very foot of the slope. A continuous maintenance of the
superficial draining system is also needed.
REFERENCES
AMANTI M., GISOTTI G. & PECCI M. (1995) - I dissesti a Roma.
In: La geologia della città di Roma: il centro storico, Cap 4.
"Geologia Tecnica". Mem. Descr. Serv. Geol. d’It., 50,
Roma.
AMANTI M., CESI C. & VITALE V. (2008) – Le frane nel territorio
di Roma. In: La geologia di Roma dal centro storico alla
periferia. Mem. Descr. Serv. Geol. d’It., 80, Roma.
FOSSA MANCINI E. (1922) – Un nuovo quartiere di Roma
(Monteverde) e le frane. Giorn. Geol. Pratica, 17, 54-66.
PROVINCIA DI ROMA (2006) - Studio di fattibilità relativo al
progetto di riqualificazione e progettazione territoriale della
Collina di Monteverde nell’area compresa tra via Ugo Bassi
e Viale Trastevere – Provincia di Roma, Dipartimento XII,
Servizio 2, “Sviluppo Locale”.
565
SESSIONE 17

SESSIONE 17
Weather and geotechnical monitoring at “Marco e Rosa De Marchi”
resort (q. 3610 m), Guzza ridge – southern side of Pizzo Bernina
(Alpi Retiche, Sondrio)
ALESSANDRO BALLINI (*), CRISTIAN LUSSANA (**) & GREGORIO MANNUCCI (*)
Key words: Collapse, geotechnical monitoring, heat balance,
meteorological monitoring, rock mass, ruin.
This paper is about the utilization of an integrated monitoring
system (weather and geotechnical) finalized to evaluate the
hazard related to events of collapse, in order to reach the
mitigation and risk reduction thanks to the presence in the area of
instability of a strategic presence at 3610 m altitude, obliged stop
for climbers facing the climb to Pizzo Bernina (4.050 m).
The collapse in the high mountains are paroxysmal
phenomena of the dismantling of cliffs probably correlated to the
actual phase of de-glaciation due to the increased heat of the last
few decades, at both global and local scale. This trend is
expressed in the alpine areas of high mountains, in the form of
two closely related effects: the contraction of area and volume of
glaciers, falling rocks, landslides and mudslides (PAGETTI, 2005).
The phenomena of collapse generate situations of risk for the
visitors of high-altitude environment and impose sudden and
significant morphological changes in the scope; the glacial-nival
reduction of coverage for most of the year, coupled with the
intense degradation of interstitial ice cliffs at high altitudes,
promotes the increase of freeze-thaw cycles, which in turn
accelerate the gradual dismantling of the cliffs (ARENSON &
SPRINGMAN, 2000).
Some examples of this “new dynamics” are represented by
different slope instability like collapse of Punta Thurwieser
(2004), the break downs of the Italian side of Monte Cervino
(2003 e 2006) and the collapse of Torre Trephor in the Gruppo
delle “Cinque Torri” on “Dolomiti cortinesi” (2004).
_________________________________
(*) ARPA Lombardia, Settore Suolo, Risorse Idriche e Meteoclimatologia –
U.O. Suolo e Servizio Geologico, a.ballini@arpalombardia.it –
g.mannucci@arpalombardia.it.
(**) ARPA Lombardia, Settore Suolo, Risorse Idriche e Meteoclimatologia –
U.O. Servizio Meteorologico Regionale, c.lussana@arpalombardia.it.
Lavoro eseguito nell’ambito del progetto “Marco e Rosa - installazione di
una stazione geotecnica e climatica in alta quota” con il contributo
finanziario di Regione Lombardia – Direzione Generale della Polizia Locale,
Prevenzione e Protezione Civile.
566
The new “Marco e Rosa” shelter is located at the Forcola di
Cresta Guzzo (3610 m) on the Italian side of Monte Bernina near
the city of Lanzada (SO). During 2003 the slope below the new
“Marco e Rosa” shelter was affected by a collapse phenomenon
that has destroyed the historical route of access to shelter called
“delle Roccette” pushing the CAI of Sondrio – department of
Valtellina, owner of the structure – to require a technical support
to the ARPA Lombardia to deepen the knowledge of the area in
ruin. To verify the consequential between weather conditions and
local climatic potential collapse, in 2007 a monitoring system
telemetry instrumentation has been designed and implemented. It
consists of geotechnical control of superficial and deep
deformation of the rock mass (2 strain gauges, 3 slit gauges, 2
inclinometers at the wall), coupled with meteorological
instrumentation for the acquisition of parameters necessary for
calculating the heat balance at the scale of the cluster (1
radiometer, 4 thermistors in sub horizontal holes, a thermohygrometer,
1 sonic ranging sensor for snow depth). To better
Fig. Fig. 1 1 – – Location of of installed equipment to to control the the rock rock instability at at the the hut hut
Marco e Rosa e Rosa (3610 m).
m).
understand the underlying causes of the instability, in 2008 the
original monitoring system was integrated with the completion of
two probes in soil with the destruction of the nucleus and the
subsequent installation and commissioning of a incline metric

tube (17 m from p.c.) and a chain thermometer (20 m from p.c.)
to measure the internal temperature of the rock mass on which the
shelter is built. The monitoring point has been equipped with a
satellite data transmission system and a webcam (Fig. 1).
Given the particular measurement conditions (high altitude), it
was decided to focus the analysis on the radiative characteristics
of the site during the three summer months of June, July and
August. Based on the analysis of the albedo, or the ratio of
reflected radiation and the global solar radiation (for a typical
summer day it is generally known that this parameter is in the
range of 0.3 and 0.4), the data are indicative of the fact that 30-
40% of incoming solar radiation is reflected from store rocks
(diorite and granodiorite; GUGLIELMIN, 2004). This value is
consistent with the indications in the literature for a bare rocky
soil. The determination of day-type summer solar radiation and
infrared radiation shows how the latter component is always
negative, on the average of the bare surface of the mass emits
energy toward the sky. The analysis of the net radiation shows
how during the night the energy is emitted from the soil to the
surface and then into the atmosphere (negative net radiation), in
contrast during daytime solar heating ensures a good energy
input.
The analysis of the available data show that the phenomenon of
instability is currently in slow or very slow evolution. The rock
mass below the shelter is deformed in agreement with changes of
physical state of the water in the cracks that disjoint the rock
mass (secondary permeability) and in response to thermal
properties of rock mass itself (LADANYI, 2006). The seasonal
“pulses”, or winter swells and summer contractions, are
interpreted as effects of cycles of freezing and thawing of ice in
the fractures, as evidenced by the consistency of geotechnical
data (Fig. 2).
Fig. 2 – Evolution of displacements measured by slit gauge EF1 (light line)
compared with the temperature (dark line).
The in situ acquisition of data related to meteorological and
geotechnical parameters is therefore a prerequisite for increasing
567
knowledge about the phenomenon occurring, in terms of
predisposing conditions and triggering mechanisms, with the
ultimate objective of achieving a geotechnical model aimed at
identifying scenarios of events and possible critical thresholds of
initiation for the management of any critical future event.
REFERENCES
ARENSON L. & SPRINGMAN S. (2000) - Slope stability and related
problems in Alpine permafrost. In: Proceedings of the
International Workshop on Permafrost Engineering, Svalbard,
Norway, pp. 185–197.
GUGLIELMIN M. (2004) - Observations on permafrost ground
thermal regimes from Antarctica and the Italian Alps, and
their relevance to global climate change. Glob. Planet.
Change, 40, 159-167.
LADANYI B. (2006) - Creep of frozen slopes and ice-filled rock
joints under temperature variation. Can. J. Civ. Eng. 33,
719–725.
PAGETTI F. (2005) - Il riscaldamento del pianeta – cambiamenti
climatici dalla scala globale alla scala locale. Franco Angeli,
Milano.
SESSIONE 17

SESSIONE 17
Geomorphological map and model of the Carrara Marble Basins
(Tuscany, Italy)
CARLO BARONI (*), PAOLO MANNUCCI (*), GIUSEPPE BRUSCHI (**) & ADRIANO RIBOLINI (*)
Key words: Apuane Alps, debris flow, fabric analysis,
geomorphology, human-induced hazard, Northern
Apennines.
Marble extraction in the Carrara basins has endured since the
first Millenium BC with relevant exploitation during the
Renaissance, including the legendary Michelangelo Quarries.
As a consequence of this long-lasting activity, the landscape is
almost completely sculptured by extensive quarry fronts and
covered by huge dump deposits, locally named ravaneti.
Through detailed field survey and aerial photograph
interpretation, we compiled a geomorphologic map at the scale of
1:5,000 of the Carrara Marble Basins. A geomorphological map
and a model at the scale of 1:10,000 derived from the 1:5,000
scale map and were printed with the financial support of the
“Fondazione Cassa di Risparmio di Carrara”.
Through geomorphological survey, historical documents,
stratigraphic and grain-size analyses, we reconstructed the
evolution of the anthropized landscape and characterized both
current geomorphic processes and past phenomena. Multitemporal
topographic maps and aerial photographs enable
assessment of changes in the extension of recent ravaneti (19 th -
20 th Centuries). Our data highlight a rapid increase in their
extension in the last 30 years.
Four main stratigraphic units are recognizable in the ravaneti.
The different texture and structure of these units reflect the
evolution of marble quarrying techniques. The oldest and deepest
debris layer is made up of flat-pebbles with an open-work
structure. This manually produced debris is associated with very
distinctive excavation cutting traces (caesurae in latin) covering a
palaeosol predating the Roman excavation activity. More than 10
sites have supplied archaeological finds of the Roman period.
Slope deposits locally separate this debris into sub-units.
Medieval-Renaissance ravaneti are locally documented on top of
this unit, burying a post-roman soil.
Coarse multi-decimetre-sized boulders (human head size, <
30 cm) with a scarce fine matrix constitute the typical ravaneto of
_________________________
(*) Dipartimento di Scienze della Terra, Università di Pisa,
baroni@dst.unipi.it
(**) Comune di Carrara
With the financial support of the Fondazione Cassa di Risparmio di Carrara
568
the period between the end of the 19 th Century and the 1950s.
The uppermost layer, with boulders and abundant fine matrix
(sand to silt), is the consequence of the new diamond wire cutting
methods, introduced in the 1970s.
Geomorphologic and grain size analysis shows that most of
the debris flow and soil slip events involve the modern ravaneti,
the others being more stable. The fine matrix produced by the
recent techniques of block cutting/grinding and which is directly
tipped into the ravaneti, strongly destabilises the dump deposits,
making them very prone to hazardous remobilization by debris
flows and shallow landslides.
In conclusion, new quarrying techniques and the reject stone
recovery system recently induced geomorphologic hazard
scenarios, being these quarry dump deposits affected by frequent
debris flows. This phenomenon is the most significant currently
active geomorphological process in this anthropic landscape.
Fig. 1 – Overview of the Ravaccione area in the Torano Basin (from
Campocecina). The quarries of Cima Canalgrande (on the left) fed ancient
and weathered quarry dumps. Active quarry dumps (lighter grey on the right)
develop from the quarries of Betogli. Michelangelo picked out the marble he
used in his astonishing sculptures from the ancient quarries of the Ravaccione
Basin (May 18, 2004).

Key words: Landslide, multiple model, regression, zonation.
Landslides, flood, earthquakes, and volcanos, are natural
disasters that cause loss of life and financial damage. The growth
of population causes increased pressure on natural resources. The
consequence is the acceleration of occurrence of natural risks
such as landslide and flood. ANBALAGAN (1992) has provided the
map of landslide hazard zonation in some regions in India. This
method is based on the factors influencing the landslide risks. He
showed that the factors of geology, topography, vegetation cover
and ground water conditions were effective factors in the
occurrence of landslides.
KHULLAR et alii (2000) have provided a map of landslide
hazard zonation of Mizaran in the Eastern north of India based on
the combination of slope, level and surface topography. They
claimed that the map conforms with the existing landslides. LAN
et alii (2004) have prepared a map of landslide hazard zonation
in the Xiaojiang watershed. They showed the factors of lithology,
geology structure, slope, aspect of the slope, elevation and the
distance from active faults were effective factors in occurrence of
landslides.
The rate of damages which are caused by the occurrence of
landslide in Iran until the early of 1999 was about 1866 billion
RLS (MAHMOODI & KARAM 1991). By considering slope,
geology, aspect and elevation and using multiple regression
analysis, PEJAM (2001) performed landslide hazard zonation of
Alamot Drainage Basin and declared that these factors were
effective factors in the instability of slopes and this method has
reasonable capability.
In this research the applicability of HAERI-SAMIEE (1997)
Zonation Model in detailed level and at a scale of 1:50000 in
Baghdasht watershed, Golestan province, is investigated. The
relation of seven factors of Haeri- Samiee Landslide hazard
zonation model such as lithology, slope, fault, river and road,
precipitation, intensity of precipitation and earthquake, were
investigated in occurrence of landslides in Baghdasht watershed
by statistical comparison of hazard map with inventory map and
_________________________
Landslide hazard zonation using multiple regression(Iran)
MASOOD BEHESHTIRAD (*), MOHAMAD REZA SARVATI (**) & NEDA NOORMANDIPOOR (°)
(*) Islamic Azad University, Baft branch, Department of Natural
Resources, masood_kn@yahoo.com.
(**) Beheshti University, Tehran
(°) Islamic Azad University, Baft branch, Department of Natural Resources
569
geometrical dimensions of landslides. Identification of the
effective factors in occurrence of landslides for predicting and
management of landslide hazard are useful. YALCIN (2008)
prepared the map of landslide hazard zonation with information
model in turkey, and his results show that geology, aspect,
vegetation cover, river and road are effective factors in
occurrence of landslides.
The Baghdasht watershed is located between 36°17' and
36°31' north latitude and 55°2' to 55°12' east longitude in the
Ghazvin province in Iran. The area of this watershed is 54,602
ha, the average elevation 2,350 meters above sea level.
The average rainfall is 620 mm per year. The type of climate
is semi humid cold. The formation of geology in this watershed is
Khosh Yalagh, Tizkoo, Mobarak, Karaj, Ilika, Sediments
quaternary and shemshak (BEHESHTIRAD, 2010).
METHODS
In multiple regression model analysis, the relation between
one variable and some independent variables is investigated.
Dependent variable is landslide inventory map and independent
variables consist of information layers as geology, slope, aspect,
distance from river, distance from road, distance from fault,
elevation, rain and land-use.
For undertaking the landslide hazard zonation, the
topographical maps at a scale of 1:50,000 were scanned. In the
Arc-Gis program environment, the coordination system
(longitude and latitude) was converted from degrees to metres
(UTM). This map was divided into cellular networks with the
dimension of 500 × 500 m as working units.
Existing landslides have been identified and an inventory map
made. The necessary information layers as geology, slope, aspect,
distance from river, distance from road, distance from fault,
elevation, rain and land-use were provided in Arc-Gis. Based on
the information layers, the distinctions of geoloy, slope, aspect,
river, road, fault, elevation, rain, land-use and percent of
landslide in each cell were determined. These data for running
model stepwise were entered into a data base in order to make
multiple model using spss program. After the computation of the
model, the landslide hazard class in each cell was determined. At
the end, based on similarities of cells classes, the map of
landslide hazard zonation was developed in the program
environment of Arc-Gis into contours of equal hazard.
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Fig. 1 –
Percent Area
35
30
25
20
15
10
5
0
4.2
9.1
In order to investigating the applicability of the multiple
regression landslide hazard zonation model and existing
landslides, a field inspection was undertaken using topographical
maps at a scale of 1:50,000, interpretation aerial photographs and
with the cooperation of local guides from Baghdasht Thios. It
was done by walking through the area identifying existing
landslides in the watershed based on field evidence. The
coordinates of the landslides were determined by GPS.
We assigned the type and geometrical dimensions of
landslides. According to the geographical position (longitude and
27.1
30.9
28.6
very low low moderate high very high
Hazard Calsses
Fig. 2 - (a) Landslide hazard zonation map based on Multiple Regression; (b)
Distribution (frequency) of H.-S. landslide hazard classes.
570
latitude), the landslide inventory map was developed in the Arc-
Gis program environment for the Baghdasht watershed (Fig. 1).
The correlation between existing landslides with the numerical
values and classes of hazard potential using the predictive model
was investigated. The high correlation would identify the
suitability model in this watershed. We used regression analysis
between existing landslide in each cell and hazard classes.
RESULTS
After the computation multiple regression model in Arc-Gis
program environment, the landslide hazard zonation map of
multiple regression model was provided (Fig. 2a).
In this Landslide hazard zonation map, the greatest area
distribution belongs to high hazard class (Fig. 2b). The least area
distribution belongs to very low hazard class (Fig. 2b).
y = 1.025 L – 0.000022 F – 0.000043 Ro + 0.00037 A +
+ 0.458 U -0.000042 Ri + 0.00129 S – 0.16
where: y= percent area of landslides in each cell; L = litology; F
= fault; Ro = distance from road; A= aspect; U= land use; Ri;
distance from river; S=slope.
REFRENCES
ANBALAGAN R. (1992) - Landslide hazard evaluation and
zonation mapping in mountainous terrain. Eng. Geol., 32,
269-277.
BEHESHTIRAD M. (2010) - Landslide hazard zonation using
information value. Islamic Azad University of Ardestan.
HAERI S.M. & SAMIEE A.H. (1997) - A new method for Landslide
hazard microzonation based on microzonation studies in
Golestan province. Earth Sci. Bull., 23, 2-16 (in Persian).
KHULLAR V.K., SHARAM R.P. & PARMANIK K. (2000) - A GIS
approach in the landslide zone of Lawngthlia in southern
Mizoran. Proc. 8 th Intern. Symp. Landslide, 3, 1461-1472.
LAN H.X., ZHOU C.H., WANG L.J. & LI R.H. (2004) - Landslide
hazard spatial analysis and prediction using GIS in the
Xiaojiang watershed, Yunnan, China. Eng. Geol., 76, 109-
128.
MAHMOODI F. & KARAMI A. (2001) - Statistical modeling for
Landslide hazard zonation using RS and GIS in Sarkhoon
watershed. Geomatic Confer., 147-155 (in Persian).
YALCIN A. (2008) - GIS – based landslide susceptibility mapping
using analytical hierarchy process and process and bivariate
statistics in Ardesen(Turkey): Comparisons of results and
confirmations. Catena, 72, 1-12.

Application of the Rockfall Hazard Rating System modified to a road
affected by high traffic intensity
Key words: Roads, rockfall hazard and risk, Southern Italy.
INTRODUCTION
In order to assess the exposition to the risk associated with
rockfalls, and to prioritize budget allocations for maintenance and
remediation works along a road affected by high traffic, an
application of the Rockfall Hazard Rating System modified
(RHRSmod) was performed. This approach (BUDETTA, 2004) was
developed beginning from the original RHRS method suggested
by PIERSON et alii (1990) at the Oregon State Highway Division.
The RHRS provides a rational method to make informed
decisions on where and how to spend construction funds.
Exponential scoring functions are used to represent the increases,
respectively, in hazard and in vulnerability that are reflected in
the nine categories forming the classification. The resulting total
score contains the elements regarding the evaluation of the degree
of the exposition to the risk along roads.
In the RHRSmod method, the ratings for the categories “ditch
effectiveness”, “geologic characteristics”, “volume of
rockfall/block size”, “climate and water circulation” and “rockfall
history” have been rendered more easy and objective. The main
modifications regard the introduction of Slope Mass Rating by
ROMANA (1988) improving the estimate of the geologic
characteristics, of the volume of the potentially unstable blocks
and the underground water circulation. Other modifications
regard the scoring for the categories “decision sight distance” and
“road geometry”. For these categories, the Italian National
Council’s standards (CONSIGLIO NAZIONALE DELLE RICERCHE,
1980) have been used.
Beginning from previous studies performed along the State
road n° 145 linking several important villages and towns of the
northern slope of the Sorrentine Peninsula (BUDETTA, 2004), this
paper shows new results regarding the southern slope of this
_________________________
(*) Section of Applied Geology, Department of Hydraulics, Geotechnical
and Environmental Engineering, University of Naples “Federico II”, emails
budetta@unina.it; michele.nappi@unina.it
(**) “Destra Sele” Basin Authority, email gerarlo@tin.it
This work was carried out with financial contributions from the University
of Naples “Federico II”.
PAOLO BUDETTA (*), GERARDO LOMBARDI (**) & MICHELE NAPPI (*)
571
region, served by the State road n° 163 (“Amalfitana”). This road
links famous tourist resorts, such as Positano, Amalfi and
Salerno, and is affected by high traffic intensity (mainly during
summer) because is the only transportation corridor of this area.
Due to mountainous setting of this region, high road cuts and
several bends, reducing the available decision sight distance
(DSD), characterize this road.
In recent years, the area crossed by the road experienced
several rockfalls causing several incidents including some
fatalities as well as a large amount of damage and traffic
interruptions. In the aftermath of each rockfall, the National
Company which owns the road (“Ente Nazionale per le Strade”)
and the “Destra Sele” Basin Authority having jurisdiction on the
area, carried out geo-mechanical studies and stabilization designs
in order to reduce the road vulnerability. Particularly, were
located the following three road sections, characterized by high
rockfall probability, and placed in the municipal territories of
Conca dei Marini, Amalfi and Maiori. The main results of the
rockfall risk scoring regarding these road sections will be shortly
explained, below.
MAIN RESULTS
The Sorrentine Peninsula consists of calcarenites, limestones
and dolomites from Trias to Cretaceous, in the shape of
monoclinal northward verging. The south slope of this structure is
steeper than the north side and is affected by intense fracturing
with NW and NE trending faults, generating wide areas affected
by high hazard mainly due to rockfall and toppling, as well as to
rock avalanches.
Along two relevant cross sections of each studied site, the
RMR and SMR ratings were evaluated to estimate geomechanical
characteristics of the outcropping rock-masses. The
higher SMR value is for the section 1 in the Amalfi site (value
80), while the lower for the section 1 in the Conca dei Marini site
(value 59).
Several traffic flow data were analysed in order to estimate
the traffic intensity during two different period of the year
(spring/summer and autumn/winter), and for different brightness
conditions (day and night). Furthermore, a detailed study of the
road geometry crossing the analysed cross sections, allowed to
determine DSD for two traffic directions, towards Naples and
towards Salerno. For each traffic direction, the available DSD is
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Fig. 1 – Main values of the parameters characterising the RHRSmod method, detected in the studied sites.
like the stopping distance in seven cases, while the lower values
affect the section 2 of the Conca dei Marini site. For the six
analysed sections, the evaluation of RHRSmod allowed to assess
that the risk greatly changes with reference to different period of
the year and brightness conditions, being the higher values in the
spring/summer period and during the day. The RHRSmod was
calculated always considering the wet road because this is the
worse condition for a rapid car stopping. The Conca dei Marini
site displays the higher values of RHRSmod in every annual period
and brightness condition while, due to a close bend strongly
reducing DSD, the absolute maximum value was recorded for the
Maiori site, in direction of Naples.
In order to prioritize remediation works to reduce the impact
risk between the landslide deposit on the road and vehicles, it is
necessary to carry out immediate stabilization measures in the
above-mentioned sites. Instead, a low urgency distinguishes the
road cuts placed in the Amalfi site.
572
REFERENCES
BUDETTA P. (2004) – Assessment of rockfall risk along roads.
Nat. Hazards Earth Sys., 4, 71-81.
CONSIGLIO NAZIONALE DELLE RICERCHE (1980) - Norme tecniche
per le costruzioni stradali. Pon. 1V, 11-15.
PIERSON L.A., DAVIS S.A. & VAN VICKLE R. (1990) – From
Rockfall Hazard Rating System – Implementation Manual.
Federal Highway Administration (FHWA), Report FHWA-
OR-EG-90-01, FHWA, U.S. Dep. Of Transp.
ROMANA M. (1988) – Assessment Practice of SMR classification
for slope appraisal. Proc. 5 th Int. Symp. on Landslides,
Balkema, Rotterdam, 1227-1229.

On the reliability of landslide inventory mapping: the case study of
Monte Albino, Nocera Inferiore (southern Italy)
Key words: Inventory, landslide, mapping.
The landslide inventory is the basis for all the landslide
zoning activities. Therefore, the inventory must be done
thoroughly in order to avoid consequential errors in landslide
susceptibility and hazard maps (FELL et alii, 2008a). Interesting
examples on the reliability of the landslide zoning are given by
VAN WESTEN et alii (1999) and ARDIZZONE et alii (2002).
This work is aimed to suggest a procedure for a reliable
landslide inventory mapping with reference to the case study of
Monte Albino (Nocera Inferiore, southern Italy), affected on
March 2005 by first-failure phenomena triggered by rainfall; this
event caused 3 fatalities and some buildings were destroyed.
For the study area (Fig. 1), four different landslide inventory
maps (at scales varying from 1:25,000 to 1:5,000) are available.
They were drawn-up by scientists and/or technicians operating
for: i) the Extraordinary Plan - Landslide Risk of the Regional
Basin Authority of the Sarno river (1999); ii) the Excerpt of the
Hydrogeological Setting Plan – Landslide Risk of the Regional
Basin Authority of the Sarno river (2002); iii) the IFFI Project of
the Campania Region – APAT (2006); iv) the Government
Commissionership for the Hydrogeological Emergency in
Campania region (2008). On the whole, about 130 landslide
phenomena were mapped; they cover the 30÷40% of the study
area. Figure 2 shows a synthesis of the abovementioned
cartographic products. It is worth to observe that all the official
documents were produced via different heuristic procedures and
they show landslide-affected areas located in different portions of
the slope. Starting from this controversial evidence, in order to
deepen the knowledge of the different kind of phenomena which
can occur on the slopes, field surveys and studies were firstly
carried out following a multidisciplinary approach (involving
_________________________
LEONARDO CASCINI (*), SILVIO DI NOCERA (**), FABIO MATANO (**), MICHELE CALVELLO (*),
SABATINO CUOMO (*) & SETTIMIO FERLISI (*)
(*) Dipartimento di Ingegneria Civile, Università di Salerno,
l.cascini@unisa.it; mcalvello@unisa.it ; scuomo@unisa.it; sferlisi@unisa.it.
(**) Dipartimento di Scienze della Terra, Università di Napoli “Federico II”,
sildinoc@unina.it; matano@unina.it
This work was carried out within the PRIN 2007 Project on “Analysis and
susceptibility and hazard zoning for landslides triggered by extreme events
(rainfall and earthquake)”.
573
competences on geology, morphology, hydrogeology, historical
data treatment, geomatics, geostatistics, etc.).
The results of these activities allowed to establish that the
zone at the toe of the hillslope is affected by hyperconcentrated
flows, landslides on open slopes and flowslides.
Fig. 1 – Studied area.
The hyperconcentrated flows were originated, during autumnwinter
periods of the 19 th century, by the washing of the air-fall
products of the explosive activity of the Vesuvius volcano. In this
regard, a strict correlation exists between the eruption events
whose related isopachs interested the study area and the
hyperconcentrated flows occurred some weeks after the
deposition of the volcano products on the Monte Albino slopes.
Since the last century, the hyperconcentrated flows have been
essentially related to erosion processes interesting the pyroclastic
soils covering the slope surface, being strongly reduced the
Vesuvius activity. The landslides on open slopes essentially affect
the triangular facets located at the base of the slopes; they may
have similar characteristics to the phenomena occurred on March
2005, classifiable as “debris avalanches” (HUNGR et alii, 2001).
Finally, the flowslides can be triggered in some areas located
in the upper part of Monte Albino massif. The magnitude of the
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displaced masses could be significantly increased by the materials
eventually entrained during the post-failure stage.
Fig. 2 - Landslides mapped in official documents.
On the basis of the results achieved during the above
described activities, a new landslide inventory map was produced
at 1:25.000 scale by adopting the criteria suggested by FELL et al.
(2008b). In particular, thanks to the availability of both data
recorded during the field surveys and aerial photographs, only the
landslide-affected areas, which are still recognizable on the basis
of geological and geomorphological criteria, were mapped. In
this regard, difficulties usually arise considering that the soil
cover involved in the occurred first-failure landslides are of small
thickness; as a consequence, the morphological signs of the
landslide-affected areas become difficult to be identified, often
starting from a few years from the dates of occurrence. Nowadays
only a limited number of phenomena can be detected on the
Monte Albino slopes; in particular, only those occurred in the last
century and, specifically, in the last decades. In the newly
produced inventory map (Fig. 3) are reported the areas (11)
affected by the landslides occurred on March 2005 as well as
those (13) involved by previous events which are still
recognizable. These latter landslides essentially occurred on open
slopes (as in the case of 2005 event) or on the sides of mountain
river beds, in the lower part of natural gullies. It is worth noting
that the number of the mapped landslides is in agreement with the
information gathered on the basis of collected historical data on
events occurred in the last century.
The significant mismatch among the available inventory maps
(Fig. 2) as well as among these latter and that produced in the
present work (Fig. 3) may be related to: i) the complexity of the
phenomena to be analysed; ii) the differences in the adopted
574
approaches (sector-based or multidisciplinary) and procedures
sometimes drastically conditioned by a subjective interpretation
of the input data. Finally, it is worth observing that, in some of
the available landslide inventories, the mapping was carried out
also considering the areas potentially affected by first-failure
phenomena which can occur in the future; however, this kind of
information should be conveniently reported in the landslide
susceptibility maps instead of in the inventories (FELL et al.,
2008b).
Fig. 3 – New landslide inventory map of the Monte Albino slopes. Legend:
red/pink -march 2005 landslide; green - post-1944 landslide; yellow - undated
landslide.
REFERENCES
ARDIZZONE F., CARDINALI M., CARRARA A., GUZZETTI F. &
REICHENBACH, P. (2002) – Impact of mapping errors on the
reliability of landslide hazard maps. Natural Hazards and
Earth System Sciences, 2, 3–14.
FELL R., COROMINAS J., BONNARD CH., CASCINI L., LEROI E., &
SAVAGE W.Z. (2008b) – Guidelines for landslide
susceptibility, hazard and risk zoning for land use planning.
Engineering Geology, 102, 85-98.
FELL R., COROMINAS J., BONNARD CH., CASCINI L., LEROI E. &
SAVAGE W.Z. (2008a) – Guidelines for landslide
susceptibility, hazard and risk zoning for land-use planning.
Commentary. Engineering Geology, 102, 99-111.
HUNGR O., EVANS S.G., BOVIS M.J., HUTCHINSON J.N. (2001) –
A review of the classification of landslides of the flow type.
Environmental & Engineering Geosciences, 7 (3), 221-238.
VAN WESTEN C.J., SEIJMONSBERGEN A.C. & MANTOVANI F.
(1999) – Comparing landslide hazard maps. Nat. Haz., 20,
137–158.

Lithotechnical characterization for debris flow triggering analysis in
South-Western Alps (Cuneo-Italy).
Key words: Cuneo (Italy), debris flow, lithotechnical
characterization, Hoek & Brown classification, Southwestern
Alps.
INTRODUCTION
This study investigates rapid channelized debris-flow related
to rainfalls in small alpine basins. Its goal is to evaluate and to
correlate different geological and technical aspects with
predisposing and triggering factors that can control these
phenomena.
The most studies place the triggering factor as short, intense
rainfall often associated with a certain quantity of rainfalls before
the event. Based on the type of weather forecast, this type of
report allows users to issue warnings or even evacuation bulletins
for high-risk weather conditions.
This paper tries to concentrate on other parameters, besides
those concerning the climate, which act as predisposing factors or
indexes of certain phenomena both in terms of magnitude and
recurrence interval. In fact, other authors tried to associate
different types of phenomena with: bedrock characteristics (LIN
et alii, 2000), geotechnical characteristics of deposits in the
source areas (BONNET-STAUB, 1998), basin morphometry,
topography of source area and debris flow accumulations
(WIECZOREK et alii, 1997).
MATERIALS AND METHODS
The study area is placed in southern Piedmont within the
Maritime and Ligurian Alps. Regarding to the geological setting,
this area is characterized by the presence of several rock
formations belonging to the Helvetic and Penninic Domains, here
represented respectively by a portion of the Argentera Massif in
_________________________
(*) Dipartimento di Scienze Mineralogiche e Petrologiche, Università degli
Studi di Torino, sara.castagna@unito.it
(**) Dipartimento di Scienze della Terra, Università degli Studi di Torino,
giuseppe.mandrone@unito.it
SARA ELISA DOMENICA CASTAGNA (*) & GIUSEPPE MANDRONE (**)
575
the SW part of the study area, and by the Brianzonese –
Subbrianzonese Domains and by Piemonte Zone of calcschists in
the central and NE part. The first is constituted by igneous and
metamorphic rocks as gneiss, granites and migmatites; the others
are mostly made of sedimentary rocks, as limestones, dolostones,
sandstones and flysch.
Starting from geological data, a lithotechnical characterization
of study area was realized, by attributing to each rock formation a
GSI (Geological Strength Index) value, according to Hoek &
Brown failure criterion (MARINOS &HOEK, 2001; HOEK et alii,
2002). GSI, both in its first formulation than in its later
modification for heterogeneous rock mass types such as flysch,
represents a quality index of rock masses, based on interlocking
of rock pieces and on discontinuities surface quality.
A lithotechnical map of the study area was realized (Fig.1):
igneous rock masses show the higher GSI value, while, as
expected, flysch and heterogeneous rock masses, with sandstones,
shale, and carbonatic terms, correspond to the lower values.
A geomorphological approach to the study led to the
identification of the alluvial fans, with their drainage basin, in the
study area, especially thanks to aerial photointerpretation
techniques. In each basin the percentage of outcropping substrate
and its main mineralogical composition (silicate, carbonate,
heterogeneous, chalk) were estimated.
PRELIMINARY RESULTS
By combining the realized lithotechnical map with surface
extent of alluvial fan, drainage basins and substrate outcropping
areas, it was possible to relate morphological features of alluvial
fans with mineralogical and geotechnical characteristics of
drainage areas.
First results show that where the drainage basin is mostly
covered by detritic deposits the ratio between the fan area and the
basin area is greater than in the other cases, with a major
percentage of substrate outcropping.
In this situation, it can be observable that basins with a great
percentage of carbonate and heterogeneous rock masses
outcropping, show the minor values of the same ratio.
Further considerations and analyses will be expected about
this matter and moreover also the hydrogeological and
meteorological approach will be considered. In fact, the
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Fig.1 – Lithotechnical map of the study area. GSI value assigned to rock formations outcropping in the study area, differed on the main mineralogical
composition: A) carbonate; B) heterogeneous; C) chalk; D) silicate; E) Quaternary deposits (GSI = 0).
infiltration mechanism of precipitation water is strongly
connected to debris flow triggering. In order to understand how
water infiltrates into the ground in the study area, instruments for
the measure of both the weather events and variations of water in
soil will be planted on the field.
Installation of weather stations, electric piezometers and soil
moisture profiler at various depths in the ground will be used to
define how the soil responds to weather, thus correlating the
weather conditions less favorable to slope stability with different
types of covers.
REFERENCES
BONNET-STAUB I. (1998) - Définition d’une typologie des dépôts
de laves torrentielles et identification de critères
granulométriques et géotechniques concernant les zones
sources. Bull. Eng. Geol. Env., 57, 359–367
576
LIN C.W., WU M.C. & SHIEH C.L. (2000) - Influence of geology
on debris-flows: Examples from Hsin-Yi, Nantou County,
Taiwan. In: G. Wieczorek and Naeser (Eds): Debris flow
hazard mitigation: mechanics, prediction and assessment.
Proc. 2° Int. Conf. on debris-flow, Taiwan, 221-229.
HOEK E., CARRANZA-TORRES C. & CORKUM B. (2002) – Hoek-
Brown criterion – 2002 edition. Proc NARMS-TAC
Conference, Toronto, 1, 267-273.
MARINOS P. & HOEK E. (2001) - Estimating the geotechnical
properties of heterogeneous rock masses such as flysch. Bull.
Eng. Geol. Env. (IAEG), 60, 85-92.
WIECZOREK G., MANDRONE G. & DECOLA L. (1997) The
influence of hillslope on debris-flow initiation. In: Cheg (ed):
Debris-Flow hazard mitigation: mechanics, prediction and
assessment”, Proc. 1° int. Conf. on debris-flow, San Francisco
(USA), 21-31.

Evaluation of reforestation effects through multitemporal
investigation in drainage basins affected by badland erosion,
Radicofani (Tuscany)
Key words: Badlands, erosion rate, geomorphological hazard,
multitemporal confrontation, Radicofani, reforestations,
River Paglia Unit.
INTRODUCTION
The Radicofani Basin is one of the structural depressions
(graben) trending NW - SE of southeastern Tuscany (LIOTTA,
1996), filled with Pliocene marine deposits. The municipality hill
area of Radicofani consists mainly of the early Pliocene clayey
sediments (River Paglia Unit). Slopes are often covered by
colluvial deposits produced by the volcanic neck of Radicofani,
consisting of late Pleistocene basalt – trachytic lavas of the
Tuscan Magmatic Province.
Fig. 1 – Reforestation with Cupressus arizonica and Pinus nigra on a slope
affected by badland erosion.
The slopes are widely affected by geomorphological hazard
consisting of very frequent badland erosion (CICCACCI et alii,
_________________________
(*) Università della Tuscia, fabio_castaldi@libero.it, chiocchi@unitus.it,
lporto@unitus.it
FABIO CASTALDI (*), UGO CHIOCCHINI (*) & LUIGI PORTOGHESI (*)
577
2008). In this scenario many reforestations were carried out in
the last fifty years with the aim at stabilizing slopes on about 320
ha of the municipal territory (Fig.1). Frugal conifers such as
Cupressus arizonica, Cupressus sempervirens, Pinus nigra and
Mediterranean pines planted in monospecific or mixed stands
were mainly used for these forest works.
The goal of our study is to evaluate through a
multidisciplinary approach the impact of reforestations on the
geomorphological instability of nine small drainage basins
belonging to the rivers Paglia and Formone watersheds. The
geological, geomorphological, hydrological and vegetational
characteristics were analyzed by a multitemporal confrontation
between the pre – reforestation and post – reforestation situations.
The results of our study are a valuable tool to improve both
knowledge of the historical morphological dynamics correlated to
forest vegetation and land planning and management.
METHODOLOGY
Each elaboration has been carried out for the year 1954 (pre -
reforestation) and year 2007 (post – reforestation).
A DEM from historical cartography was constructed and
compared with the actual DEM. The difference between the two
DEMs leads to estimate the erosion/deposition annual rates for
each drainage basin.
The aerial – photo interpretation allowed to define areas
affected by badland erosion and the results were reported on a
GIS to calculate the surface area.
The land use was described by the CORINE Land Cover
methodology (BOSSARD et alii, 2000) using the ortho - photo
interpretation. Furthermore the study of drainage networks on the
aerial – photo and GIS environment (Fig. 2) led to calculate the
hierarchal anomaly index and the indirect evaluation of
denudation rate index (CICCACCI et alii, 1980; DELLA SETA et
alii, 2007).
Fourteen circular sample plots of ten meters radius were
established in the five main forest types to work out the stand
such as number of stems, mean diameter, basal area, top height
and mean height. The forest survey allowed also to evaluate the
adaptability of the tree species used in the reforestations to clayey
substrate affected by a high geomorphological hazard setting.
SESSIONE 17

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The differences between the pre and post reforestation
situations are remarkable. The land use turns shift from a
widespread agriculture with particular attitude for oliviculture to
a more diversified land use where arable areas alternate with
pastures and agroforestry areas. The reforestations have led to a
good improvement and regularization of the hydrographic
network. Computation of the denudation rate index highlights this
trend for all studied small drainage basins.
Fig. 2 – DEM and drainage network of the torrent Cacarello (about 900 ha) .
REFERENCES
BOSSARD M., FERANEC J. & OTAHEL J. (2000) - CORINE land
cover technical guide. Addendum 2000. European
Environment Agency.
CICCACCI S., FREDI P., LUPIA PALMIERI E. & PUGLIESE F. (1980)
– Contributo dell’analisi geomorfica quantitativa alla
valutazione dell’entità dell’erosione nei bacini fluviali. Boll.
Soc. Geol. It., 99, 455 – 516.
CICCACCI S., GALIANO M., ROMA M.A. & SALVATORE M.C.
(2008) - Morphological analysis and erosion rate evaluation
in badlands of Radicofani area (Southern Tuscany - Italy).
Catena, 74, 87 - 97.
DELLA SETA M., DEL MONTE M., FREDI P. & LUPIA PALMIERI E.
(2007) - Direct and indirect evaluation of denudation rates in
Central Italy. Catena, 71, 21 - 30.
LIOTTA D. (1996) – Analisi del settore centro – meridionale del
bacino pliocenico di Radicofani (Toscana meridionale). Boll.
Soc. Geol. It., 115, 115 – 143.
578

Geotechnical characterization of the Macigno Fm. debris by
dynamic penetration tests in the Serchio River basin (Tuscany, Italy)
Key words: Debris covers, internal friction angle, landslide,
Macigno Fm., relative density.
Due to its structural-tectonic features, geographicmorphological
configuration, and climatic conditions, the Serchio
River basin is frequently interested by seismical events and
floods. Therefore, since the Eighties several studies and surveys
aimed at the reduction of seismical and hydrogeological risk were
carried out. The landslide hazard evaluation is of primary
importance for the territorial planning (DALLAN et alii, 1991;
D’AMATO AVANZI et alii, 1999). Moreover, previous studies
showed that the highest number of landslides in this basin occurs
where argillitic rocks and sandstones (Macigno Fm.) crop out, or
they involve debris materials (CANCELLI et alii, 2002; D’AMATO
AVANZI et alii, 1999, 2002, 2004).
The main purpose of this study is to provide a contribution to
the study of the mechanical strength properties of the debris
covers of the Macigno Fm. (sandstone interbedded by phyllite),
which can be involved in instability phenomena, mainly by soil
slip-debris flow (Fig. 1) during intense rainfall (D’AMATO
AVANZI et alii, 2002, 2004). These slope materials exhibit a great
textural variability, either vertical or lateral; however, they are
commonly composed by sandy-pebbly composition, with minor
silty-clayey fraction. The knowledge of physic-mechanical
properties of these materials is very important in order to
comprehend the conditions that trigger landslides in case of both
rainy and seismical events. On the other hand, the Macigno Fm.
is particularly widespread in the Serchio River basin.
The activity was carried out by research and elaboration of the
raw data obtained by means of penetration tests (DPT) (medium
and super-heavy penetrometers), standard penetration tests (SPT),
in order to determine the typical values of the internal friction
angle f p (°) and the relative density Dr (%). In fact, due to the
low costs and time of analysis, the penetration test is one of the
most used techniques in order to obtain an approximate
reconstruction of the underground model and the soil parameters.
_________________________
GIACOMO D’AMATO AVANZI (*), SUSANNA DUCHI (*), YURI GALANTI (*),
ROBERTO GIANNECCHINI (*) & DIEGO LO PRESTI (**)
(*) Dipartimento di Scienze della Terra, Università di Pisa,
galanti@dst.unipi.it
(**) Dipartimento di Ingegneria Civile, Università di Pisa
579
Fig. 1 - Soil slip-debris flow triggered in the debris covers of the
Macigno Fm. near Fosciandora Village (LU).
The results of the dynamic penetration tests were afterwards
related to the mechanical strength properties of the debris covers
by means of empirical methods used for granular materials. In
particular, the relative density was determined using the
correlation proposed by SKEMPTON (1986), while the
SCHMERTMANN (1978) relation was used in order to obtain the
internal friction. Figure 2 shows the trend of debris internal
friction angle at different depths. These values are typical of the
sediments studied, in particular fine sand, medium sand with
gravel and sand and gravel.
These data were compared with those obtained by means of
direct shear tests, reaching a good agreement (Fig.3).
In conclusion, this study contributes in determining the typical
values of the friction angle and the relative density of the
Macigno Fm. cover materials by means of commonly used and
money saving indirect methods.
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depth (m)
internal friction angle (°)
0
1
2
3
4
5
6
7
8
9
10
11
50
45
40
35
30
25
20
15
10
internal friction angle (°)
0 5 10 15 20 25 30 35 40 45 50
5
0
Fine Sand
Medium Sand with Gravel
Sand & Gravel
Fig. 2 - Internal friction angle trend at different depths for the sediments
analyzed.
direct shear test
DPT test
SPT test
Fine Sand Medium Sand with Gravel Sand & Gravel
Fig. 3 - Comparison between the internal friction angle values obtained by
direct shear tests, DPT test, and SPT tests for the materials analyzed.
REFERENCES
CANCELLI A., D’AMATO AVANZI G., POCHINI A. & PUCCINELLI A.
(2002) - Caratterizzazione geologica e litologico-tecnica
delle piane del Serchio e della Turrite Secca in prossimità di
Castelnuovo di Garfagnana (Lucca). Riv. It. Geot., 3, 17-32.
DALLAN L., NARDI R., PUCCINELLI A., D’AMATO AVANZI G. &
TRIVELLINI M. (2002) - Valutazione del rischio da frana in
Garfagnana e nella Media Valle del Serchio (Lucca). 3)
Carta geologica e carta della franosità degli elementi
“Sillano”, “Corfino”, “Fosciandora” e “Ceserana” (scala
1:10.000). Boll. Soc. Geol. It., 110, 245-272.
D’AMATO AVANZI G., PIERONI A. & PUCCINELLI A. (1999) -
Valutazione della pericolosità delle frane in aree a maggior
vulnerabilità del Bacino del Fiume Serchio (Toscana). Atti
Conv. Lincei, 154, 175-181.
580
D’AMATO AVANZI G., GIANNECCHINI R. & PUCCINELLI A. (2002)
- I movimenti franosi del novembre 2000 nella provincia di
Lucca: osservazioni preliminari. Atti Conv. “Il dissesto
idrogeologico: inventario e prospettive”, Roma, Atti Conv.
Lincei, 181, 365-377.
D’AMATO AVANZI G., GIANNECCHINI R. & PUCCINELLI A. (2004)
- The influence of the geological and geomorphological
setting on the shallow landslides. A typical example in a
temperate climate environment: the 19 th , 1996 catastrophe un
the north-western Tuscany (Italy). Eng. Geol., 73, 215-228.
SHMERTMANN J.H. (1978) - Guidelines for cone penetration test
performance and desingn. U.S. Dep. Of Transportation,
FHEA, R 78-209, Washington D.C. (USA).
SKEMPTON A.W. (1986) - Standard penetration test procedures
and effects in sands of overburden pressure, relative density,
particle size, aging and overconsolidation. Geotechnique, 3,
425-447.

Geomechanical features and landslide susceptibility of rock
formations in Northern Tuscany (Italy)
GIACOMO D’AMATO AVANZI (*), FRANCESCO FALASCHI (**), ROBERTO GIANNECCHINI (*),
DARIA MARCHETTI (*), ALBERTO POCHINI (*) & ALBERTO PUCCINELLI (*)
Key words: Geomechanics, landslide, Northern Apennines.
Several different geological formations crop out in the
Northern Tuscany (Italy), where the geological, morpho-climatic
and seismic characteristics determine high landslide
susceptibility. This study particularly focuses on the upper
Serchio River basin, where slope instability severely threatens
population, villages and facilities. Geo-engineering survey and
characterization with in situ and laboratory tests were performed,
Tab. 1 - The main geotechnical units cropping out in the study area.
_________________________
(*) Dipartimento di Scienze della Terra, Pisa, damato@dst.unipi.it
(**) Autorità di Bacino del Fiume Serchio, Lucca, segreteria@bacinoserchio.it
581
in order to define rock mass classification and geotechnical
properties of the most widespread rocky formations cropping out
in the basin, and assess their relationships with slope instability.
Therefore, several properties were investigated, mainly
referring to rock strength, structure, spacing and conditions of
discontinuities, alteration. Field and laboratory tests were
performed and included Schmidt Hammer Test, Point Load
Strength Test and Unconfined Compressive Strength, aiming at
defining the main rock and rock mass parameters. Then, the
Bieniawski’s RMR (Rock Mass Rating) and the Hoek’s GSI
(Geological Strength Index) were applied, in order to obtain an
overall rock mass parameterization.
Thus many dozens of geotechnical units were established and
grouped according to their behaviour. Figure 1 in the next page
depicts the areal distribution of the 13 main geotechnical units.
Table 1 lists these units together with some related
lithostratigraphic unit, and summarizes their geotechnical
properties.
Subsequently, the study area was classified and subdivided
into several classes, mainly based on their physical-mechanical
properties. This allowed to realize a GIS-based geotechnical map
of the considered area, representing the areal distribution of the
geotechnical properties of the classified rock formations. Finally,
this map was compared with the landslide distribution of the area,
in order to assess the landslide susceptibility of the considered
formations.
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Fig. 1 - Areal distribution of the 13 main geotechnical units in the study area (see Tab. 1 for the meaning of the numbers).
582

_________________________
The landslides triggered by the December 2009 meteorological
events in North-Western Tuscany (Italy): first results
Fig. 1 - Location map of Lucca and Pistoia Provinces.
GIACOMO D’AMATO AVANZI (*), YURI GALANTI (*) & ROBERTO GIANNECCHINI (*)
Key words: Flood, landslide, North-Western Tuscany, rainfall,
snowfall.
Heavy precipitation (rainfall and also abundant snowfalls
from December 18 to 21 at sea level as well) occurred in North-
Western Tuscany in December 2009. Such precipitation caused
floods and landslides in the Serchio River Valley, in Versilia
(Lucca Province) and in the Pistoia Apennine (Pistoia Province).
The Serchio River was interested by a discharge up to 1900
m 3 /s (NARDI, 2010), breaking the embankments and causing
floods in the Lucca and Pisa plains (about 30 km 2 of flooded
ground, Fig. 1).
The abundant rainfall associated with the rapid snow melting
determined limit equilibrium conditions in a lot of slopes in the
study area. Many slopes collapsed during the subsequent heavy
rainfall events on December 22-23 and, mainly, on December 24-
25.
Altogether in December 2009 the total rainfall amount was
very high. The highest values were reached at the Campagrina
raingauge (Apuan Alps, 997.8 mm) and at the Pracchia raingauge
(Pistoia Apennine, 676.8 mm). Throughout the considered area
(*) Dipartimento di Scienze della Terra - Università di Pisa,
galanti@dst.unipi.it
583
the total rainfall of December 2009 corresponds to the 30% of the
annual average precipitations. Unfortunately, the lack of a
snowgauge in the regional monitoring network does not enable
accurate snowfalls estimation. However, the rapid snow melting
might have had a significant role in determining the slope
instability conditions. This phenomenon was also caused by rapid
increase of the minimum temperature (from -3.2 °C on December
20 to +11.9 °C on December 23 recorded at the thermometric
station of Seravezza, Versilia) and by subsequent heavy rainfall
(Fig. 2).
Fig. 2 - Comparison between daily rainfall and temperature respectively
recorded at Cardoso raingauge (Versilia) and at the thermometric station of
Seravezza (Versilia) (data by Tuscany Region Hydrologic Service).
The most damaging rainfall event occurred during the night
between the 24 and 25 December. From 9 p.m. on 23 to 11 a.m.
on 25 uninterrupted rainfalls were recorded. In particular, the
precipitation reached the maximum intensity from 12 p.m. on 24
to 3 a.m. on December 25, recording 263.8 mm and 164.6 mm at
the Campagrina and Fabbriche di Vallico stations, respectively. A
similar event occurred in the Pistoia Apennine where, from 12
p.m. on December 24 to 4 a.m. on 25, 169.2 mm were recorded at
the Pracchia raingauge.
The December 2009 events caused over 600 landslides in the
North-Western Tuscany. These landslides were mostly classified
as rapid shallow movements (complex, translational debris slideflow),
also known as soil slip-debris flows (Fig. 4). Such
landslides are typical of particularly intense rainfall in this area
SESSIONE 17

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(D’AMATO AVANZI et alii, 2002, 2004). However, in some cases
different types of movements also occurred (rock and debris
translational slides and rotational-translational slides; Fig. 5)
A lot of landslides were of first generation, and mainly
involved the debris-colluvial covers of the slopes (few decimetres
to some meters thick). In rare cases, the landslides involved the
most deformed and fractured portion of the bedrock. In general,
the landslides bedrock is mainly constituted by sandstone
(Macigno Fm.), metamorphic sandstone and siltstone
(Pseudomacigno Fm.) and by phyllite and schist (Apuan
Metamorphic Complex).
Fig. 3 - Hourly rainfall recorded from December 22 to 25 at the Pracchia
raingauge (data by Tuscany Region Hydrologic Service).
Fig. 4 - Soil slip-debris flow triggered on the eluvio-colluvial slope cover in
the Serchio Valley near the Castelnuovo Garfagnana village (LU).
584
In conclusion, the December 2009 landslides were determined
by multiple and concomitant triggering factors. The rapid snow
melting might have played an important role (at present not
quantified) in determining instability conditions and collapses of
the slopes, where the rainfalls were more intense. In addition,
several landslides, still triggered by the extreme events, involved
the road network, whose surface water drainage system is often
obsolete, inadequate or absent.
Fig. 5 - Rotational-translational slide involving fractured rock and debris in
the Reno Valley near Pracchia village (Pistoia Apennine).
REFERENCES
D’AMATO AVANZI G., GIANNECCHINI R. & PUCCINELLI A. (2002)
- I movimenti franosi del novembre 2000 nella provincia di
Lucca: osservazioni preliminari. Atti del Convegno “Il
dissesto idrogeologico: inventario e prospettive”, Accademia
Nazionale dei Lincei, 181, 365-377.
D’AMATO AVANZI G., GIANNECCHINI R. & PUCCINELLI A. (2004)
- The influence of the geological and geomorphological
settings on the shallow landslides. A typical example in a
temperate climate environment: the June 19 th , 1996
catastrophe in the north-western Tuscany (Italy). Eng. Geol.,
73 (3-4), 215-228.
NARDI R. (2010) - Le rotture arginali del fiume Serchio durante
la piena del 25 dicembre 2009. Geoitalia, 30, 34-37.

Slope stability analysis of the S. Maria in Castello sanctuary's rock
(Vecchiano, Tuscany, Italy): geomechanical characterization and
distinct elements numerical modeling
GIACOMO D'AMATO AVANZI (*), DARIA MARCHETTI (*) & ALESSANDRO DE ROSA (*)
Key words: Instability, numerical modeling, quarry, Vecchiano.
Vecchiano is located in the northern part of the Pisa plain, just
at the foot of D'Oltre Serchio mounts.
During the 20 th century the landscape surrounding this village
Fig. 1 – Numerical model of a quarry wall's portion. The arrows indicates
the vector's versus, direction and intensity of the single blocks.
has been deeply modified by intense extractive activities.
Large and vertical quarry walls, affected by serious instability
problems, are the most visible legacy of those activities
(TONGIORGI et alii., 1982).
The investigations of this graduation thesis concern a quarry
that is located below the S. Maria in Castello sanctuary, adjacent
to the northern boundary of Vecchiano.
This quarry represents a menace for ecology and people,
because of the degraded conditions of the floor, and the serious
instability problems of the walls (MAZZANTI, 1988).
This site is a prior case to include in PAERP project
(Provincial Plane of Extraction Activities) of the Provincia di
Pisa.
Geo-engineering techniques permitted to advance new
hypothesis about the revaluation of the quarry.
_________________________
(*) Dipartimento di Scienze della Terra, Pisa, damato@dst.unipi.it
585
Measures of recovery and instability reduction are proposed
to increase the safety of the area.
Several different steps leaded to summarize the geologic
previous knowledge of the area and to examine in deep structural
and geomechanical aspects of the rock mass (D'Amato & Nardi,
1993).
The study started with the collection of preliminary
information concerning historical, geologic-structural and
geomorphological information of the area.
Subsequent in situ activities included survey on a detailed
scale, collection of photos and rock samples, geometric
measurements and Schmidt hammer tests.
Different laboratory activities, such as uniaxial compression
tests (Point load test) and geomechanical classifications of the
rock mass, permitted to obtain cohesion and friction angle values.
All collected data have been used with GIS (Geographic
Information System) and numerical analysis software (UDEC
4.0).
The geological model created with these software include
quarry face instabilities and slope stability analysis, taking into
account slipping and overturning movements.
REFERENCES
D’AMATO AVANZI G. & NARDI I. (1993) – Indizi di neotettonica
nei monti d’Oltre Serchio: faglie distensive recenti al bordo
della pianura pisana e depositi ciottolosi a quota 170 metri.
Boll. Soc. Geol. It., 112, 601-614.
MAZZANTI R. (1988) - Geomorfologia del comune di Vecchiano.
In: "Il fiume, la campagna, il mare. Reperti, documenti,
immagini per la storia di Vecchiano". Comune di Vecchiano.
Bandecchi & Vivaldi, Pontedera (PI), 23-46.
TONGIORGI M., ALBANI R. & GUELFI F. (1982) - Studio geologico
sulle cave dei Monti Pisani. Associazione intercomunale
"Area Pisana" n°12. Dipartimento di Scienze della Terra,
Università di Pisa.
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The use of flash flood events in fluviokarst canyons to evidence
loosing reaches through hydrological modeling and empirical peak
flow estimation
Key words: Central East Sardinia, flash floods, loosing reaches,
modelling, peak flow estimation.
INTRODUCTION
Flash flood events in fluviokarstic catchments are difficult to
model because of their hydrological complexity. This type of
modelling is even more challenging for ungauged rivers (DE
WAELE, 2008; NORBIATO et alii, 2009). Moreover, in carbonate
areas, part of the precipitation and resulting superficial flow is
rapidly transferred underground, and quantifying this karst
aquifer recharge from stream losses is an extremely difficult task
(CARTER &DRISCOLL, 2006). Also some karst systems not only
withdraw water from the surface flow but can in later stages of a
flood return part of the water to the surface streams (BAILLY-
COMTE et alii, 2009). This can make peak discharge estimates in
karst areas even more complicated.
This research has analysed a few exceptional meteorological
events that occurred in central-east Sardinia since December
2004 and triggered flash floods in the main rivers and especially
in some karst canyons. One of the aims of this study was to
compare the modelled peak flow results with the empirical ones
in order to localise sinking (or rising) stream reaches and to
estimate the amount of water loss (or gain) along the karstic
stream channel. The obtained results can then be compared with
the speleological knowledge.
_________________________
(*) Italian Institute of Speleology, Department of Earth Science, University
of Bologna, jo.dewaele@unibo.it
(**) Department of Earth Science, University of Bologna,
mario.martina@unibo.it
(º) Water Resources and Environmental Geology Research Group,
University of Almeria, lsanna@ual.es
(°°) Sardinian Environmental Protection Agency, Sassari
(§) Gruppo Archeo Speleo Ambientale Urzulei, Associazione Speleologica
Progetto Supramonte
JO DE WAELE (*), MARIO L.V. MARTINA (**), LAURA SANNA(º),
ANTONELLO COSSU (°°) & SALVATORE CABRAS (§)
586
The research has been carried out in two canyons, Codula
Ilune and Riu Flumineddu (DE WAELE et alii, 2010), where
underground karst is rather well known, and in another river,
Codula di Sisine, where speleological knowledge is rather scarce.
METHODS
Many authors have tried to develop methods to estimate peak
discharges of rivers without relying on accurate rainfall
observational data (COSTA, 1987; JOHNSON & WARBURTON,
2002). These methods include combinations of geomorphological
field reconnaissance (e.g., high water marks) and
sedimentological data (e.g., cobble size).
Field measurements have been carried out at 8, 13 and 23
river transects carefully chosen respectively along Codula Ilune,
Riu Flumineddu and Codula di Sisine valleys. The major flash
floods for the first two have occurred in December 2004, while
Codula di Sisine experienced its most severe flood in November
2009. Measurements include flood water slope (S), high water
marks, wetted perimeter (P), cross-sectional area (A), and mean
diameter of the largest by the flood transported boulders (di).
Peak discharge can be obtained using the Manning equation:
v = 1/n S 1/2 (A/P) 2/3
where n is the roughness coefficient calculated using the
following equation (JARRETT, 1984):
n = 0.32 S 0.38 ·R -0.16
The minimum velocity of flood water can also be estimated
using the following equation (COSTA, 1983):
v = 0.18 di 0.487
The peak flow Q can easily be obtained using the continuity
equation:
Q = v A
The results obtained with these empirical methods can then be
compared with those obtained by a distributed hydrological
model (TOPKAPI) (CIARAPICA &TODINI, 2002) based on the
available rainfall data and physical characteristics of the drainage

asin. The TOPKAPI model proposed is structured around three
basic modules that represent, in turn, the soil water component,
the surface water component, and the channel water component
(drainage network component). The parameter values of the
model are shown to be scale independent and are obtainable from
digital elevation maps, soil maps, and vegetation or land use
maps in terms of slopes, soil permeability, topology, and surface
roughness. In this model an 80% loss due to diffuse rainfall
infiltration into the carbonate outcrops has been considered, in
order to obtain similar peak flows between the empirical methods
and the model before the rivers enter the carbonate areas. Since
the hydrological model does not take into account the river losses
(through sinks), the difference between modelled peak flows and
those obtained by the empirical methods are considered to be
representative of river loss estimates.
RESULTS
Measurements and results are reported in Table 1.
Table 1 – Measurements
River Nº
transects
Surveyed
River length
(km)
Max
peak
flow
(m 3 /s)
Total
loss
(m 3 /s)
Flumineddu 13 12 2500 200
Ilune 8 5.5 1700 900
Sisine 23 7.5 1100 500
In the two rivers where speleological knowledge is in a rather
advanced stage, river losses correspond to places where
important sinkholes and subterranean rivers are known. In
Flumineddu an estimate of water flow in the caves during the
flood, based on the dimensions of the cave passages and the
height reached by the flood waters, corresponds rather well with
the estimated water losses.
Also in Codula Ilune most of the water disappears close to the
contact between dolostones and granites, where the underground
river that flows in the biggest known cave system of Sardinia
reaches peak flows four times bigger than in the Flumineddu
caves. Cave passages in this karst system, in fact, are four times
the size of those explored in the Flumineddu canyon.
In Sisine no major river sinks are known, probably covered by
alluvium, although some large cave systems that discharge fresh
water into the sea are present along the coast. The loosing river
reaches seem to be concentrated in the probable feeding areas of
these submarine springs.
CONCLUSIONS
This research has shown the possibility of recognising sinking
stream sections in fluviokarstic canyons confronting peak flow
587
estimates from a hydrological model (that does not take into
account sinks along the river beds) and empirical methods (that
allow to estimate real peak flow along carefully chosen river
transects). This experimental method has allowed to recognise
known sinking stream sections in two areas where speleological
knowledge has confirmed underground water flow, and has put in
evidence loosing stream sections in a canyon (Sisine) where
underground flow has not yet been discovered. This opens new
perspectives in the identification of most probable areas where
underground flow appears to be concentrated, thus probably
hosting important and still unexplored cave systems.
REFERENCES
BAILLY-COMTE V., JOURDE H. & PISTRE S. (2009) -
Conceptualization and classification of groundwatersurface
water hydrodynamic interactions in karst
watersheds: case of the karst watershed of the Coulazou
River (Southern France). J. Hydrol., 376, 456-462.
CARTER J.M. & DRISCOLL D.G. (2006) - Estimating recharge
using relations between precipitation and yield in a
mountainous area with large variability in precipitation.
J. Hydrol., 316, 71-83.
CIARAPICA L. & TODINI E. (2002) - TOPKAPI: a model for
the representation of the rainfall-runoff process at
different scales. Hydrol. Proc., 16, 207-229.
COSTA J.E. (1983) - Paleohydraulic reconstruction of flashflood
peaks from boulder deposits in the Colorado Front
Range. Geol. Soc. Am. Bull., 94, 986-1004.
COSTA J.E. (1987) - Hydraulics and basin morphometry of
the largest flash floods in the coterminous United States.
J. Hydrol., 93, 313-338.
DE WAELE J. (2008) - Interaction between a dam site and
karst springs: the case of Supramonte (central-east
Sardinia, Italy). Eng. Geol., 99, 128-137.
DE WAELE J., MARTINA M.L.V., SANNA L., CABRAS S. &
COSSU A. (2010) - Flash flood hydrology in karstic
terrain: Flumineddu canyon, central-east Sardinia.
Geomorphology, 120, 162-173.
JARRETT R.D. (1984) - Hydraulics of high-gradient streams.
J. of Hydraul. Eng., 110, 1519-1539.
JOHNSON R.M. & WARBURTON J. (2002) - Flooding and
geomorphic impacts in a mountain torrent: Raise Beck,
Central Lake District, England. Earth Surf. Proc.
Landforms, 27, 945-969.
NORBIATO D., BORGAM. & DINALE R. (2009) - Flash flood
warning in ungauged basins by use of the flash flood
guidance and model-based runoff thresholds. Meteorol.
Applic., 16, 65-75.
SESSIONE 17

SESSIONE 17
The event of November 10, 2009 at Casamicciola on the island of
Ischia. A report on the interaction between flooding and landslides
SOSSIO DEL PRETE (*), GIUSEPPE DI CRESCENZO (**) , LUCA DI IORIO (°) & ANTONIO SANTO (°°)
Key words: Flooding, flow-type landslides, Southern Italy.
The island of Ischia is particularly susceptible to landslides
and flooding because of its geological-structural and geomorphological
settings. The urbanisation over recent decades
coupled with the development of tourism on the island, has
increased the risk factors. In particular, the susceptibility of the
area is mainly associated with rock fall, flow-like landslides and
rapid flooding of sediment of varying degrees of concentration.
In the last century the island has been repeatedly affected by
natural disasters, including the one in October 1910 which
interested the northern slope of Mount Epomeo, where hyperconcentrated
flows invaded the town of Casamicciola sowing
death and destruction. In the same area a strong alluvial event
occurred in November 10, 2009.
After the event, a detailed geo-morphological survey was
conducted (scale 1:2000) in order to better understand the
interaction between the flood event and the gravitational
phenomena. The study was conducted on the two catchment areas
(Ervaniello and Sinigallia) that have the closing section near the
Casamicciola town (Piazza Bagni).
Therefore all landslides present on the slopes of valleys were
mapped and an estimate of the volume of material involved
during detachment and sliding was calculated. At the same time,
all areas of accumulation were also mapped differentiating, where
possible, landslide bodies from flood deposits. In the foothills
area, near the town and towards the sea, the pathways of the flows
were reconstructed in some detail from the observation of
hydraulic rods, the movement of sediment and related topics with
the help of many videos recorded shortly after the start of the
event and during the same.
Pluviometric data were also analysed and, in particular, the
hourly rainfall rate has been linked with the flow stream. This
allowed an estimate with a good degree of accuracy of the run-off
times from the watersheds.
_________________________
(*) Geologist, dpsossio@alice.it
(**) Phd, University of Naples Federico II, g.di.crescenzo@alice.it
(°) Geologist, drigpp@alice.it
(°°) Department of Hydraulic, Geotechnical and Environmental
Engineering, Applied Geology Division, University of Naples Federico II,
santo@unina.it
588
The data collated resulted in a dynamic reconstruction of the
flood event which struck the town of Casamicciola. It was a
complex phenomenon which is caused by a landslide
characterised by a source area localised in the mountain areas
prone to flood flows. Growing urbanisation and the development
of geo-morphological conditions of the basins have been
contributing factors. An understanding of the trigger factors and
further development of these phenomena in specific contexts such
as those on Ischia are crucial for a more correct analysis of the
susceptibility and mitigation of risk.

The multi-disciplinary approach to studying the evolution of
landslides: the example of Pescacci flow in the Miocene-Pliocene
Marchean pre-apennine (central Italy)
Key words: Landslides, Marche region, Miocene-Pliocene
deposits, multidisciplinary approach.
In this work we presented the geomorphological analysis in a
area affected by a recent landslides characterized by a presence of
Pliocene marine deposits in the Marchean preapennine (Pescacci
locality in the Serra San Quirico territory).
More emphasis is attributed at the historical study because the
landslide, in the time, determined a progressive alteration both
slope profile and superficial hydrological conditions, with
creations of different edges scarp, steps, trenches, water
emergencies, etc. and other particularities as increasing of the
floristic and vegetation variety (Fig.1).
Fig. 1 – Pescacci locality in the Serra San Quirico territory
The evolution of this landslides is characterized by different
velocity in the time; in particular is possible to define a
movement with step alternating with different phases
characterized by quiescence. Recent reactivation produce
different phenomena: in upper part of area is possible to
recognize more slides of different block that affected the body of
ancient landslide; in the lower part the materials regarding the
_________________________
(*) Scuola di Scienze Ambientali, Università di Camerino,
piero.farabollini@unicam.it
(**) Geologo, libero professionista, Cerreto d’Esi (AN)
(°) Università Politecnica delle Marche, Università di Ancona
PIERO FARABOLLINI (*), MARIO MENTONI (**) & MARINA ALLEGREZZA (°)
589
body of ancient landslides is affected by a new flow.
The first maps and documents of this landslide date the
creation of this movement by a slope process that involve the
terrain during the first phase of XIX Century; previously, other
maps, dated around the XVIII Century, show the presence of a
small lake at the end of body of landslide named Fusiano lake
(Fig.2). Actually this lake is missing.
Fig. 2 – Ancient map of Rocca Contrada, in which the Fusiano Lake is
indicated (circle).
The different approach (geological, geomorphological,
historic, floristic-vegetation and the analysis with comparison of
different aerophotographs) testified the diachronic evolution of
this movement, with particular regards of the ratio of escarpment
retreat, and the interference with the fluvial dynamic and other
fluvial modification (in particular with the genesis of small lake,
the modification of fluvial profile of stream, and other different
fluvial irregularities).
SESSIONE 17

SESSIONE 17
Assessing landslide hazard: the slope instability hazard map of the
Castelnuovo di Garfagnana territory (Tuscany, Italy)
Key words: Landslide hazard, map, slope instability.
This paper is concerned with an experimental study aimed at
evaluating the landslide susceptibility using a multidisciplinary
approach. It is included in a wider research project, promoted by
the Tuscany Region Administration and APAT-Italian Geological
Survey. This project is aimed at defining the landslide hazard in
the area of the Sheet 250 «Castelnuovo di Garfagnana» (1:50,000
scale) of the new Geological Map of Italy (Fig. 1) (see the ISPRA
- Italian Geological Survey web site for detail).
The peculiar geological and geomorphological settings of the
study area, the severe climatic conditions favour hydro-geological
instability. This area, due to its geographical position and
conformation, is one of the rainiest in Italy: the annual average
rainfall is a typical value in the internal Apennines zones (about
1500-2000 mm). Geological and geo-engineering characteristics
of rocks and soils cause widespread landslide-prone areas, lifethreatening
and exposing to severe danger of towns, resorts,
factories and roads.
The landslide susceptibility evaluation adopted in this study is
referred to spatially defined landslide susceptibility areas, and no
estimate is given as regards the time of occurrence. Moreover, the
methodology applied in ranking slope instability concerned the
most representative landslide types that are slides and complex
slide-flow movements.
Conditional analysis was the first step of the methodology,
applied for evaluating the terrain zonation into different landslide
susceptibility categories. This is a conceptually easy statistical
method aimed at the qualitative evaluation of the importance of
the instability factors. In the second step advanced statistical
method (Logistic Regression) was applied in order to
quantitatively evaluate the effectiveness of the predisposing
factors and to provide the susceptibility ranking of the mapping
units.
The multidisciplinary approach provides geological,
_________________________
PAOLO ROBERTO FEDERICI (*), ALBERTO PUCCINELLI (*), GIACOMO D’AMATO AVANZI (*),
FRANCESCO FALASCHI (*), ROBERTO GIANNECCHINI (*), DARIA MARCHETTI (*), ALBERTO POCHINI (*),
FRANCO RAPETTI (*) & ADRIANO RIBOLINI (*)
(*) Dipartimento di Scienze della Terra, Pisa, damato@dst.unipi.it
590
geomorphological and geo-engineering characterization, together
with GIS-supported spatial analysis and statistical data analysis
The results showed a quantitative response, more reliable about
the effectiveness of each instability factors, with the possibility of
verifying their statistical significance.
The final product (Fig. 2) consists of a landslide susceptibility
map at 1:50,000 scale, put in a frame with some small scale maps
showing the areal distribution of the most significant factors, and
the related illustrative notes.
Fig. 1 - Location of the study area.

Fig. 2 - Overall view of the slope instability hazard map of the Castelnuovo di Garfagnana territory.
591
SESSIONE 17

SESSIONE 17
Historical data and flood/landslide hazard: main results in the
Versilia River basin (Tuscany, Italy)
Key words: Flood, hazard, historical data, Italy, landslide,
Versilia.
INTRODUCTION
The Versilia, in north-western Tuscany, is one of the most
known tourist regions in Italy, situated between the Ligurian Sea
to the West and the Apuan Alps to the East. The last are a
mountain chain which reaches almost 2,000 m in elevation and is
located a few kilometres from the coastline. This particular
geographic position favours in Versilia frequent and intense
rainfalls, which sometimes cause severe damage and destruction.
The Versilia River basin drains the southern portion of the Apuan
Alps (Fig. 1).
The importance of the historical research in the flood and
Fig. 1 - Location map of the Versilia River basin.
_________________________
(*) Dipartimento di Scienze della Terra, Università di Pisa,
rgiannecchini@dst.unipi.it, damato@dst.unipi.it
ROBERTO GIANNECCHINI (*) & GIACOMO D’AMATO AVANZI (*)
592
landslide hazard determination is recognized by several authors
(e.g. GUZZETTI et alii, 1994; GUZZETTI, 2000; AMANTI et alii,
2001; GLADE, 2001; CARRARA et alii, 2003).
In this short paper, the most significant results of a historical
archive investigation on floods and landslides in the Versilia
River basin are synthesized. The main purpose is to contribute to
the assessment of the hydrogeological hazard in the Apuan-
Versilian area as well as to collect useful data to realize a
catalogue of disastrous events.
The research allowed collecting much information about
landslides (in particular shallow landslides, typical phenomena
triggered by heavy rainstorms in this area) and floods, sometimes
consisting in a mere description of the damage, in particular for
the most remote events. Recently, the availability of objective
data (rain amount, hydrometric level of rivers and torrents, etc.)
allowed quantifying the event intensity by mean of physical
parameters.
RESULTS
The results confirmed hazard and vulnerability of the studied
territory, which was emphasized by the tragic June 19, 1996
hydrogeological catastrophe (14 deaths and about 500 millions of
Euro, D’AMATO AVANZI et alii, 2004). Recently, significant
damaging events occurred also in December 2009. Other high
severity events were identified in 1636, 1774, 1846, 1885 and
1902, together with a lot of less intense events, causing however
sensible geomorphologic effects and damage.
Altogether from 1328 to 2009, 186 sensible events were
found (the average frequency resulted of 1 sensible event every
3.7 years).
The spatial and temporal distribution of the meteorological
events showed a tendency to recur in the same areas and a
pronounced rise in frequency during the last centuries. This likely
depends on many concurring factors, among which there are:
increased number and reliability of the information sources;
increased attention to the damaging phenomena; spreading of the
elements at risk in hazardous areas; possible climate changes.
Referring to the study area, the historical research allowed
individuating the most hazardous period of the year, in which the
flood/landslide event probability raises: the three-month period
between September and November appears to be particularly at
risk (Fig. 2).

60
50
40
% 30
20
10
0
Dec, Jan,
Feb
Mar, Apr,
May
Jun, Jul,
Aug
Sep, Oct,
Nov
Fig. 2 - Distribution of the flood/landslide event occurred in the Versilia
River basin related to the four seasons of the year. The autumnal season
is the most hazardous one.
Furthermore, the collected data allowed obtaining a
preliminary, but significant classification of the identified events.
The classification was based on the event severity, deduced or
estimated by the collected information on intensity and damage,
partially following the suggestions of the French DRM -
DÉLÉGATION AUX RISQUES MAJEURS (1990). Four intensity
classes were individuated, in which the E4 class is comparable
with the 1996 event, which can be regarded as a reference event:
E1: low intensity
E2: medium intensity
E3: high intensity
E4: very high intensity
The results (Fig. 3) showed that an event characterized by
intensity comparable with that of the June 19, 1996 event could
have a recurrence time of about 100 years. In Fig. 4 is
represented an image showing damage produced by a disastrous
event, probably comparable with the 1996 one. On the contrary,
other hydrologic/pluviometric studies estimated the recurrence
time of such an event at a few hundreds of years. We can infer
that in the approach in evaluating the hazard of a territory the
100
80
60
40
20
0
Class of Intensity
no. events
E1 E2 E3 E4
Fig. 3 - No. of events in the four classes of intensity individuated: E1:
low intensity; E2: medium intensity; E3: high intensity; E4: very high
intensity.
%
593
B
Fig. 4 - Damages caused by the catastrophic event occurred on
September 25-26, 1885 (L’ILLUSTRAZIONE ITALIANA, 1885).
historical approach provides useful and effective data.
REFERENCES
AMANTI M., BERTOLINI G. & RAMASCO M. (2001) - The Italian
landslides inventory-IFFI Project. In Jorge E. et alii (eds)
Proc. III Panamerican Symposium on Landslides, Cartagena,
Colombia, 29 July-3 August 2001, Societad Colombiana de
Geotecnica, Bogotà, 2, 841-846.
CARRARA A., CROSTA G. & FRATTINI P. (2003) -
Geomorphological and historical data in assessing landslide
hazard. Earth Surf. Process. Landforms, 28, 1125-1142.
D’AMATO AVANZI G., GIANNECCHINI R. & PUCCINELLI A. (2004)
- The influence of the geological and geomorphological
settings on the shallow landslides. A typical example in a
temperate climate environment: the June 19 th , 1996
catastrophe in the north-western Tuscany (Italy). Eng. Geol.,
73 (3-4), 215-228.
DRM - DELEGATION AUX RISQUES MAJEURS (1990) - Les ptudes
SUpliminaires j la cartographie Upglementaire des risques
naturales majeurs. La Documentation Francaise, 143.
GLADE T. (2001) - Landslide hazard assessment and historical
landslide data - an inseparable couple? In: “The use of
historical data in natural hazard assessments”, Glade T.,
Albini P., Francés F. (eds). Kluwer: Dordrecht.
GUZZETTI F. (2000) - Landslide fatalities and the evaluation of
landslide risk in Italy. Eng. Geol., 58, 89-107.
GUZZETTI F., CARDINALI M. & REICHENBACH P. (1994) - The AVI
project: a bibliographical and archive inventory of landslides
and floods in Italy. Environ. Manag., 18, 623-633.
L’ILLUSTRAZIONE ITALIANA, Anno XII, n. 46, 15 novembre 1885.
SESSIONE 17

SESSIONE 17
Critical rainfall thresholds for triggering rapid shallow landslides in
the Eastern Ligurian Riviera (Italy)
Key words: Critical rainfall threshold, Eastern Ligurian Riviera,
Italy, landslide hazard, shallow landlslide.
INTRODUCTION
The Eastern Ligurian Riviera (Fig. 1) represents an area
characterized by high environmental value, mainly attributable to
its geographical position, morphological conformation and
climate. Such area, which includes the famous Cinque Terre, is in
Fig. 1 – Location map of Eastern Ligurian Riviera and Cinque Terre.
fact characterized by hills and mountains that overlooks the
Ligurian Sea, reaching altitudes of about 700-800 m a.s.l. These
features originate a very particular landscape, with ancient
terracing destined to agricultural activity (the vineyard of Cinque
Terre are particularly vintage and renowned worldwide),
disposed on steep slopes, almost vertically on the sea,
occasionally interrupted by some little inlets. These geographical
features significantly influence the local micro-climate,
characterized by relatively abundant annual rainfall amount,
where sometimes heavy rainstorms occur.
In several cases, such pluviometric events triggered many
shallow landslides (Fig. 2), causing damage and troubles to the
_________________________
ROBERTO GIANNECCHINI (*), DINO DAMILANO (*) & ALBERTO PUCCINELLI (*)
(*) Dipartimento di Scienze della Terra, Università di Pisa,
pucci@dst.unipi.it, rgiannecchini@dst.unipi.it
594
local population (for example, during the September 10, 1981
downpour hundreds of shallow landslides triggered in the
Levanto area, in the western portion of the study zone).
Therefore, the individuation of critical rainfall threshold for
triggering landslides assumes a strategic value in order to
predispose efficient alert systems and to manage risk situations,
especially in regions with strong tourist attitude and problems
with the road network.
Aimed at providing a contribution to the landslide hazard
evaluation of the study area, a detailed analysis of the main
pluviometric events from 1967 to 2006 was carried out, then
comparing their characteristics (in terms of rainfall amount,
intensity, duration) with landslides occurrence, obtained by
historical news, technical reports, publications, etc. The main
rainstorms that caused damage and landslides occurred in 1968,
1970, 1977, 1981, 1984, 1992, 1996, 1998 and 2000.
Fig. 2 – A shallow landslide in the Cinque Terre area (courtesy EptaConsult,
La Spezia).
RESULTS
The pluviometric data were obtained by three raingauges in
the area (Levanto, Vernazza, Portovenere, see Fig. 1). In order to
obtain the critical rainfall thresholds curve, the methodology
firstly proposed by CAINE (1980) (also applied by GOVI &

I (mm/h)
100
10
lower instability
field
Duration/Intensity
intermediate instability
field
SORZANA, 1980, JIBSON, 1989, GIANNECCHINI, 2006, etc.) was
used in this research. As regards the Levanto raingauge, the
research identified 290 significant rainfall events; on the basis of
the extent of effects caused, such events were subdivided into
four groups (Fig. 3): 1) events that induced many shallow
landslides and floods; 2) events that induced several shallow
landslides and floods; 3) events that locally induced some
shallow landslides and small floods; 4) no information about the
effects induced. These data allow us to individuate on the graph
three critical rainfall threshold curves which separate four
different stability fields with good approximation: stability, lower
instability, intermediate instability and upper stability.
Similar results were found also for Portovenere and Vernazza
stations.
Interesting results were also obtained by means of the
normalization of the pluviometric data using the mean annual
precipitation, while relations with the antecedent rainfall are at
present in progress, in order to comprehend indirectly the role of
the soil moisture in the landslding triggering mechanism.
Despite the limits that an empirical approach (black box
model) includes, it is often the only one able to obtain useful
results on a wide area, in absence of the several information (e.g.
geotechnical, hydrogeological, hydrologic) that a deterministic
approach needs.
stability field
595
REFERENCES
I = 131,65D -0,9417
I = 43,279 D -0,7254
I = 18,998D -0,672
1
no landslides
few landslides
several landslides
many landslides
0,1
0,1 1 10 100
D (h)
upper instability
field
Fig. 3 – Duration/Intensity relationship for 290 pluviometric events recorded at Levanto raingauge and compared with landslide occurrence. A lower threshold
curve (blue), an intermediate curve (green) and an upper one (red) are recognizable and separate four fields with different stability degree, decreasing from
bottom to top.
CAINE N. (1980) - The rainfall intensity-duration control of
shallow landslides and debris flows. Geografiska Annaler,
62A, 23-27.
GIANNECCHINI R. (2006) - Relationship between rainfall and
shallow landslides in the southern Apuan Alps (Italy). Nat.
Hazards Earth Syst. Sci., 6, 357-364.
GOVI M., SORZANA P.F. (1980) - Landslide susceptibility as
function of critical rainfall amount in Piedmont basin (North-
Western Italy). Stud. Geomorphol. Carpatho-Balcanica,
Krakow, 14, 43-60.
JIBSON R.W. (1989) - Debris flows in Southern Puerto Rico.
Geol. Soc. Am. Bull., 236, 29-55.
SESSIONE 17

SESSIONE 17
Sinkhole hazard in urban areas. A case study from Naples (Italy)
Key words: Anthropogenic sink, cavity, Naples, sinkhole.
PRELIMINARY REMARKS
Activities aimed to integrate the national database of
sinkholes, available online, have been carried out from
Geological Survey of Italy (ISPRA).
Particularly, new data related to anthropogenic sinkholes
interesting urban areas have been considered.
As it is well-known, anthropogenic sinkholes assume a
particular rule, cause their genetic and evolutive differences and
peculiarities. In addition, the cultural and settlement context
interested by sinkholes is frequently reason of high economic or
human loss.
Contemporaneously, besides acquiring new data and
enriching the database, case-history studies, as Neapolitan urban
area, have been carried out.
INTRODUCTION
Naples city’s territory is one of the urbanized areas mostly
interested by anthropogenic sinkholes in the world (Fig. 1).
The reasons are the geological and structural settings, but also
the peculiarities of its historical-urbanistic development.
Notwithstanding, specific studies related to sinking
phenomena in Neapolitan area do not exist in literature.
Certainly, it is necessary to highlight the importance of some
works, as CATENACCI (1992) or the Proceedings of Naples
underground study Committee (AA.VV., 1967). However, the
only one anthropogenic sinkhole’s census today existing has been
realized from Italian Civil Protection Department, and it is related
to a forty years period, from the ending of ‘60s at the beginning
of 2000. In this period about 140 sinkholes in Naples (CORAZZA,
2004) were censed. Another census has been carried out from
C.U.G.Ri. (2000); but all these works are quite incomplete, and
lacking in informations concerning collapses reported by
historical news, from the beginnings of XX century at least.
_________________________
(*) ISPRA – Istituto Superiore per la Protezione e la Ricerca Ambientale –
Servizio Geologico d’Italia; paolomaria.guarino@isprambiente.it,
stefania.nisio@isprambiente.it
PAOLO M. GUARINO (*) & STEFANIA NISIO (*)
596
ANTHROPOGENIC SINKHOLES
The whole of sinkholes, damages to building and historicalartistic
patrimony and loss of human lives attributes to Neapolitan
urban area the maximum risk level. It is enough to say, for
example, that the collapses which happened on 23 rd September
2009, interested the S. Carlo alle Mortelle church, which
accommodates seventeenth century’s paintings, and provoked
the evacuation of more than forty families.
About the causes of collapses, their triggering is due to
primer-factors constituted by heavy precipitations and new or
thoughtless anthropic works.
But, above all, some factors act a proneness rule: they
include anthropogenic and natural factors.
Among anthropogenic factors, the main rule is carried out by
a widespread artificial cavities net and by a very old and
inadequate sewer system. Geotechnical terrains properties and
historical territory’s transformations are the principal natural
proneness factors.
The excavation of artificial cavities in Naples dates back to
remote ages. The oldest ones include some graves dating to
Enaeolithic period, excavated in the tuff bedrock.
Underground cavities dating to Hellenistic period are more
numerous; they were used only for funeral hypogeum.
Fig. 1 – Naples: view of sinking produced by the cavity’s roof collapse.

During Roman age, to these use-destinations of cavities, the
harvest and adduction of water by means the excavation of
cisterns or aqueducts (e.g. the acquedotto Claudio) and the
connections by means of artificial galleries (e.g. the cripta
neapolitana) came on top.
The XV century marked the beginning of a period of intense
urban development which caused a dizzy demand for building
materials, and a consequent opening of underground caves, which
persisted during the following centuries.
In the last fifty years, some cavities were used as antiaircraft
shelter and, subsequently, were turned into dumps.
It’s not rare to observe the sequence of different usedestinations
in the same cavity: at the beginning turned into
funeral hypogeum, subsequently transformed in a quarry, and,
finally, in a dump.
About the system of sewer, the rapid urbanization increase
and the effects of a devastating cholera epidemic in 1884
resulted in adopting a free surface system of sewer, at the ending
of nineteenth century.
This typology of sewer was not suitable for the rapid
urbanistic increase, and consequent conditions of pressurized
flow happened very frequently, giving underground erosion and
caves formation.
Finally, it’s important to quote the rule carried out from low
erosion strength of pozzolanic terrains and alluvial deposits
deposed by streams flowing around the old city, and the presence
of terrains susceptible to liquefaction in the eastern urban sector.
WORK IN PROGRESS
First of all, the work in progress has been finalized to an
update of the knowledge of sinking phenomena in Neapolitan
urban area.
Identification, recognition and mapping of collapses have
been carried out. Anthropogenic sinkhole data have been stored
in a Geographical Information System (GIS) and database
associate, containing the principal data related to the event: date
and major morphological characteristics (diameter, depth and
square).
During the second phase, the study of controlling factors has
been carried out, by means of a multi-layered geologic database,
the insertion of cavities and borehole logs and other features data.
The information processing allowed to realize a Sinkhole
Inventory Map and to set a multi-theme approach to the
comprehension of the collapse controlling factors, aimed to
mapping hazard conditions.
597
REFERENCES
AA.VV. (1967) - Il sottosuolo di Napoli. A.G.I. Atti VIII
Convegno Nazionale di Geotecnica.
CATENACCI V. (1992) – Il dissesto geologico e geoambientale in
Italia dal dopoguerra al 1990. Mem. Descr. Carta Geol. d’It.,
XLVII.
CORAZZA A. (2004) – Il rischio di fenomeni di sprofondamento
in Italia: le attività del Dipartimento della Protezione Civile.
Atti 1° Seminario “Stato dell’arte sullo studio dei fenomeni di
sinkholes e ruolo delle amministrazioni statali e locali nel
governo del territorio”, Roma, 20-21 Maggio 2004, 319-330.
C.U.G.RI. (2000) – Il sistema fognario della Città di Napoli alle
soglie del 2000. Arti Grafiche Solimene. Casoria (NA).
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SESSIONE 17
Debris-flow susceptibility assessment in the “Costa Viola” mountain
ridge (southern Calabria): the Favazzina study area
GIULIO G.R. IOVINE (*), ANNAMARIA D. PELLEGRINO (**) & ORESTE G. TERRANOVA (°)
Key words: Calabria, debris flow, modelling, susceptibility.
The “Costa Viola” mountain ridge, facing the Tyrrhenian Sea
between the villages of Palmi and Villa San Giovanni (southern
Calabria), is sadly renowned for being exposed to severe seismic
and geo-hydrological risk conditions, in addition to tsunamis
along the coast. The coastal sector between Bagnara Calabra and
Scilla – where the village of Favazzina, here considered, is
located – is crossed by the railway, the highway “Salerno-Reggio
di Calabria” (A3), the southern Tyrrhenian trunk road (SS.18).
In the study area, the main factors conditioning slope morphoevolution
are represented by tectonics (both as structural setting
and seismicity), lithological and climatic characteristics, and
human activities (e.g. widespread cuts and disordered drainage
network).
The Palaeozoic metamorphic and crystalline bedrock that
constitutes the skeleton of the mountain ridge (AMODIO MORELLI
et alii, 1976) is strongly tectonized, and deeply weathered. At the
base of the mountain ridge, a NE-SW trending fault marks the
transition between the metamorphic/crystalline basement and the
sedimentary terrains of the coastal plan: this morpho-structural
element belongs to the Calabrian-Sicilian Rift Zone, a normal
fault belt developed along the eastern coast of Sicily and the
western side of the Calabrian Arc since Middle Pleistocene
(MONACO &TORTORICI, 2000). From a morphological point of
view, the area is characterized by steep and uneven slopes, cut by
deep canyons; a set of marine terraces can be recognized at 100-
200 m, 350 m and ca. 590 m a.s.l. Along the coast, small highgradient
torrents flows into the Tyrrhenian Sea, draining the
western slope of the Costa Viola mountain ridge. Cold winter air
fronts commonly approach Calabria from NW, originating
intense storms. The narrow and discontinuous strip of land
between the coastline and the base of the ridge is densely
urbanized, and reaches a maximum extent of ca. 300 m at
Favazzina.
_________________________
(*) CNR-IRPI, iovine@irpi.cnr.it
(**) Autorità di Bacino Regionale, Regione Calabria,
an.pellegrino@regcal.it
(°) CNR-IRPI, terranova@irpi.cnr.it
598
Fig. 1 – On top, panoramic view of the uppermost portion of the slope
affected by a debris flow activation on 31 March 2005. On bottom, distal
portion of the same debris flow, that damaged the SS.18, the railway and
the urbanized area of Favazzina.
This sector has repeatedly been affected by slope instability
events in the past, mainly related to debris slides, rock falls and
debris flows. Among the most recent events, those occurred in
2001 and in 2005 severely hit the main infrastructures and sectors
of the urbanized areas (ABR-CALABRIA, 2001; 2005; 2006;
BONAVINA et alii, 2005). On May 12, 2001, a debris flow
developed along the Torrent Favagreca, just south of the village
of Favazzina, damaging the station of the SNAM methane
pipeline, the railway and the SS.18, causing the derailment of the
ICN Torino-Reggio di Calabria; a second debris flow developed
along a nearby canyon, located northward of the Favagreca, and
hit the highway A3 near the Brancato tunnel. On 31 March 2005,
a similar event damaged great part of the village of Favazzina, the
SS.18, and caused the derailment of the ICN Reggio di Calabria-

Milano. During the winter seasons 2008/2009 (VERSACE, 2009)
and 2009/2010, the “Costa Viola” mountain ridge suffered again
from notable damage due to occurrence of different types of
slope movements.
An attempt of debris-flow susceptibility mapping has been
performed for the surroundings of Favazzina. The adopted
approach is based on a physical process model (FLO-2D;
O’BRIEN et alii, 1993), inspired from the finite difference
Diffusive Hydrodynamic Model (DHM) by HROMADKA &YEN
(1987). Flood routing in 2D is accomplished through a numerical
integration of the equations of motion, and the conservation of
fluid volume. The model is able to route rainfall-runoff and flood
hydrographs over unconfined flow surfaces or in channels. In the
model, a dynamic wave approximation to the momentum
equation is adopted, allowing to simulating street flow, buildings
and obstructions, sediment transport, spatially variable rainfall
and infiltration, and floodways. The flow progression over the
computational domain (discretized into uniform, square grid
elements) is controlled by topography and resistance to flow. The
model routes mudflows as a fluid continuum, by predicting
viscous fluid motion as a function of sediment concentration.
Model calibration has been performed by considering
available information concerning the debris flows triggered
during the cited 2001 event. On the other hand, information
related to the 2005 cases (not considered for calibration) has
successively been used to validate the model results.
Once validated, the model has been applied to the sector of
interest, aiming at predicting the zones exposed to the effects of
future debris-flow events, by assuming distinct scenarios related
to hydrographs computed for return periods of 25-200 years. The
selection of the potential sources has been performed through an
Expert Evaluation Approach (LEROI, 1996), by taking into
consideration available literature and technical reports on
landslide risk in the study area (PAI, 2001; PELLEGRINO &
BORRELLI, 2007; cf. also cited reports by ABR-CALABRIA), and
the results of aerial-photo interpretation and geomorphological
surveys (unpublished).
In this paper, after briefly describing the modelling approach,
the results of calibration and validation against the 2001 and
2005 cases are discussed. Then, the selection of the presumable
source areas is commented, in the light of available
geomorphological and historic data. Finally, the results obtained
in terms of debris-flow susceptibility mapping are presented.
REFERENCES
ABR-CALABRIA (2001) - Studio sullo stato del dissesto
geomorfologico ed idrogeologico dell’area compresa tra i
comuni di Scilla e Bagnara (RC). Autorità di Bacino
Regionale, Regione Calabria, Report 11.06.2001.
599
ABR-CALABRIA (2005) - Relazione sui fenomeni franosi che
hanno interessato il versante tra Bagnara Calabra e Scilla
(Favazzina, RC) – Marzo 2005. Autorità di Bacino Regionale,
Regione Calabria, Report aprile 2005.
ABR-CALABRIA (2006) - Mitigazione del rischio idrogeologico
nel tratto di versante compreso tra Bagnara Calabra e Scilla
(RC). Quadro conoscitivo e strategia di intervento. Autorità
di Bacino Regionale, Regione Calabria e Settore 32 del
Dipartimento Lavori Pubblici della Regione Calabria, Report
maggio 2006.
AMODIO MORELLI L., BONARDI G., COLONNA V., DIETRICH D.,
GIUNTA G., IPPOLITO F., LIGUORI V., LORENZONI S. et alii
(1976) - L'arco Calabro-peloritano nell'orogene
appenninico-magrebide. Mem. Soc. Geol. It., 17, 1-60.
BONAVINA M., BOZZANO F., MARTINO S., PELLEGRINO A.,
PRESTININZI A. & SCANDURRA R. (2005) - Le colate di fango
e detrito lungo il versante costiero tra Scilla e Bagnara
Calabra (Reggio Calabria): valutazioni preliminari di
suscettività. Giorn. Geol. Appl., 2, 65–74.
HROMADKA T.V. & YEN C.C. (1987) - Diffusive hydrodynamic
model. U.S. Geological Survey, Water Resources
Investigations Report 87-4137, Denver Federal Center,
Colorado.
LEROI E. (1996) – Landslide hazard – Risk maps at different
scales: objectives, tools, and developments. In: Proc. VII Int.
Symp. on Landslides, Trondheim, 1, 35-52.
MONACO C. & TORTORICI L. (2000) - Active faulting in the
Calabrian arc and eastern Sicily. Journal of Geodynamics,
29, 407-424.
O´BRIEN J.S., JULIEN P.Y. & FULLERTON W.T. (1993) - Two
Dimensional Mudflow Simulation. J. Hydr. Eng. ASCE,
119(2), 244-261.
PAI-CALABRIA (2001). Piano Stralcio di Bacino per l’Assetto
Idrogeologico (PAI). Autorità di Bacino Regionale, Regione
Calabria, cf. http://www.adbcalabria.it/.
PELLEGRINO A. & BORRELLI S. (2007) – Analisi del dissesto da
frana in Calabria. In: Rapporto sulle frane in Italia. Il
Progetto IFFI – Metodologia, risultati e rapporti regionali.
Rapporti APAT, 78, 599-632. (Maps available at
http://www.mais.sinanet.apat.it/cartanetiffi/).
VERSACE P. (2009) - Relazione di sintesi e schede di sopralluogo.
Prefettura di Cosenza - Ufficio Territoriale del Governo -
Gruppo di valutazione per l’emergenza idrogeologica.
Conference CD, ORG-Calabria.
SESSIONE 17

SESSIONE 17
Key words: Desertification risk, environmental indices,
Mediterranean environment, socio-economic indices.
This work uses as a reference the ESAs model
(Environmental Sensitive Areas to Desertification; KOSMAS et
alii, 1999) which is modified through a set of new indicators
which take into account the specific environmental and socioeconomic
characteristics of Apulia region (Southern Italy)
representing a typical semi-arid Mediterranean coastal area.
A new set of identifiable parameters relevant for planning and
control measures is proposed focusing on the main environmental
problems (land degradation and desertification) and socioeconomic
driving forces. These supplementary indicators are
integrated in the ESAs model and, by using a GIS, and applied
for the risk assessment to desertification of Apulia region.
The analyses include the elaboration of the whole set of
indices on both the regional and the administrative scales which
constitute the principal territorial units for the management of
natural resources. The results have demonstrated that the
introduction of new dynamic quantitative indices, with a notable
degree of details, has improved substantially the overall
evaluation of the desertification risk in the region.
The proposed approach permits the identification and
refinement of different degrees of sensibility of an area to land
degradation as well as the analyses of the factors affecting
desertification and their evaluation in terms of spatial and
temporal distribution. Moreover, this new method is conceptually
very simple and easily adaptable for dynamic scenarios analysis
which are important in climate change studies.
Due to its applicability at different scales (from local to
regional and national), the presented methodology can be
proposed for the definition of priorities in adoption of strategies
to mitigate desertification in the semi-arid Mediterranean
environments.
_________________________
The evaluation of a new ESAs approach for the assessment of
desertification risk in Apulia region (southern Italy)
GAETANO LADISA (*), MLADEN TODOROVIC (*) & GIULIANA TRISORIO LIUZZI (**)
(*) Istituto Agronomico Mediterraneo, CIHEAM-IAMB, Bari,
ladisa@iamb.it
(**) Dipartimento di Progettazione e Gestione dei Sistemi agro-zootecnici e
forestali, Università “A. Moro”, Bari
600
REFERENCES
KOSMAS, C., FERRARA,A.,BRIASSOULI,H.&IMESON, I. (1999) -
Methodology for mapping ESAs to desertification. In: C.
Kosmas, M. Kirkby and N. Geeson (Eds.) – The MEDALUS
Project. Mediterranean Desertification and Land Use. Manual
on key indicators of desertification and mapping
Environmentally Sensitive Areas to desertification. EUR
18882, 31-47.

Characters of fluvial risk in Po alluvial plain
FRANCA MARAGA (*), VIRGILIO ANSELMO (**), GIANFRANCA BELLARDONE (°), FURIO DUTTO (°°),
FEDERICA FILIPPI (§) & LUISA PELLEGRINI (§§)
Key words: Channel change, bed scour, river bank movement,
Italy, Po Plain, Po River system, soil loss.
INTRODUCTION
Fluvial risk factors are described as related to the river
channel mobility and supported by the observations on the flood
events able to mobilize and transfer sediments along the water
course.
Human activities and engineering works as well as rivers in
lands and properties are often damaged by river channel and
water flooding dynamics.
Damages are observed as land loss on the plain and as
collapse of river training works and road connections.
Fig. 1 – Bridge collapse of the motorway Turin-Aosta by pier scouring along
the Orco river, Po plain in Turin province, 2000 flood (courtesy of Susella
G., ARPA Piemonte).
_________________________
(*) National Research Council, Dep. Earth and Environment, Research
Institute for geo-hydrological Protection, franca.maraga@irpi.cnr.it
(**) Consulting Engineers “Anselmo Associati”, info@anselmoassociati.it
(°) ARPA Piedmont, gianfranca.bellardone@regione.piemonte.it
(°°) Province of Turin, furio.dutto@provincia.torino.it
(§) River Po Basin Authority , federica.filippi@adbpo.it
(§§) Pavia University Dep.of Earth Sciences, luisa.pellegrini@unipv.it
CNR-IRPI - in the framework of the project on the natural risks
601
Study cases on flooding effects illustrate the flooding
vulnerability along a reach of 200 km of the River Po from Turin
to Cremona.
The observed fluvial system is representative of an erosion
system one, with erosional processes in progress.
The flood morphogenetic dynamics result in shortening the
watercourses (meander cut-off, river straightening, channel
canalisation) and in a faster peak flow propagation (GOVI &
TURITTO, 1993; MARAGA et alii, 2000, 2003).
The flooding effects generated risk conditions especially due
to the water flow erosion of riverbanks and bed as well as
sediment transport. These effects induced and are still inducing
damages to bridges and riverbanks.
BRIDGE VULNERABILITY
As concerning the bridge vulnerability, pier scouring is
frequently observed (Fig. 1) in composite sedimentary settlement
of the channel, having gravel beds related to the fluvial risk at the
event scale (SUSELLA, 2003; TROPEANO et alii, 2006).
A fine sediment substratum of deltaic silty and sandy deposits
is often observed below the gravel.
In some rivers of the upper Po plain, waters are locally
flowing on the channel bed incised into the pre-fluvial
sedimentary body, generating changes in the roughness of the
channel bed, originally buried by the fluvial gravel sediments.
No sediment supply is able to restore and maintain the thin
sheet of previous fluvial gravel deposits overlaying the
substratum in fine sediments.
In a case of extreme evolution of river bed in the Turin
alluvial plain (Stura di Lanzo river, Alpine tributary of the Po
river in Turin) the channel incision on the fluvial plain has locally
cut some meters into the fine sediments of the substratum, a
process that started in the 1980s (PELLEGRINI et alii, 2008).
A reference reach 500 m long and 150 m wide was surveyed
in 2004 (610 points), in order to evaluate the progress of channel
downcutting in the fine sedimentary body, evaluated in 6 m
according to the abandoned 1950s channel bed remains.
The bridge located downstream the reference reach was
destroyed twice, the last time in 2000 flood event.
Several bridges as well as important water diversions of the
considered fluvial system were destroyed as effect of the 1994
event. The River Po flood plain from Turin downstream to the
SESSIONE 17

SESSIONE 17
confluence of Tanaro shows an interesting example of the
changes induced by a river to the geometric and environmental
characters of the flood prone areas. Permanent changes on the
plain against soil and roads as a consequence of the November
1994 big flood were due to the side erosion of the main channel
and to gully erosion on the flooded plain (MARAGA, 1998). Major
damages were observed along the abandoned channels of ancient
river beds. Levees were overtopped, bridges and roads were
swept away, bank recession was evaluated of the order of 200 m.
Bank recession processes were observed also during the October
2000 major flood. Geomorphic changes are extended to the
whole extent of the flood prone area (CAPPELLIN et alii, 1998;
MARAGA &TURITTO, 1998).
LAND VULNERABILITY
As concerning the land vulnerability on the riverine lands, the
erosion processes and land losses are referred.
Erosive and sedimentary processes in the fluvial dynamic
characterise the lateral river bank erosion and sediment supply.
An assessment of land loss related to the long term fluvial risk
were checked along a River Po reach from Tanaro (Pavia) to
Adda (Cremona), the first tributary flowing from the Apennines
and the second one flowing from the Alps.
The reach about 200 km long and 200 m wide was selected as
representative of the bank adjustments.
Comparative analyses were carried out by series of aerial
photographs and channel section surveys and maps to obtain
evaluation of the land losses because of bank erosion from 1955
to 1988.
The period showed the most important channel changes since
the great population increase (1950s) and before the large river
management works (1990s).
The results are derived from 54 bank erosion sites located
both on the left bank (29 sites) and on the right one (25 sites),
involving a total area of about 8.5 million m 2 of land loss; the
volumes are obtained from the mapped area and the
corresponding mean depth of the eroded bank.
The cumulate volume of land loss because of bank recession
is more than 60 million m 3 (DUTTO &MARAGA, 1991). The
greatest intensity in observed in case of channel instability and in
composite bank slopes (gravel at the bank toe and sand at the
top). Po river bank erosion are updated to the last flood events in
selected sites to show minor variations after 1988, as a joint
effect of the river bank protection works and of the channel
deepening processes.
Acknowledgements
M. Baldo, F. Godone, G. Rivelli, topographic survey; R.
Massobrio sediment grain size analysis; C. Pelissero, G. Rivelli,
morphometric data elaboration; P. G. Trebò, image processing
602
(Cnr-IRPI, branch of Turin).
To Mario Govi, IRPI Turin former director († 2009).
REFERENCES
CAPPELLIN R., GODONE F. & MARAGA F. (1998) –
Perimetrazione georeferenziata dei campi di attività
morfogenetica in area inondabile. Rilievi connessi alla
secolare inondazione 1994 del Fiume Po tra Dora Baltea e
Sesia. CNR-IRPI, Torino, Rapporto interno R.I. 98/13.
DUTTO F. & MARAGA F. (1991) - Valutazione dei sedimenti
mobilizzati nel periodo 1955-1988 lungo le sponde del Fiume
Po. CNR-IRPI, Torino, Rapporto interno, M.I. 91/01.
GOVI M. & TURITTO O. (1993) - Processi di dinamica fluviale
lungo l’asta del Po. Acqua-Aria, 575-588.
MARAGA F. (1998) - Pericolosità naturale dei territori fluviali.
In: IX Congresso Nazionale dei Geologi, Roma, 17-20 Aprile
1997, 261-269.
MARAGA F., BELLINO L. & MASINO A. (2000) - Interventi storici
di sistemazione fluviale per la tutela del patrimonio urbano in
Pianura Padana (Italia Settentrionale). Atti Convegno
GeoBen 2000, Condizionamenti Geologici e geotecnica nella
Conservazione del patrimonio Storico Culturale, Torino 7-9
giugno 2000, 613-622.
MARAGA F., MASINO A. & VIOLA E. (2003) - Evoluzioni
idrografiche del Fiume Po nel tempo ultrasecolare. Atti della
7° Conferenza nazionale ASITA, Verona 28-31 ottobre 2003,
1415 - 1420.
MARAGA F. & TURITTO O. (1998) - Diagnosi geomorfologica
d'inondabilità in casi di studio sull'idrografia padana. Atti
del Convegno Internazionale “Alba 96: La previsione delle
catastrofi idrogeologiche, il contributo della ricerca
scientifica”, Alba (CN) 5-7 novembre 1996, (2), 313-334.
PELLEGRINI L., MARAGA F., TURITTO O. AUDISIO C. & DUCI G.
(2008) – Evoluzione morfologica di alvei fluviali mobili nel
settore occidentale del bacino padano. Il Quaternario,
21(1B), 251-266.
SUSELLA G. (ED.) (2003) – Evento alluvionale regionale del 13-
16 ottobre 2000. Arpa Piemonte, L’Artistica Savigliano, 415
pp.
TROPEANO D., LUINO F. & TURCONI L. (2006) – Eventi di piena e
frana in Italia settentrionale nel periodo 2002-2004. GNDCI,
Pubblicazione n. 2911, Società Meteorologica Subalpina,
Castello Borello, Bussoleno (TO).
TURITTO O., MARAGA F., LUINO F. (1995) - Impatto sulle
infrastrutture viarie prodotto da piene con inondazione. Geol.
Appl. Idrogeol., 30 (I), 75-88.

Key words: Floodplain evolution geomorphological analysis,
LiDAR, stream erosion.
The Serchio river basin (about 1600 km 2 wide), includes hilly
and mountainous areas, where historical towns lie together with
industries, factories and tourist facilities, linked by welldeveloped
infrastructures. The geological and geomorphological
settings of the basin, the severe climatic conditions favour hydrogeological
instability. Frequently heavy and\or relentless rainfall
caused the Serchio River and its tributary to overflow, lifethreatening
and exposing to severe danger towns, resorts,
factories and roads. Many landslides occur causing severe
damages, high hazard and risk.
This situation wholly justifies efforts to improve knowledge
of stream dynamics, inundation recurrence and floodplain
geomorphological evolution in high risk valley floor areas.
Since 2006, the Serchio River Basin Authority (Italian
Department of the Environment) has commissioned a LiDAR
(Light Detection and Ranging) survey into the valley floor of the
Serchio River and along some of its major tributaries, in order to
improve knowledge of stream dynamics, to analyse and monitor
the territory of jurisdiction.
The LiDAR aerial mapping constitutes an innovative and
effective instrument for advanced hydrologic and
geomorphological assessment. High precision Digital Surface
Model (DSM) completed with buildings and vegetation, a filtered
DSM obtained by removing vegetation, and a Digital Terrain
Model (DTM) derived from the DSM by post-processing,
allowed for hydrologic modelling and geomorphological
mapping, almost unfeasible by the regional technical map, nor on
aerial photos. Multi-temporal aerial photogrammetric analysis
was also performed in order to compare the digital model with
the photorealistic model and match them together.
The outcome of this study is a step forward into hydrologic
and geomorphological assessment of floodplain dynamics and
evolution., with particular regard to stream erosion activity,
flooded areas reconstruction and mapping. Also, the most evident
_________________________
Riverbed and floodplain evolution in the Serchio River basin
RAFFAELLO NARDI (*), FRANCESCO FALASCHI (*), STEFANO SADUN (*), NICOLA COSCINI (*),
NICOLA DEL SEPPIA (*), MANUELA COLMAN (*), ANDREA DI GRAZIA (*), FRANCESCA QUILICI (*),
GIACOMO D’AMATO AVANZI (**), ROBERTO GIANNECCHINI (**) & ALBERTO PUCCINELLI (**)
(*) Autorità di Bacino del Fiume Serchio, segreteria@bacinoserchio.it
(**) Dipartimento di Scienze della Terra, Università di Pisa,
damato@dst.unipi.it
603
transformation of the floodplain due to the human activities, such
as buildings enlargement, landfill, stores of wasted and\or
buildings materials, were identified and monitored.
Fig. 1 – LiDAR shaded relief sample image (Serchio River Basin Authority).
SESSIONE 17

SESSIONE 17
Sinkholes: new cases. Some examples from Umbria region (Italy)
Key words: Acquasparta, Bevagna, Orvieto sinkholes, Umbria.
INTRODUCTION
Many sub-circular ponds, lakes and dry cavities in Umbrian
territory, originated in historical age, should be due to piping
sinkhole phenomena.
This hypothesis is supported by the geological, morphological
and hydro-geological setting of the area interested by the
sinkholes.
The small lakes have diameters from few to hundreds of
meters and depth up to fifteen meters. The names are of
dialectical origin and usually they indicate a kind of sinking (e.g.
‘abyss’). Some legends refer to the origin of the lakes as a quick
catastrophic collapse. Usually, these depressions are originated
by karst erosion (collapsed dolines). Sometimes the genetic
process should be related to the presence of artesian, mineralized
waters and gas emissions (mainly CO2 and H2S) that contribute to
the formation of the sinkholes through a mechanical upward
erosion (deep piping process; NISIO, 2003).
These cavities are water filled (drown sinkholes) and are
located on thin grained impermeable or semi-permeable
sediments (silty clay, silt) more than 100 m thick.
The correlation between collapses and piping sinkholes is
confirmed by the “drowning” of the cavity soon after the
formations creating a ponds or a sub-circular lake, sometimes
with underwater springs that feed the small lake.
In some cases many information are available about the date
and the modalities of the cave genesis (Aiso lake, Alto lake,
Sugano lake, Vadimone lake etc.). The sinkhole ponds (more
than 50 phenomena) are concentrated in Umbrian alluvial plains
(Tiber, Topino, Tinia river plains). In this work some sinkhole
prone areas of Perugia and Terni districts are considered.
UMBRIAN SINKHOLE PRONE AREAS
Bevagna area (Perugia district) is located at the cross of some
_________________________
(*) ISPRA – Istituto Superiore per la Protezione e la Ricerca Ambientale –
Servizio Geologico d’Italia, stefania.nisio@isprambiente.it
STEFANIA NISIO (*)
604
rivers: Topino, Tinia, Teverone, in an alluvial plain rich of
numerous springs. Other little lakes and springs (now filled) are
represented in ancient maps.
One lake is also present, Aiso lake (Fig. 1); it is located near
Bevagna city; it shows 25 m of diameter and 13 m of depth; at the
bottom some springs are presents. Some geochemical analyses
are conducted.
Fig. 1 –Aiso lake view, Bevagna plain (Perugia district).
It was originated probably in historical age (pre-Roman age);
some legends describe its origin (from the 1300) as a quick
catastrophic collapse (TRABALZA, 1914; BARONTI, 1997). The
water of the Aiso lake runs in an other sub-circular pond (Aisillo
lake), sacrum place of cult in Roman age (ALBANESI &PICUTI,
2009), also originated from a catastrophic subsidence.
The analyses of all Bevagna territory have been showed other
small lakes and dry cavities (e.g. ‘Madonna delle Rose’ cavity).
These morphologies could be due to deep piping sinkhole
phenomena. This hypothesis is supported by geological, hydrogeological
and structural setting of the Bevagna plain area.
The Bevagna plain area is characterized by alluvial sediments
(clay and silt with more than one hundred of meters) at the top of
a main syncline, with N-S trend.
Some fault systems cross the Topino alluvial plain: the
cavities are locates with NS trend. In the Bevagna plain area are
present aquifers related to deep hydro-geological circuits
(confined aquifers).
In the Acquasparta plain area an other little lake is located,
Lago Alto or Casigliano lake (NISIO, 2008; Fig. 2).
It is originated by a collapse (as referred in a legend); it is
located in alluvial terraces at the top of marine clays (more than

50 meters of clay); the plain is bordered by carbonatic ridge
interested by strong karst phenomena. Furthermore, the
Acquasparta area is characterized by generous underground
mineralized waters, as testified by the numerous springs (S.
Faustino mineral springs), mostly sulphurous and rich of gas.
Fig.2 – Lago Alto view, Acquasparta area (Terni district).
Fig. 3 – Sugano lake view, Orvieto (Terni district).
Information about this lake are preserved in few ancient
documents in the Casigliano Castle. Geological,
geomorphological and hydro-geological studies have been
conducted and some preliminary hypotheses are presented to
explain the genesis of this lake.
The Sugano Lake (unknown in geological literature; Fig. 3)
was originated by a collapse in historical age (probably at the
beginnings of the 1900). Information about this lake are in some
legends; the lake is located in a plain area over pyroclastic cover
(up 100 meters of thickness).
The Vadimone lake (between Viterbo and Terni districts) is
unknown in geological literature but it is mentioned in historic
documents in Roman age; it is recognized in volcanic areas on
pyroclastic deposits. This phenomenon was supposed to be
volcanic craters (maar). In this study it is considered a
catastrophic collapse related to deep piping phenomena,
reactivated in different centuries.
The Vadimone sinkhole is represented by a cylindrical shaped
cavity with 75 meters diameter and 4 meters depth (17 m in the
past) on pyroclastic deposits.
605
After the discovery of the ancient lakes, others Umbrian plain
area have been investigated.
The analysis of the aerial photographs has allowed the
location of many sinkhole ponds and paleo-morphologies. From
the historical sources the presence of other numerous lakes, now
extinct and of difficult location have been verified: the studies are
in progress.
Examining the concerned area it is possible to conclude that
some of the Umbrian censed spring ponds and sub-circular
morphologies have been originated from the sinkhole sensu
stricto phenomenon (NISIO, 2003).
REFERENCES
ALBANESI M. & PICUTI M. R. (2009) - Un luogo di culto d’epoca
romana all’Aisillo di Bevagna (Perugia). Mélanges de
l’Ecole française de Rome. Antiquité, 121 (1), 133-179.
BARONTI G. (1997) - La leggenda dell’Áiso. L’opposizione
secco/umido come modello esplicativo del mondo in un
racconto di tradizione orale del territorio di Bevagna
(Perugia, Umbria) In ‘Il lago...uno spazio domestico. Studi in
memoria di Alessandro Alimenti’, Perugia, 1997. Quaderni
del Museo della Pesca del Lago Trasimeno, 3, 21-50.
NISIO S. (2003) – I fenomeni di sprofondamento: stato delle
conoscenze ed alcuni esempi in Italia Centrale. Il
Quaternario, 16 (1), 121-132.
NISIO S. (2008) - I fenomeni naturali di sinkhole nelle aree di
pianura italiane. Mem. Descr. Carta Geol. d’It., 85, 475 pp.
TRABALZA O. C. (1914) - Due leggende nel territorio di Bevagna
(Umbria). Lares: Bull. Soc. Etnogr. It., 3 (2-3), 151-161.
SESSIONE 17

SESSIONE 17
Impact and benefit profits of a combined approach
based on the use of multi -interferometric analysis (acquisition of
ERS – ENVISAT PS ) applied to a pre - existing landslide inventory
Key words: Impact and benefit profits, InSAR data, landslides.
Terrafirma is an initiative funded by ESA (European Space
Agency) and University of Florence (UNIFI) in the framework of
GMES (Global monitoring for Environment and Security)
looking for new techniques to better protect European citizens
against environment risks and to reduce their consequences. The
project aims at producing pan-European services based on the
latest technology to measure terrain motion from satellite InSAR
data relating to landslides (Fig. 1). In this context, an analysis
concerning the Reggio Calabria District and the southern portions
of the Vibo Valentia and Catanzaro Districts (Calabria, Italy), to
update a pre-existing landslide inventory, through a combined
approach based on the use of multi-interferometric analysis
(Acquisition of ERS – ENVISAT PS, 1992 - 2006) and photo
interpretation was carried out. The pre-existing landslide is
referred to acquisition of Landslide Inventory developed by the
Authority of River Basin of Calabria Region (ABR), in the world
of the researches aiming to the Hazard and Risk delimitations of
River Basin plans (PAI -L. 267/98) and the IFFI Project (Italian
Landslide Inventory). The ABR (Recipient) collected historical
documents, archive data and mapped the areas affected by
landslides; in addition, ABR carried out and tested projects
related to its planning and programming responsibility.
ESA, UNIFI and ABR entered in a contractual agreement
(Service Level Agreement) for the assembly of a Terrafirma
Landslide Inventory Product (LSI). The Contract forecasts a
feedback action by means of ABR, to perform through a more
detailed analysis and its input and additional interpretation in
order to define the possible strategies that could be planned with
the Calabrian basin LSI product. The purpose of the feedback
action is to support the future improvement and refinement of LSI
Product.
The paper deals with the methodology grow up to test the
consistency of PS output data and to assess the efficiency level of
multi-interferometric analysis.
The step of the validation of LSI product was carried out by
_________________________
(*) Autorità di Bacino Regionale, Regione Calabria,
an.pellegrino@regcal.it
ANNAMARIA PELLEGRINO (*) & TIZIANA LA PIETRA (*)
606
considering:
1- the comparison between the LSI Product and PAI/IFFI
alphanumeric and cartographic database, which are necessaries to
every type of “prevision and planning measures” (Fig.2).
2-Cases studies of utilisation and the comparison with
alternative service and information sources.
Fig.1 - Sketch of Terrafirma data base.
These different cases are representative of geological and
geomorphological setting of the Calabrian Arc.
The study of natural slope morphodynamics is an extremely
complex subject. Aspects to be investigated range from
lithological-structural setting, state and type of activity of
landforms and processes, climate and related runoff water and
groundwater circulation, to behaviour of the rock mass and/or
soils involved.
Therefore, it is fundamental to build a geological-evolutionary
model of the slope integrating a multi-disciplinary approaches
with a detailed monitoring of high hazardous active landslides.
The principal goals of this step were: i) a critical analysis of
utility for end-user-ABR; ii) developing a work grid and
specifications comparing the above LSI Product and PAI/IFFI
data.
Paper review first outcomes for the assessment of the practical
advantages and limitations of the experimental PS output data.
Impact and benefit profits were recorded considering the

shielding responsibility of ABR, objective restrictions of multiinterferometric
analysis and a correctly evaluation of the
mismatches of adopted methodological approaches.
Fig.2 - Example of map management, considering different thematic for a correct
quantitative valuation of output data.
607
SESSIONE 17

SESSIONE 17
Grade-2 zonation on susceptibility to seismic-induced landslides in
the Irpinia-Sannio areas, southern Apennines, Italy
Key words: Grade-2 zonation, Irpinia area, landslide
susceptibility, Sannio area, seismic-induced landslides.
INTRODUCTION
The Apennine sector of the Campania region, southern Italy,
is an area with a very high seismic hazard. The shaking related to
the seismicity of this area may be a major cause for landslide
triggering. Therefore, to be effective, the study of the seismic
hazard of such a landslide-prone region must also include a
detailed assessment of the seismic slope stability. For regional
approach analyses, study scales from 1:50,000 to 1:10,000
(grade-2 zonation) are considered proper (FELL et alii, 2008).
Currently, there are only a few grade-2 methods for assessing the
seismic-induced landslide susceptibility (e.g., TC4, 1999;
SAYGILI &RATHJE, 2008), due to the complexity of the different
factors controlling slope stability. A grade-2 study should actually
involve a careful analysis and evaluation of the geological,
geotechnical and geophysical factors that influence the
susceptibility of a site to failures induced by earthquakes.
In this paper we present an application of a new grade-2
zoning method for seismic-induced landslide susceptibility
(RAPOLLA et alii, 2010). Here two different seismic areas of the
Campania Region, Sannio and Irpinia, have been considered.
These zones are characterized by several seismic-induced
landslides, some of them re-activated after the 1980 earthquake
and located many tens of kilometers away from the earthquake
epicenter.
_________________________
(*) Department of Earth Sciences, University of Naples Federico II.
daniela.tarallo@unina.it
(**) C.U.G.RI. - Centre for Research on Major Hazards, Universities of
Naples and Salerno
Paper developed within the research project of national interest PRIN 2007
“Evaluation of geophysical and geological aspects of landslide
susceptibility to severe natural events and relative land zoning” (project
2007LE8ZC5_003, R.U. resp. A.R.)
DANIELA TARALLO (*), ANTONIO RAPOLLA (*) (**), SILVIO DI NOCERA (*),
FABIO MATANO (*) & VALERIA PAOLETTI (*)
608
EARTHQUAKE TRIGGERED LANDSLIDE
SUSCEPTIBILITY
The utilized GIS-based procedure (RAPOLLA et alii, 2010)
employs only three factors that we believe are the most
significant in the susceptibility assessment: i) the type of the
outcropping rock/soil and their properties expressed as
transversal seismic velocities (Vs), ii) the slope angle and iii) the
MCS Intensity (Mercalli-Cancani-Sieberg) characterizing the
area.
The lithological characteristics of the study areas were
obtained from geological maps with 1:25,000 scale (ISPRA –
SERVIZIO GEOLOGICO NAZIONALE, 2010). The investigated
lithologies consist of thin- to thick-bedded conglomerates,
arenites or clastic limestones, and of clays and varicoloured clays,
widespread in the Irpinia and Sannio areas. The attribution of the
representative shear wave velocity value to those units required a
careful evaluation of their geotechnical and geophysical behavior.
Those formations are often characterized by stratified sequences,
with alternations of rock and clay levels that at times are very
thick. The presence of discontinuities and the resulting abundant
presence of water mostly in the rainy period cause abrupt losses
of cohesion and an average behaviour of plastic type, with shear
wave velocities that are significantly lower with respect to normal
conditions (COTECCHIA et alii, 1981). The above described
situation may lead to instability of the slopes, both in static and in
dynamic conditions during earthquakes, particularly in the rainy
periods. These lithological features represent therefore important
predisposing factors to instability. It should be remarked that in
the southern Apennine region climate, the influence of water on
the cohesion is variable during the year being seasonally
dependent. However, the seasonal variability trend may be
considered constant in time. We obviously refer our data to the
worst condition that is during the high rainy periods.
As regards the slope angles, they were obtained from high
resolution digital elevation model (cells of 20 m × 20 m) of the
topography of the investigated areas.
Finally, the choice of the type of seismic data to be used as
input for computing the MCS Intensity characterizing the area
depends on the scale of study. When dealing with a regional scale

the use as seismic input of data derived from the national scale
hazard estimates (e.g.: INGV, 2004; DM, 2008) – accounting for
the influence on the region of several main earthquakes – could
be preferable to the use of the macroseismic field of a specific
event. This latter approach considers instead the “scenario” for
the worst event expected in the specific study area and we believe
it to be more proper when dealing with grade-2 zoning. However,
in this grade-2 study we employed both approaches to make our
analysis more complete.
All these data have been digitized and rasterized with a 20 m
grid spacing. The result of the study was compared with an
upgraded landslide database, obtained by the implementation of
the CEDIT database (ROMEO &DELFINO, 1997) with the Autorità
di Bacino dei Fiumi Liri-Garigliano-Volturno inventory
(CASCINI, 2008) and previous studies, such as ESPOSITO et alii
(1998). The landslide location was then improved by the analysis
of DTM, aerial photography and field data. In the study areas a
hundred seismic landslides were recognized, mainly referred to
slides and flows. Most of these have been reactivated by the
earthquake of 23 November 1980.
The Seismic Landslide Susceptibility levels obtained by using
the Intensity values of the 1980 Irpinia-Lucania earthquake have
been classified in four classes (Fig. 1) showing the degree of
susceptibility in relative terms. The Sannio and Irpinia sectors are
characterized by high susceptibility levels and a large number of
seismic-induced landslides actually occurred there. This
highlights to a very good fitting of the landslides with the
susceptibility areal distribution.
Also by using the PGA values of the Italian national scale
hazard estimates (INGV, 2004) the results show a good match
between the distribution of the sources of historical landslides
and the areas we identified as the most dangerous ones.
Fig.1 – Map of Seismic Landslide Susceptibility level in the Irpinia area
obtained by using the Intensity values of the 1980 Irpinia-Lucania earthquake.
609
REFERENCES
CASCINI L. (2008) Applicability of landslide susceptibility and
hazard zoning at different scales. Eng. Geol., 102, 164–177.
COTECCHIA V. (1981) - Considerazioni sui problemi
geomorfologici, idrogeologici e geotecnici evidenziatisi nel
territorio colpito dal sisma Campano-Lucano del 23
Novembre 1980 e possibilità di intervento del Progetto
Finalizzato “Conservazione del Suolo” del CNR. Rend. Soc.
Geol. It., 4, 73–102.
DM (2008) - Ministry Decree “Nuove Norme Tecniche per le
Costruzioni”. D.M. 14/01/2008, Gazzetta Ufficiale n. 29 del
4 febbraio 2008, Suppl. Ord. 30.
ESPOSITO E., GARGIULO A., IACCARINO G. & PORFIDO S. (1998) -
Distribuzione dei fenomeni franosi riattivati dai terremoti
dell’Appennino meridionale. Censimento delle frane del
terremoto del 1980. Proc. Conv. Int. Prevention of
Hydrogeological Hazards: The Role of Scientific Research
CNR-IRPI, Alba, 1, 409–429.
FELL R., COROMINAS J., BONNARD C., CASCINI L., LEROI E. &
SAVAGE W.Z. (2008) - Guidelines for landslide susceptibility,
hazard and risk zoning for land use planning. Eng. Geol.,
102, 85–98.
INGV (2004) - Redazione della mappa di pericolosità sismica.
INGV, Rome, pp 65. http://zonesismiche.mi.ingv.it/
ISPRA - SERVIZIO GEOLOGICO NAZIONALE (2010) - Carta
Geologica d’Italia 1:5000 - Progetto CARG.
http://www.ispra.it/
RAPOLLA A., PAOLETTI V. & SECOMANDI M. (2010) -
Seismically-induced landslide susceptibility evaluation:
application of a new procedure to the island of Ischia,
Campania Region, Southern Italy. Eng. Geol., 114, 10–25.
ROMEO R. & DELFINO L. (1997) - CEDIT (release 1.1.), Catalogo
Nazionale Effetti Deformativi del Suolo Indotti da Forti
Terremoti, Servizio Sismico Nazionale. Rapporto Tecnico
SSN/RT/97/04, May 1997, pp. 66.
SAYGILI, G. & RATHJE, E.M. (2008) - Empirical Predictive
Models for earthquake-Induced Sliding Displacements of
Slopes. J. Geotech. Geoenviron., 134 (6), 790–803.
TC4 - TECHNICAL COMMITTEE FOR EARTHQUAKE GEOTECHNICAL
ENGINEERING (1999) - Manual for Zonation on Seismic
Geotechnical Hazards. International Society for Soil
Mechanics and Geotechnical Engineering, Japanese
Geotechnical Society, 210 pp.
SESSIONE 17

SESSIONE 17
An attempt to model the relationships between rainfall and landslide
occurrence in Calabria
Key words: Calabria. hydrological modelling, rainfall, slope
movement, triggering.
Calabria (southern Italy) is among the most affected regions
in Europe by severe geo-hydrological events, with remarkable
effects in terms of victims and socio-economic loss. During the
consecutive winter seasons 2008/2009 and 2009/2010, abundant
and prolonged rainfalls hit the region, triggering flooding and
erosion processes, and numerous slope movements of different
types and extent. In 2008/2009, the most affected areas were
mainly located in the NW sector of the region (IOVINE et alii,
2009; VERSACE, 2009), along the eastern slope of the Coastal
Chain, and, subordinately, along its western slope facing the
Tyrrhenian Sea; other villages were also threatened along the
southern Tyrrhenian coast, and the Jonian coast. In 2009/2010,
major effects were recorded again along the inner flank of the
Coastal Chain, with minor processes triggered along the northern
Sila Massif, the south-western portion of the Cosenza province,
and the surroundings of Catanzaro and Vibo Valentia. During
both winter seasons, severe damage was induced to major
lifelines (above all, in the Cosenza province), tens of buildings
had to be evacuated, and 2 victims were caused by a small
landslide along the “A3” highway on 25 January 2009. The most
impressive event occurred on 15 February 2010 at Maierato,
nearby Vibo Valentia, fortunately causing no victims.
Most of the above mentioned landslides were triggered in the
northern portion of the region, within a quite homogeneous
geological, geomorphologic and climatic context (Fig.1). In this
study, a set of slope movements occurring along the western flank
of the Crati graben was selected, thanks to availability of suitable
data concerning the geological setting, the series of historic
events occurred in the last decades, and rainfall series.
The study area extends along the eastern slope of the Coastal
Chain, between the villages of San Marco Argentano and
Cosenza. From a geological point of view (AMODIO MORELLI et
alii, 1976), the area is characterized by outcrops of Palaeozoic
metamorphic and crystalline units, commonly fractured and
weathered, in the western sector, and by late Miocene to actual
sediments in the eastern sector. At the base of the mountain flank,
_________________________
ORESTE G. TERRANOVA (*), STEFANO L. GARIANO (*), PASQUALE IAQUINTA (*) & GIULIO G.R. IOVINE (*)
(*) CNR-IRPI, terranova@irpi.cnr.it, slgariano@gmail.com,
iaquinta@irpi.cnr.it, iovine@irpi.cnr.it
610
a major concave break in slope marks the transition between the
metamorphic/crystalline basement and the sedimentary terrains of
the graben: this morphological element corresponds with a N-S
trending fault system, belonging to the Calabrian-Sicilian Rift
Zone. This latter is a normal fault belt, running along the eastern
coast of Sicily and the western side of the Calabrian Arc, that
developed since Middle Pleistocene due to a regional WNW-ESE
Fig. 1 – Location of the study area (cf. blue dashed line) and main geological
complexes of Calabria (after SORRISO-VALVO, 1993, mod.). Rock units are
grouped according to the main lithological components. Key: 1) carbonate
units of the Apennine range, and limestone cover of Alpine units; 2) very low
to low-grade metamorphic units, at places with ophiolites - these rocks mainly
belong to Alpine units derived from oceanic crust, and only subordinately to
the continental, crust-derived Alpin units (4) or to Apennine units (1); 3)
sedimentary, flysch-type sequence of the lowermost part of the continental,
crust-derived units; 4) intermediate to high-grade metamorphic and intrusive
rocks of the Alpine units derived from continental crust; 5) turbiditic, mainly
coarse-grained deposits; 6) flysch-type nappes, mainly marley- clayey; 7)
flysch-type nappes, with chaotic structure; 8) sedimentary autochthonous
units (Miocene to Holocene). In black, the main tectonic structures belonging
to the Calabrian-Sicilian Rift Zone (after Monaco and Tortorici, 2000, mod.)
are also shown. The sites affected by the main landslide activations occurred
during winter 2008/2009 (a) and 2009/2010 (b) are also shown.

oriented extensional phase (MONACO & TORTORICI, 2000).
Together with the inner portion of the Aspromonte Massif, the
Coastal Chain is one of the rainiest zones of Calabria: here
rainfalls mainly occur during winter and spring, with rare but
notable peaks in autumn. The cold winter air fronts that approach
Calabria from NW commonly cause extremely intense storms.
A first attempt of hydrological modelling was performed to
define triggering scenarios for distinct “classes” of slope
movements (from superficial to deep-seated) in the western flank
of the Crati graben. The adopted model is based on a
hydrological, empirical approach, inspired from FLaiR
(SIRANGELO & VERSACE, 1992). In particular, by assigning
suitable values to model parameters, a threshold of the mobility
function can be identified that allows to predicting the known
landslide activations occurred in the past (or future events), by
minimizing false alarms. The ranges of parameters are related to
specific hydrological conditions that characterize the triggering
events, and then the type of mobilized landslides (Fig.2).
Fig. 2 – Scheme of the adopted hydrological approach.
Model calibration can be performed either on a local or regional
scale of application: the historical series of mobilizations of a
given case study can in fact be considered for a site-specific
analysis, aiming at predicting future activations of a given slope
movement. On the other hand, the times of occurrence of a set of
landslides of the same class, recorded in within a homogeneous
sector of interest, can be used for an areal evaluation of triggering
scenarios. In this study, calibration was performed against a set of
study cases, selected for each class of considered phenomena on
the western flank of the Crati graben. At this purpose, an
automated technique of optimization was adopted based on
Genetic Algorithms, as recently employed for debris flows by
IOVINE et alii (2005). At the local scale a subset of the known
times of occurrence of a given phenomenon was not employed;
likewise, in the analysis performed at the areal scale, the historic
information related to some of the slope movements of the study
area was not considered. In both cases, data not considered for
611
calibration was later on used to validate the model results. The
capability of the model to properly predict the observed events of
activation resulted to depend on suitable input information, while
its efficiency lies on proper characterization of the phenomena of
interest. After describing the modelling approach, the results
obtained for the selected cases of study are discussed, together
with the variation ranges of the parameters obtained for distinct
classes of phenomena.
REFERENCES
AMODIO MORELLI L., BONARDI G., COLONNA V., DIETRICH D.,
GIUNTA G., IPPOLITO F., LIGUORI V., LORENZONI S. et al.
(1976) - L'arco Calabro-peloritano nell'orogene
appenninico-magrebide. Mem. Soc. Geol. It., 17, 1-60.
IOVINE G., IAQUINTA P. & TERRANOVA O. (2009) - Emergency
management of landslide risk during Autumn-Winter
2008/2009 in Calabria (Italy). The example of San Benedetto
Ullano. In: R.S. Anderssen, R.D. Braddock and L.T.H.
Newham (Eds.) - Proc. 18th World IMACS Congr. and
MODSIM09 Int. Congr. on Modelling and Simulation,
Cairns, 2686-2693.
IOVINE G., D’AMBROSIO D. & DI GREGORIO S. (2005) – Applying
genetic algorithms for calibrating a hexagonal cellular
automata model for the simulation of debris flows
characterised by strong inertial effects. Geomorphology,
66(1-4), 287-303.
MONACO C. & TORTORICI L. (2000) - Active faulting in the
Calabrian arc and eastern Sicily. J. Geodyn., 29, 407-424.
SIRANGELO B. & VERSACE P. (1992) - Modelli stocastici di
precipitazione e soglie pluviometriche di innesco dei
movimenti franosi. In: Proc. XXIII Convegno Nazionale di
Idraulica e Costruzioni Idrauliche, Firenze, 3, D361–D373.
SORRISO-VALVO G.M. (1993) - The geomorphology of Calabria
– a sketch. Geogr. Fis. Din. Quat., 16 (1), 75-80.
VERSACE P. (2009) - Relazione di sintesi e schede di sopralluogo.
Prefettura di Cosenza - Ufficio Territoriale del Governo -
Gruppo di valutazione per l’emergenza idrogeologica.
Conference CD, ORG-Calabria.
SESSIONE 17

SESSIONE 17
612

SESSIONE 18
Geologia delle conche intermontane
CONVENERS
Marco Pantaloni (Servizio Geologico d'Italia Roma)
Maurizio D'Orefice (Servizio Geologico d'Italia Roma)
Fernando Calamita (Università degli Studi di Chieti “G. d'Annunzio”)
613
SESSIONE 18

SESSIONE 18
New chrono-stratigraphic data on the Boiano basin infilling
(Molise, Italy)
VINCENZO AMATO (*), PIETRO P.C. AUCELLI (**), MASSIMO CESARANO (*), GERARDO PAPPONE (**),
PAOLA PETROSINO (°), CARMEN M. ROSSKOPF (*) & ELDA RUSSO ERMOLLI (°)
Key words:, 40 Ar/ 39 Ar dating, intramountain basin, Italy, Middle
Pleistocene, Molise, palaeoenvironment, tephro-stratigraphy.
INTRODUCTION AND PREVIOUS KNOWLEDGE
The Boiano basin (ca. 500 m a.s.l.) is located between the
carbonate Matese and Montagnola di Frosolone massifs and the
adjacent Sannio hills (Fig. 1). It is a 4 km large tectonic
intramountain depression, elongated 20 km in a NW-SE
direction, and nowadays drained by the Biferno river. The
Fig. 1 –Geological scheme of the Matese-Montagnola di Frosolone area. 1)
fluvial-palustrine deposits (Quaternary); 2) Foredeep and piggy-back
siliciclastic deposits (Miocene); 3) Clays, marls and limestones of the Sannio
Unit (Upper Cretaceous-Miocene); 4) Limestones, dolomites and marls of the
inner carbonate platform (a) and carbonate slope deposits (b) (Triassic-
Miocene) 5) Main thrusts, dashed when inferred 6) Main extensional faults,
dashed when inferred.
deformation history of this basin is characterized by several
compression phases occurred between Miocene and Pliocene,
followed first by strike-slip tectonics and then, since Middle
Pleistocene, by extensional tectonics (DI BUCCI et alii, 2002, with
references). Main faults show a NW-SE trend and several of them
are still active and responsible for the historical and present
seismicity. Even if the tectonic evolution of the basin was
investigated in detail, little is known about the stratigraphy and
chronology of its Quaternary infilling. Only in the SE sector of
_______________________
(*) Università del Molise, vincenzo.amato@unimol.it
(**) Università Parthenope di Napoli, p.aucelli@alice.it
(°) Università Federico II di Napoli, ermolli@unina.it
614
the basin (Campochiaro area) it is ascertained that the infilling
consists of at least 200 m of fluvial-lacustrine deposits of Middle
Pleistocene to Holocene age (RUSSO &TERRIBILE, 1995). Other
chrono-stratigraphical constraints come from S. Massimo (Fig.1),
along the NW side of the Matese massif, where residual strips of
fluvio-lacustrine sediments, cropping out at 300 m above the
present plain, were 40 Ar/ 39 Ar dated to 0.6 Ma (DI BUCCI et alii,
2005).
Fig. 2 – Geological map of the Boiano area and location of cores
NEW CHRONO-STRATIGRAPHIC DATA
To increase the data currently available on chronostratigraphy
of the Boiano Quaternary infilling we analyzed in
detail data coming from some drilled boreholes (B6, B2, B1 and
M1; Fig. 2), together with those coming from a 160-m borehole
which we appositely drilled in the area of Boiano (482 m asl; Fig.
2 and 3). The S1 core (Fig. 2) which did not reach the pre-
Quaternary bedrock, allowed the reconstruction of a detailed
stratigraphy and the correlation with the other examined core
successions. The most significant levels were investigated by
means of tephro-stratigraphy (MOL initials, Fig. 3) and
palynology which considerably contributed to improve the
chrono-stratigrapical and paleo-environmental knowledge. The
chronological framework was more clearly constrained through
the 40 Ar/ 39 Ar dating of a tephra layer sampled in the S1

succession at 122 m of depth (MOL 13). The drilled successions
were subdivided, according to the UBSU criteria, into three lithostratigraphic
units: two units buried below the plain (UQS1 e
UQS2), and one unit, cropping out in different sectors of the
plain (UQS 3) (Fig. 3). The lowermost, 85 m thick unit (UQS1) is
Fig. 3 – Stratigraphic log of the Boiano core (S1) with litho-stratigraphic,
tephrostratigraphic and chronological results.
mainly made up of clayey levels, at times peaty and laminated,
and of silty-clayey levels rich in reworked volcanoclastic
material. Lithofacies testify alternating lacustrine and palustrine
environments and rare alluvial episodes. Two pyroclastic layers,
mainly made up of white coarse pumice fragments and grayish
ashes, were sampled at 122 and 112 m of depth, respectively
(MOL 13 and MOL 12). These levels were analyzed and MOL
13 was 40 Ar/ 39 Ar dated to 426 ±5.5 ka. Tephro-stratigraphic
analysis allowed these levels to be ascribed to the distal products
of the Roccamonfina volcano. In this unit, preliminary pollen data
show, from the base, the occurrence of a sequence of alternating
interglacial-glacial-interglacial phases. The age of 426 ka is
consistent with the floral and vegetation pattern of the glacial
phase of the Oxigen Isotopic Stage (O.I.S.) 12. The basal
interglacial period was then ascribed to O.I.S. 13. The 80-75 m
interval recorded as well a forested landscape similar to that
detected at the core base and thus possibly can be correlated to
O.I.S. 11. As regards the paleoenvironmental aspects, the
constant presence of Cyperaceae and spores in pollen spectra is
consistent with the persistence of marshy conditions and humid
soils around the site, as suggested by the sediments facies.
Exposed data indicate that the first filling cycle of the Boiano
basin was lacuo-palustrine and can be referred to a time interval
from O.I.S. 13 to O.I.S. 11 (from ca. 500 to 400 ka). In about 100
ka, 85 m of lacuo-palustrine sediments were deposited with a
615
mean sedimentation rate of ca. 1 mm/a, suggesting that the
Boiano area was strongly subsiding. Unit UQS1 is limited at its
top by a clear erosion surface (Fig. 3), well marked by an abrupt
lithologic change. The second buried unit (UQS2), 45 m thick,
consists of silty and sandy levels, at times rich in organic matter
or altered, as typical in environments with alternating subaerial
and submerged conditions. Towards the top, frequent sandy and
gravel levels of fluvial origin are found. At ca. 70 m of depth a
coarse white pumice layer with grey ash (MOL 11) and a
decimetre-thick reworked volcanoclastic layer (MOL 10) were
sampled. Tephrostratigraphic analysis of these layers allowed
their correlation to the Roccamonfina eruption known as the
White Trachytic Tuff (WTT), recently dated to 331±2 ka. Pollen
data from this core interval suggest the occurrence of an
interglacial period which should correspond to O.I.S. 9, as the
age of the WTT suggests. Also this unit is characterized at its top
by a clear erosion surface, well marked by an abrupt lithologic
change. Unit UQS3, partly cropping out, is about 30 m thick and
consists of alternating silty and sandy layers, at times peaty or
altered as typical in environments with alternating subaerial and
submerged conditions, testified by the occurrence of alluvial
sands and gravels, more frequent near the top. A pyroclastic fall
deposit at 10 m of depth, dark orange in color and containing
yellow pumices, was analyzed and referred to the Neapolitan
Yellow Tuff (NYT; 15 ka). The presence of the NYT and of
archeological levels in the uppermost part of the succession
allows this unit to be ascribed to the Late Pleistocene-Holocene.
The three described units were also recognized in the B6 and M1
boreholes, where both the volcanic layer, the WTT and the layer
dated to 426 ka, are present at 21 and 38 m of depth, respectively.
The different altitudes at which the these levels were found in the
cores suggests the presence of a fault between boreholes B6 and
S1, passing through the Boiano town. Acquired chronostratigraphic
data indicate that this fault was active during Middle
Pleistocene and, very likely, still during Late Pleistocene and
Holocene, as strongly suggested by the persistence of marshy
environments in the Boiano sector until historical times.
REFERENCES
DI BUCCI D., CORRADO S. & NASO G. (2002) - Active faults at the
boundary between Central and Southern Apennines (Isernia,
Italy). Tectonophysics, 359, 47-63.
DI BUCCI D., CORRADO S., NASO G. & VILLA I. M. (2005) Growth
interaction and seismogenic potential of coupled active
normal faults (Isernia Basin, central-southern Italy). Terra
Nova, 17, 1, 44-55
RUSSO F. & TERRIBILE F. (1995) – Osservazioni
geomorfologiche, stratigrafiche e pedologiche sul
Quaternario del Bacino di Boiano (Campobasso). Il
Quaternario, 8 (1), 239-254.
SESSIONE 18

SESSIONE 18
The minor semi-graben of the Elsa River upper reach:
a hydrographic puzzle
CARLO BARTOLINI (*), CARLO TACCONI STEFANELLI (*), ENRICO CAPEZZUOLI (**) & FABIO SANDRELLI (**)
Key words: Elsa River, Middle – Late Pleistocene uplift,
Montagnola Senese, river capture.
INTRODUCTION
The morphologic setting of the upper reach of the Elsa River
is rather peculiar. For less than three km length, the River flows
WSW in a relatively narrow valley, then it sharply bends with an
elbow to the right entering a wide valley (Fig. 1), which
manifestly antedates the onset of the present hydrographic
pattern. The windgap (see for instance BARTOLINI &PECCERILLO,
2002, p.51) between the now underfit Elsa R. and the
neighbouring Rosìa R. is located at Podere Poggiaccio, a few
hundred meters southward from the Elsa elbow (Fig. 1).
Fig. 1 – Morphologic setting (modified after http://maps.google.it/maps).
The onset of the wide and straight valley, extending for
approximately 12 km, is clearly connected to the normal fault
which borders to the west this sector of the Montagnola Senese
(Fig. 2). The fault line depression bears an elongated outcrop of
_________________________
(*) Dip. Scienze della Terra, Univ. di Firenze, bartolini@unifi.it.
(**) Dip. Scienze della Terra, Univ. di Siena, capezzuoli@unisi.it.
616
Middle Pliocene sediments, relic of a widespread sedimentary
blanket extending much further to the east. Due to the relevant
Middle–Late Pleistocene uplift which affected the area, the
Pliocene sediments have been elsewhere extensively wiped off.
The present course of the Elsa R. is the outcome of a piracy
event carried out by the Rosia R., which flows eastward, at right
angle from the underfit valley, towards the nearby Sovicille
intermountain basin (Fig. 1).
Three questions arise:
i) is there any sedimentological evidence of a former Elsa R.
extending southward beyond the windgap of Podere
Poggiaccio?
ii) which relevant event prompted the capture operated by the
Rosia R., thus overwhelming the role of the upper Elsa semi
graben as master control of the hydrographic network in the
area?
iii) when did the capture take place?
DISCUSSION
As to the first question, the straight reach of the Elsa valley
down to Molino d’Elsa, where it gently bends to the right, does
not bear evident traces of fluvial terraces. Most alluvial
sediments, at places outcropping in the valley bottom, belong to
alluvial cones fed by tributaries draining the Montagnola. The
presently underfit Elsa R. is unsuited to get in charge such
deposits. One of these cones, now deeply dissected, possibly
produced the westward diversion of the Elsa R. near the village of
Pievescola. The dry valley trending NE from Pievescola bears,
near Villa San Chimento, rounded gravel of the Triassic
Anageniti minute Fm. which, as such, cannot be of local origin
but rather must have been laid by a longitudinal water course
draining to the north. The closest outcrops of Anageniti minute
Fm. are presently found in the upper Feccia R. basin, far south of
the Podere Poggiaccio, i.e. of the Elsa/Rosìa divide.
The event which prompted the beheading of the former Elsa
R. due to the Rosìa river head retreat (ii) was most likely the
uplift of the area and namely of the Montagnola Senese. The
Rosìa R. took advantage of this uplift because of its base level
located on the subsiding Sovicille basin at a relatively short
distance from the former Elsa R. The Rosìa river head retreat was
moreover prompted by its location at the Verrucano/Calcare

Fig. 2 – Geological cross section of the upper Elsa Valley (modified after COSTANTINI et alii, 2009).
cavernoso contact where karstic underground erosion is favoured.
As to the age of the capture (iii), according to CAPEZZUOLI et
alii (2009, with reference therein), the uplift quietly began, in the
southern Valdelsa Basin, with the deposition of the Campiglia di
Foci Synthem, spanning the time interval of 500 to 250 ky. An
acceleration of the uplift took place after the onset of the Abbadia
Synthem, dated at approximately 50 ky. The initial uplift predates
the capture.
REFERENCES
BARTOLINI C. & PECCERILLO A. (2002) – I fattori geologici delle
forme del rilievo. Lezioni di Geomorfologia strutturale.
Pitagora Editrice, Bologna, 216 pp.
CAPEZZUOLI E., PRIORI S., COSTANTINI E.A.C. & SANDRELLI F.
(2009) - Stratigraphic and paleopedological aspects from the
Middle Pleistocene continental deposits of the southern
Valdelsa Basin. Ital. J. Geosci., 128 (2), 395-402.
COSTANTINI A., DECANDIA F.A., LAZZAROTTO A., LIOTTA D.,
MAZZEI R., PASCUCCI V., SALVATORINI G.F. & SANDRELLI F.
617
(2009) - Note illustrative della Carta Geologica d’Italia alla
scala 1:50.000, Foglio 296: Siena. APAT - Agenzia per la
protezione dell’ambiente e per i servizi tecnici, Dipartimento
Difesa del Suolo - Servizio Geologico d’Italia, 131 pp.
SESSIONE 18

SESSIONE 18
Key words: Amatrice Basin, central Apennines, intermontane
basin, Mt. Gorzano fault.
The Amatrice Basin occupies the northern part of a broad
NNW-SSE stretching depression that includes, to the south, the
Campotosto basin. The entire depression is bounded on the
eastern side by the Mt. Gorzano normal fault that seems to have
determined its formation and controlled its subsequent
development. This fault is also considered to be presently active
and potentially seismogenic (BLUMETTI et alii, 1993; GALADINI &
GALLI, 2003; BONCIO et alii, 2004).
The catchment area of the Amatrice basin is mostly developed
on the Mt. Gorzano fault hanging wall (Fig. 1). The relative
movement - eastern side up - on the West-dipping Mt. Gorzano
fault determined the Marne con Cerrogna (calcareous marls and
marls; Burdigalian-Tortonian) and Marne a Pteropodi (marls;
Tortonian-Messinian) formations to become exposed on its foot
wall. Except for a small sector on its far western edge, the rest of
the catchment area is dominated by the Laga formation
(Messinian), a quartz-rich sandstone dominated succession
(CORDA &MORELLI, 1996). Significant continental deposits are
only found on the eastern side of the catchment, in a small sector
between the Tronto River (the main river of the basin) and the
trace of the Mt. Gorzano fault. Because of the lack of elements
for direct dating, their age is poorly constrained and based only
on regional correlation with other Apennines intermontane
basins. Generally, these continental deposits have been
subdivided into three depositional units, one of which is
proportionally very minor and scattered, that are attributed to the
Lower Pleistocene - Upper Pleistocene (CACCIUNI et alii, 1995).
To gain insight into the long-term activity of the Mt. Gorzano
fault and its role in controlling the evolution of the Amatrice
basin, we carried out a stratigraphic and geomorphic analysis of
the continental deposits.
_________________________
Provenance of the Amatrice Basin (central Apennines) infill:
implications for the long-term activity of the Mt. Gorzano fault
(*) Istituto Nazionale di Geofisica e Vulcanologia, Sezione di Sismologia e
Tettonofisica, roberto.basili@ingv.it
(**) ISPRA, Servizio Geologico d’Italia/Dipartimento Difesa del Suolo,
chiara.dambrogi@isprambiente.it
This research has benefited from funding provided by the Italian Presidenza
del Consiglio dei Ministri - Dipartimento della Protezione Civile (DPC).
Scientific papers funded by DPC do not represent its official opinion and
policies.
ROBERTO BASILI (*) & CHIARA D’AMBROGI (**)
618
We positively identified two clastic continental units within
the main depositional body that filled up the Amatrice basin. Just
downstream from the River Tronto head, the steep valley walls of
a deeply incised gorge provide a comprehensive exposure of the
Fig. 1 – Geological sketch map of the Amatrice basin. Legend: a) normal
fault; b) catchment limit; c) Continental deposits (Quaternary); d) Laga
formation (Messinian); Marne a Pteropodi (Tortonian-Messinian) and Marne
con Cerrogna (Burdigalian-Tortonian) formations. Arrow points at the
location of the Quaternary deposit exposure shown in figure 2.
lower and older unit. This is a coarse, moderately rounded,
gravel-to-cobble, clast-supported, up to 30 meters thick
conglomerate. Its composition is almost exclusively made up of
arenaceous clasts derived from the Laga formation. Occasionally,
the sedimentary fabric suggests a roughly south-to-north direction
of transport.
The higher and younger unit is exposed near the top of the
Tronto River gorge and in a number of stream incisions and road
cuts. This is a coarse, moderately rounded, gravel-to-cobble,
clast-supported, up to 10 meters thick conglomerate with
interspersed boulders. Its composition is predominantly made up
of arenaceous clasts derived from the Laga formation but the
calcareous component derived from the Marne con Cerrogna
formation is clearly identifiable and measurable (Fig 2). The
chaotic fabric and the reduced level of clast roundness suggest a

Fig. 2 – Left: exposure of the Quaternary continental deposit of the Amatrice basin infill (See Fig. 1 for location). Right: clasts of the Marne con Cerrogna
formation are outlined; circles indicate clasts of about 1 cm in diameter. Each square of the grid in the foreground of both panels is 50x50 cm.
very local sediment supply from the near slope to the East of the
basin. This deposit evolves gradually upward into coarse-to-fine,
variously weathered, eluvial sand and to the top soil. Its top
depositional surface coincides with a broad plateau, occasionally
overlain by younger debris fans.
Our preliminary estimations show that the relative content of
the calcareous component within the younger unit is of about 5-
6%. This is a lower limit because we ignore the relative content
within the matrix that we assigned by default to the arenaceous
component. A more detailed provenance analysis of the
calcareous component shows that a significant number of clasts
were derived from the lower and older portion of the Marne con
Cerrogna formation. The relative content between arenaceous and
calcareous components in the source area, i.e. the mountain slope
on the eastern side of the basin, is about 7-16%.
Considering all sources of uncertainty in these estimates,
including that the calcareous clasts are more subject to chemical
weathering than the arenaceous clasts, we can consider the
relative abundance of calcareous rock in the source area and
within the continental deposit to be rather similar to one another.
This implies that the Marne con Cerrogna formation should have
been already exposed at the time when the continental unit at the
top of the Amatrice basin infill was deposited. We suggest that
the careful estimation of these relative abundances will help
provide an estimate of the relative increment of geological
displacement on the Mt. Gorzano fault and the resulting
increment in the Marne con Cerrogna formation exposure since
the time of depositional abandonment of the younger continental
unit.
REFERENCES
BLUMETTI A.M., DRAMIS F., & MICHETTI A.M. (1993) – Faultgenerated
mountain fronts in the central Apennines (central
b)
619
Italy): geomorphological features and seismotectonic
implications. Earth Surf. Proc. Land., 18, 203-223.
BONCIO P., LAVECCHIA G., MILANA G. & ROZZI B. (2004) –
Seismogenesis in Central Apennines, Italy: an integrated
analysis of minor earthquake sequences and structural data
in the Amatrice-Campotosto area. Ann. Geophys., 47, 1723-
1742.
CACCIUNI A., CENTAMORE E., DI STEFANO R. & DRAMIS F.
(1995) – Evoluzione morfotettonica della Conca di Amatrice.
Studi Geol. Camerti, Vol. Spec. 2, 95-100.
CORDA L. & MORELLI C. (1996) – Compositional evolution of
the Laga and Cellino sandstones (Messinian-Lower Pliocene,
Adriatic foredeep). Boll. Soc. Geol. It., 115, 423-437.
GALADINI F. & GALLI P. (2003) – Paleoseismology of silent faults
in the Central Apennines (Italy): the Mt. Vettore and Laga
Mts. faults. Ann. Geophys., 46, 815-836.
SESSIONE 18

SESSIONE 18
Quaternary intermontane basins in the Central Apennines inherited
from pre-thrusting normal faults
Key words: Central Apennines, intermontane basins, inversion
tectonics.
The Central-Northern Apennine is characterized by curved
shapes described by NW-SE trending fold-and-thrust structures
and two main NNE-SSW features, the Olevano-Antrodoco and
the Sangro-Volturno oblique thrust ramps, that sign the
separation between the different sectors of the Apennines (e.g.,
PATACCA et alii, 1990). Starting from Neogene, the Apennines
were characterized by coeval occurrence of normal and thrust
faults along the western and eastern belt margins, respectively
(ELTER et alii, 1975).
At present, the Central-Northern Apennine is a tectonically
active region: the external compressive front of the chain is
characterized by M < 5 (PACE et alii, 2006 and references
therein) and ipocentral depth of 15-30 km; the axial zone is
characterized by syn-orogenic seismic extensional events in the
upper crust (up to 15 km) with M=7 (CALAMITA &PIZZI, 1994;
GALADINI &GALLI, 2000); furthermore transcurrent mechanism
characterize the Marchean pede-Apennines, Umbrian pre-
Apennines and Molise-Puglia foreland areas.
Particularly, the NW-SE trending normal fault systems show
historical and seismical activity (PIZZI & GALADINI, 2009). They
are characterized by 15 to 35 km of length and vertical
displacement of hundred meters and cause the development of
intermontane basins filled by Quaternary deposits in the
backlimbs of Neogene compressive structures.
For many of these structures, pre-thrusting activity linked to
the Jurassic Adria paleomargin or to the Neogene foreland basins
with siliciclastic sedimentation is documented (SCISCIANI et alii,
2002). During Neogene positive inversion tectonics, the NW-SE
and WNW-ESE trending pre-thrusting normal faults were
displaced and passively translated in the hangingwall blocks of
the thrust planes, while the N-S to NNE-SSW trending prethrusting
normal faults were reactivated in a transpressive
deformational context (CALAMITA et alii, 2009). As a
consequence, NW-SE trending pre-thrusting normal faults are
passively translated in the western limb of anticlines and are
_________________________
FERNANDO CALAMITA (*), SARA SATOLLI (*) & ALESSANDRA DI DOMENICA (*)
(*) Dipartimento di Scienze, Università “G.d’Annunzio” of Chieti-Pescara,
calamita@unich.it
620
confined by NNE-SSW features of the chain. Such faults have
been reactivated during the Quaternary negative inversion
tectonics event and border the intermontane basins of the Central
Apennines.
The NW-SE fault systems are fully activated during larger
seismic events (M ~ 7) and only partly activated during smaller
events. However, they are confined by the main transversal
structures (Olevano-Antrodoco-Sibillini, Gran Sasso E-W
oblique thrust ramps). The spacing of normal faults and thickness
of fragile crust control the segmentation and longitudinal grown
of active normal faults. Morever, ipocentre location and energy
relase associated with earthquakes in the different sectors of the
chain are confined by transpressive oblique thrust ramps
(Valnerina, Olevano-Antrodoco- Sibillini, Sangro-Volturno, Gran
Sasso).
This observation is in accordance with the distribution of the
recent seismic sequence of L’Aquila that displays an evident gap
close to the E-W Gran Sasso oblique thrust ramp that split the
whole seismicity of the Laga Mountains, related to the Monte
Gorzano fault, from the L’Aquila seismicity, associated with the
Paganica fault.
The relation between NW-SE normal fault systems and the
NNE-SSW oblique thrust ramps is crucial in fault segmentation
analysis and, hence, in seismic hazard assessment, due to the
ability of pre-existing cross-structure to control the faults growth.
In such context is possible to reconstruct (according to
MANTOVANI et alii, 1997, and CALAMITA et alii, 2009 and
references therein) a dynamic model for the Central-Northern
Apennines of lateral extrusion caused by a maximum stress axes
oriented NNW-SSE and linked to the Africa-Europe convergence
(Fig. 1). The lateral extrusion of the Central-Northern Apennine
arc causes compression in the frontal part of the belt and
extension in its axial part, locate in the hangingwall of the
lithospheric thrust ramp. Such extensional process causes the
reactivation of NW-SE pre-thrusting normal faults,
compartmentalized by Pliocene oblique thrust ramps. Whereas,
the strike-slip deformation in the Marchean pede-Apennines,
Umbrian pre-Apennines and Molise-Puglia foreland areas can be
interpreted as a direct consequence of the remote stress field
related to the Africa-Europe convergence.

Fig. 1 - Schematic representation of the Central Apennines active tectonic context. Focal mechanism and main geological structures (active: grey; inactive:
black) are represented. Big grey arrows represent the direction of the maximum remote stress induced by the Africa-Europe convergence, responsible of lateral
extrusion of the Northern-Central Apennines arc.
REFERENCES
CALAMITA F., PIZZI A., SCISCIANI V., SATOLLI S. & POMPOSO G.
(2009) – Assetto tettonico e sismicità nell’Appennino
centrale. Riassunti del 28° Convegno GNGTS.
CALAMITA F. & PIZZI A. (1994) – Recent and active extensional
tectonics in the southern umbro-marchean Apennines (central
Italy). Mem. Soc. Geol. It., 48, 541-548.
ELTER, P.,G.GIGLIA, TONGIORGI M., & TREVISAN L. (1975) –
Tensional and compressional areas in recent (Tortonian to
Present) evolution of north Apennines. Boll. Geofis. Teor.
Appl., 17, 3 – 18.
GALADINI F. & GALLI P. (2000) – Active tectonics in the Central
Apennines (Italy) – input data for Seismic Hazard
Assessment. Nat. Hazards, 22, 225-270.
MANTOVANI E., ALBARELLO D., TAMBURELLI C., BABBUCCI D. &
VITI M. (1997) – Plate convergence, crustal delamination,
extrusion tectonics and minimization of shortening work as
621
main controlling factors of the recent Mediterranean
deformations pattern. Ann. Geofis., 40, 611-643.
PACE B., PERUZZA L., LAVECCHIA G. & BONCIO P. (2006) –
Layered seismogenic source model and probabilistic seismichazard
analyses in central Italy. B. Seism. Soc. Am., 96, (1),
107-132.
PATACCA E., SARTORI R. & SCANDONE P. (1990) – Tyrrhenian
basin and Apenninic arcs: Kinematic relations since Late
Tortonian time. Mem. Soc. Geol. It., 45, 425-451.
PIZZI A. & GALADINI F. (2009) – Pre-existing cross-structures
and active fault segmentation in the northern-central
Apennines (Italy). Tectonophysics, 476, 304-319.
SCISCIANI V., TAVARNELLI E. & CALAMITA F. (2002) – The
interaction of extensional and contractional deformations in
the outer zones of the Central Apennines, Italy. J. Struct.
Geol., 24, 1647-1658.
SESSIONE 18

SESSIONE 18
Key words: Gravity prospecting, L’Aquila, Middle Aterno Valley,
quaternary deposits, seismic amplification.
A gravity study was carried out to identify the geological and
structural features of the Middle Aterno Valley. It was targeted to
assess the seismic hazard of the city of L’Aquila and surrounding
areas, after the Abruzzo 2009 earthquake.
In this study a set of approximately 2000 gravity stations
measured partly by the Servizio Geofisica of ISPRA and partly
by the University of Rome were used. New stations were
established in some critical areas with a nearly homogeneous
distribution and a data separation of 500 m: more than 100
gravity stations have been located on L’Aquila city (BLUMETTI et
alii, 2002). All the available data have been reprocessed and
uniformed.
The Bouguer anomaly map was computed using a density
value of 2600 kg/m 3 for both Bouguer and terrain corrections. It
has been drawn with 1 mGal contour interval taking into account
an estimated error affecting the data of 0.020 mGal.
Gravity anomalies have been used for the construction of a
3D model of the area. These data, together with geological
surface data allowed for the understanding of the Plio-quaternary
tectonic setting of the basin.
The study area has been differentiated into different domains
with respect to structural and morphological features of different
styles of faults.
Geology and gravity data show that the local amplification
phenomena are due to the fact that the historical center of
L’Aquila was built on a coarse breccias (debris-flow deposits
with decameter scale limestone blocks) overlying sandy and
clayey lacustrine sediments. As these sediments have a low
density, gravity prospecting very easily identifies them. Residual
anomalies, showing a relative gravity low corresponding to the
historical center of L’Aquila, and surrounding areas, indicated
that these sediments are up to 250 m-thick.
_________________________
Gravity features of the Middle Aterno Valley
MARIA DI NEZZA (*), MICHELE DI FILIPPO (*) (°) & FERNANDO FERRI (**)
(*) Dipartimento di Scienze della Terra, Università “Sapienza” di Roma,
mariahdn@tin.it
(**) Dipartimento Difesa del Suolo, Servizio Geofisica, ISPRA,
fernando.ferri@isprambiente.it
(°) IGAG-CNR, michele.difilippo@uniroma1.it
This work was partially funded by the Italian Dipartimento della Protezione
Civile in the frame of the Ordinanza n. 3772 19 May 2009.
622
Gravity prospecting also revealed the uprooting of the Meso-
Cenozoic reliefs which outcrop in the middle of area the basin in
the area of Coppito. Here, the gravity anomalies are negative and
not positive as would be expected from outcropping geological
bedrock.
Gravity prospecting showed that paleo-landslide and debris
flow deposits have a considerable thickness and influenced the
Quaternary evolution of the Middle Aterno Valley. Moreover
steep gradients of residual anomalies are indicative of other
structural alignments. The residual anomalies trends show a
complex geometry of the buried geological bedrock. This buried
morphology is conducive to strong propagation of seismic waves.
Based on residual anomalies a gravity model was built, which
cross-cuts the Middle Aterno Valley in a NNE-SSW direction
(Fig.1). The computation showed a considerable thickness of the
Quaternary sediments.
Fig. 1 – Elevation longitudinal profile, residual gravity anomaly (solid line)
and regional anomaly (dashed line) along the Aterno river.
REFERENCES
BLUMETTI A.M., DI FILIPPO M., ZAFFIRO P., MARSAN P. & TORO
B. (2002) – Seismic hazard characterization of the city of
L’Aquila (Abruzzo, Central Italy): new data from geological,
morphotectonic and gravity prospecting analysis. In F.
Dramis, P. Farabollini and P. Molin (Eds) - Large-scale
vertical movements and related gravitational processes. Stud.
Geol. Camerti, Vol. Sp., Int. Workshop Camerino - Rome,
21-26 Giugno 1999, 7-18.
DI NEZZA M., DI FILIPPO M., CESI C. & FERRI F. (2010) – Gravity
study of the Middle Aterno Valley. Geophys. Res. Abstracts,
12, EGU2010-14163.

Key words: Aterno, geoelectric, geophysics, gravity,
intermountain basin.
INTRODUCTION
This paper presents some preliminary results of geophysical
surveys undertaken by the Servizio Geofisica of ISPRA in three
intermountain basins located in the upper Aterno river valley
(Abruzzo) West of L’Aquila city, i.e. from SE to NW, the
Aquila-Coppito, Pizzoli and Montereale plains.
The study area is of particular interest due to the relevant
seismic activity in the Aterno valley from Pleistocene to Present
(GRUPPO DI LAVORO CPTI, 2004). Among several active faults
which are present in the area (BOSI, 1975; BLUMETTI et alii,
1996; GALADINI et alii, 2000), the Monte Pettino fault is located
on the NE border of the Aquila-Coppito basin, the Monte Marine
fault is on the NE limit of the Pizzoli basin and the Capitignano
fault on the NE border of the Montereale basin. On April 6 th 2009
an earthquake (Ml = 5.8; Mw = 6.2) occurred near L'Aquila
(INGV, 2009) as a result of fault dislocation on a NW-SE
oriented extensional structure. The seismic sequence occurred not
only in the Aterno valley but also in the Campotosto (aftershock
of Mw 5.4) and Montereale area.
GRAVITY ANOMALIES
A new compilation of gravity data is presented in the form of
Bouguer and residual anomaly maps. 640 ENI gravity
observations from the Geophysical Database of ISPRA and 506
unpublished gravity measurements by the Servizio Geofisica of
ISPRA were used. The latter gravity survey was specifically
targeted to improve the knowledge on the deep geological setting
of the basins.
Bouguer anomalies were computed using modern standards
(FERRI et alii, 2007; FERRI et alii, 2008): the topographic
correction was processed using high resolution digital elevation
_________________________
(*) ISPRA, fernando.ferri@isprambiente.it
Geophysical surveys in some intermountain basins
of the Central Appenines
FERNANDO FERRI (*), VALERIA EULILLI (*), LUCA MARIA PUZZILLI (*),
STEFANO CALCATERRA (*) & CLAUDIO PULSINELLI (*)
623
models and a spherical cap was used for the computation of the
Bouguer correction. The density value used is 2.67 g/cm 3 and can
be referred to the meso-cenozoic carbonatic terrains outcropping
along the borders of the plains.
A Regional gravity field, computed using a 2 nd order
polynomial surface fitted to the gravity data of Central Italy, was
subtracted from the Bouguer anomalies in order to obtain
Residual anomalies that correlate better with the local structures
of interest.
The analysis of the Bouguer (Fig.1) and Residual maps shows
that the main gravimetric discontinuities with higher gradient are
usually located on the North Eastern and South Western borders
of the basins, following the main NW-SE structural trends of the
area. Moreover the gravity maps also show that this general
feature is often complicated by NE-SW discontinuities with the
result that the Quaternary deposits thickness is often highly
Fig. 1 – Bouguer Anomalies (contour interval 1 mGal), the outlines of the
intermountain basins and the Campotosto lake are also showed, points are
gravity stations.
SESSIONE 18

SESSIONE 18
variable. In some instance there is evidence that isolated outcrops
of meso-cenozoic deposits are uprooted, confirming the findings
of earlier studies (BLUMETTI et alii, 2001). Gravity modelling
was also used to support the interpretation of the basins
subsurface and reveals the geometry of the carbonate bedrock and
of the master normal faults. The gravity models also show the
presence of subsurface faults, subsidiaries of the known main
systems.
GEOELECTRIC TOMOGRAPHIES
At the eastern border of the Montereale plain geoelectrical
arrays have been conducted in order to support the findings of the
ongoing geological survey and to confirm the existence of some
buried extensional faults which lower the flysch substratum and
trend NW-SE, parallel to the Capitignano fault. The Quaternary
cover consists of talus, fluvial, lacustrine deposits and debrisflows,
with a growing thickness towards the plain center. Three
geoelectrical tomographies (ERT) using Wenner and dipoledipole
arrays were mesured, each profile with a lenght of 950 m:
the measured resistivity of the different sedimentary layers,
calibrated with preliminary stratigraphic informations from
boreholes, allows a good resolution for superficial covers
whereas the resistivity contrast is not enough to define limits and
geometries of deeper bodies.
These preliminary results suggest a wider use of this method
in the future in order to obtain a greater detail using different
arrays and electrode spacings, moreover to confirm the presence
of the assumed dislocations.
In the framework of an ongoing multidisciplinary work on the
evaluation of the local seismic response in the L’Aquila-Coppito
plain (ORLANDO et alii, 2003), a geoelectrical survey was
conducted to investigate the electrical properties and geometries
of the Quaternary sedimentary cover in the area between the plain
NE border (m. Pettino) and an isolated outcrop of Meso-
Cenozoic limestones (colle dei Grilli).
The ERT geoelectrical tomographies using Wenner and
dipole-dipole arrays had a maximum depth of investigation of
100 m. The geoelectrical surveys showed a carbonatic bedrock
dipping toward the axis of the valley and allowed to characterize
the overlaying Quaternary sequence of the plain, detecting
alternating sedimentary layers with specific resistivity properties.
These surveys highlight the great complexity of the subsurface
structures of these basins.
ACKNOWLEDGEMENTS
The Authors wish to thank ENI E&P for the use of their
gravity data in the ISPRA Geophysical Database.
624
REFERENCES
BAGNAIA R., D’EPIFANIO A. & SYLOS LABINI S. (1989) - Aquila
and Subequan basins: an example of quaternary evolution in
central Apennines, Italy. Quatern. Nova, 2, 1-23.
BLUMETTI A.M., CAVINATO G.P. & TALLINI M. (1996) -
Evoluzione Plio – Quaternaria della Conca di Aquila -
Scoppito: Studio preliminare. Il Quaternario, 9 (1), 281-286.
BLUMETTI A.M., DI FILIPPO M., ZAFFIRO P., MARSAN P. & TORO
B. (2002) – Seismic hazard characterization of the city of
L’Aquila (Abruzzo, Central Italy): new data from geological,
morphotectonic and gravity prospecting analysis. In F.
Dramis, P. Farabollini and P. Molin (Eds) - Large-scale
vertical movements and related gravitational processes. Stud.
Geol. Camerti, Vol. Sp., Int. Workshop Camerino - Rome,
21-26 Giugno 1999, 7-18.
BOSI C. (1975) - Osservazioni preliminari su faglie
probabilmente attive nell’Appennino centrale. Boll. Soc.
Geol. It., 94, 827-859.
BOSI C. & BERTINI T. (1970) - Geologia della Media Valle
dell'Aterno. Mem. Soc. Geol. It., IX, 719-777.
FERRI F., PORFIDIA B., COREN F. & ZANOLLA C. (2007) - A new
gravity mapping project of Italy at 1:250000 scale. Epitome,
Geoitalia 2007, 2, 474-475.
FERRI F., ZANOLLA C., PORFIDIA B., COREN F. & CESI C. (2008):
Carta delle Anomalie di Bouguer dell’Italia e mari
circostanti, alla scala 1:1.000.000. Atti 28 th Convegno
GNGTS, 438-439.
GALADINI F., MESSINA P. & SPOSATO A. (2000) - Tettonica
quaternaria nell'Appennino centrale e caratterizzazione
dell'attività di faglie nel Pleistocene superiore-Olocene. In: F.
Galadini, C. Meletti and A. Rebez (Eds.) - Le ricerche del
GNDT nel campo della pericolosità sismica (1996-1999).
CNR - Gruppo Nazionale per la Difesa dai Terremoti, Roma,
181-192.
GRUPPO DI LAVORO CPTI (2004) - Catalogo Parametrico dei
Terremoti Italiani, versione 2004 (CPTI04).
http://www.ingv.it.
ISTITUTO NAZIONALE DI GEOFISICA E VULCANOLOGIA (2009) -
The L'Aquila seismic sequence - April 2009.
http://www.ingv.it.
ORLANDO L., BONCI L.,CALCATERRA S., DE NARDIS R., EULILLI
V., FERRI F., MARSAN P., MILANA G. & RAOLI F. (2003) -
Interpretazione integrata di dati geofisici per la valutazione
della risposta sismica dei sedimenti della conca L’Aquila-
Scoppito. Geoitalia 2003, 4° Forum FIST – Federazione
Italiana di Scienze della Terra, 554-555.

Key words: Active tectonic, L’Aquila 2009 earthquake,
Quaternary, tectonic-sedimentary evolution.
So far, the Quaternary geology of the L’Aquila region has
been the subject of few works, and hitherto no detailed studies
have been focused on the 2009 earthquake mesoseismic zone.
The main geomorphological features of this region are seen as
series of tectonic depressions located along the Aterno River
Valley (e.g., GALADINI &MESSINA, 2004). One of these basins
roughly matches with the 2009 epicentral area and includes, from
north-west to south-east, the surroundigs of Paganica, San
Gregorio, Poggio Picenze, Barisciano and San Demetrio ne’
Vestini villages.
New morphological, stratigraphic and tephrostratigraphic
investigations, integrated with previous studies in the southern
portion (BOSI &BERTINI, 1970; BERTINI &BOSI, 1993), allowed
us to recognise three main depositional cycles:
• A Lower (Early Pleistocene) fluvio-lacustrine cycle, which
includes from central to marginal basin environments: ca. 100
m of whitish carbonate lacustrine silts (San Nicandro Fm. of
BERTINI & BOSI, 1993); a powerful deltaic gravel-sand
complex (ca. 100 m thick), including lacustrine foreset (Valle
Orsa Fm.) and fluvial topset (Valle dell’Inferno Fm) deposits;
alluvial fan (Valle Valiano Fm.) and slope-derived limestone
breccias with characteristic pink-matrix (Fonte Vedice Fm.).
• An Upper (ca. 550-350 ka) fluvio-lacustrine cycle, completely
carved in the former, made up mainly by volcanic-rich siltysands,
and subordinately gravels (San Mauro Fm.).
• A Late (Upper Pleistocene) alluvial-fluvial cycle matching
with the Paganica alluvial fan and other minor comparable
systems.
The three depositional cycles are separated by erosional
surfaces and/or paleosols. In particular, a distinctive paleosol,
often stratigraphically associated with an idiosyncratic tephra
layer, occurs in-between the deposits of the Lower and the Upper
fluvio-lacustrine cycles.
_________________________
Tectonic and sedimentary evolution of the past 1 Myr in the
L’Aquila 2009 mesoseismic region, central Apennine
BIAGIO GIACCIO (*), PAOLO GALLI (**), PAOLO MESSINA (*), EMANUELA FALCUCCI (°), FABRIZIO GALADINI (°),
STEFANO GORI (°) & GIANCARLO SCARDIA (°)
(*) IGAG-CNR, Rome, biagio.giaccio@igag.cnr.it
(**) Dipartimento della Protezione Civile Nazionale,
paolo.galli@protezionevivile.it
(°) INGV-Sezione Milano, falcucci@mi.ingv.it
625
The chronological framework of the succession was provided
by previous and ongoing paleomagnetic measurements and new
tephrostratigraphic studies. More precisely, several
paleomagnetic measurements performed on different sediments of
the Lower fluvial-lacustrine cycle revealed an inverse polarity
(FABIO SPERANZA, personal communication) indicating an age
older than 780 ka. On the other hand, the fingerprinting of four
well-dated tephra layers (Tufo pisolitico di Trigoria, ca. 560 ka;
Pozzolane Rosse, ca. 460 ka, Tufo Rosso a Scorie Nere, ca. 450
ka; Tufo di Villa Senni ca. 360 ka), occurring within the
sediments of the Upper fluvio-lacustrine cycle, allow us to date
this latter between ca. 550 and 350 ka.
Some units of these three depositional cycles are associated to
well-preserved, terraced, depositional top surfaces. These
surfaces are displaced by a system of normal faults which are
composed by at least three, up to ca. 18 km-long, sub-parallel
WNW-ESE trending segments (here named eastern, central and
western faults). The westernmost one fits with the surface breaks
observed in the 2009 earthquake (e.g. FALCUCCI et alii, 2009).
This allowed us to evaluate the temporal-spatial evolution and the
style of the tectonic deformation for different time windows.
In the area between Barisciano and San Demetrio ne’ Vestini
the top depositional surface of the deltaic system of the Lower
fluvio-lacustrine cycle (Valle dell’Inferno and Valle Orsa Fms.) is
displaced by the complete system of three sub-parallel faults by
more than 400 m. This implicates a slip-rate > 0.4 mm/yr,
assuming for the top of the Lower cycles an approximate age of 1
Ma. On the contrary, northward, in the area of Poggio Picenze,
the deformation of this morpho-sedimentary unit is mostly
accommodated by a WNW-ESE trending flexure, dipping mainly
westward.
To the north, near the Paganica village, the tectonic
deformations are again mainly leaded by fault movements. Here,
along the easternmost fault, the top depositional surface of the
Upper fluvio-lacustrine cycle (450±100 ka) is displaced by ca. 80
m. Therefore, the slip rate for this fault segment is ca. 0.19±0.04
mm/yr (i.e. 80 m/450±100 kyr). A comparable slip rate can be
calculated for the central fault segment as well, across which the
same unit is displaced by ca. 70 m (0.17±0.03 m/yr). On the other
hand, the displacement of the bottom of this unit across all of the
three faults is of ca. 250 m, indicating a rate of 0.58±0.13 mm/yr
(i.e. 250 m/450±100 kyr), which is three times those calculated
for the easternmost and central segments.
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SESSIONE 18
On the whole, independently from the considered time
windows (~1 Ma vs. 500 ka), our investigations indicate that the
total slip rate across the fault system was consistently evaluable at
ca. 0.6-0.5 mm/yr. This study also indicates that during the past 1
Myr the tectonic deformation of the paleogeographic domains
was not uniform either in time, space or style. Indeed, whilst the
northern (Paganica) and southern (San Demetrio) sectors of the
basin were preferentially downthrown by brittle normal faulting,
the central part of the basin (Poggio Picenze) experienced a
gentle regional warping, without appreciable faulting.
As far as the timing is concerned, the easternmost fault
segments started the offset of Quaternary deposits early, at least
ca. 1 Ma, progressively transferring the throw to the central and
westernmost splays, where the most recent faulting traces,
including those related to the 2009 earthquake, indeed occurred.
REFERENCES
BERTINI T. & BOSI C. (1993) - La tettonica quaternaria della
conca di Fossa (L’Aquila). Il Quaternario, 6, 293-314.
BOSI C. & BERTINI T. (1970) - Geologia della media valle
dell’Aterno. Mem. Soc. Geol. It., 9, 719-777.
FALCUCCI E., GORI S., PERONACE E., FUBELLI G., MORO M.,
SAROLI M., GIACCIO B., MESSINA P., NASO G., SCARDIA G.,
SPOSATO A.,VOLTAGGIO M., GALLI P. & GALADINI F., (2009)
- The Paganica Fault and Surface Coseismic Ruptures
Caused by the 6 April 2009 Earthquake (L’Aquila, Central
Italy). Seismol. Res. Lett., 80, 940-950.
GALADINI F. & MESSINA P. (2004) - Early-middle Pleistocene
eastward migration of the Abruzzi Apennine (central Italy)
extensional domain. J. Geodyn., 37, 57-81.
626

Key words: Geomorphology, High Tiber Valley, landscape
evolution, neotectonic.
Landscape evolution in active tectonic areas is the result of
the interaction between bedrock uplift/subsidence, deposition,
compaction and erosion processes (ENGLAND &MOLNAR, 1990).
Bedrock uplift and deposition carry upward bedrock, on the
contrary subsidence, compaction and erosion reduce the mean
surface height. While compaction and deposition take place
mainly in sedimentary basins, bedrock uplift and denudation
show their action primarily on mountain landscape (BURBANK &
ANDERSON, 2000). In sedimentary basins, whose creation and
evolution are controlled mainly by tectonic events, all these
factors can be measured and compared in order to establish
where, when and how they affect the surface processes and the
resulting landscape. The main factors to consider are the
evolution time, the width of the target area (local versus regional
rates) and the rapidity of the response of morphogenetic
processes (inertia). To consider all these variables the
investigation methods, for the long term deformation, are
integrated with geologic and geomorphologic surveys in order to
identify and quantify the short term landscape response. In this
paper we propose the preliminary results about the mid-term
evolution of High Tiber Valley Quaternary basin, focusing about
geomorphological and geological evidences.
The High Tiber Valley is a continental basin elongated from
Sansepolcro in the north to Perugia to the south for 70 km and
bounded eastward by Umbrian Apennines and westward by the
Sub-Apennines ridges of the Tuscan domain (Fig. 1). The
Apennines are mountain chain, anticlines and narrow synclines,
due to a compressive phase (Miocene) with a NW-SE direction.
During a second extensional tectonic phase, that affected the area
in the Pleistocene with a general uplift, several intermountain
basins had been formed (including the High Tiber Valley) filled
_________________________
Morphotectonic evolution of High Tiber Valley (Umbria, Italy)
related to an active low angle normal fault segmentation
LAURA MELELLI (*), MASSIMILIANO BARCHI (*), FRANCESCO BROZZETTI (**), ANDREA LUPATTELLI (*),
FRANCESCO MIRABELLA (*), FAUSTO PAZZAGLIA (*), STEFANO PUCCI (°) & LAURA SACCUCCI (*)
(*) Dipartimento di Scienze della Terra, Università di Perugia,
lmelelli@unipg.it
(**) Dipartimento di Scienze della Terra, Università D’Annunzio, Chieti,
f.brozzetti@dst.unich.it
(°) Istituto Nazionale di Geofisica e Vulcanologia, Roma.
627
with fluvial lacustrine deposits and bounded by normal fault
systems. The High Tiber Valley geometry and evolution is
controlled by an extensional fault system driven by the
Altotiberina normal fault (ATF) in the Northern Apennines. The
fault is a low-angle (average dip about 17°) NE-dipping structure
active since the lower Quaternary (BARCHI et alii, 1998; BONCIO
et alii, 2000). On the basis of the along strike long-term offset
distribution, a continuous structure extending for at least 60 km is
recognized like the regional detachment for several smaller
synthetic and antithetic splays, the youngest of which border the
Quaternary Tiber valley.
The present day landscape is the sum of many factors on
several temporal scales: a regional uplift in order of 0.5 mm/yr
affecting all the Apennine chain, climatic change and eustatic sea
level variations. Time scales deformations are almost three: a first
compressive phase dating back to about 3 million years ago
responsible for creating the Apennines, a normal faulting phase
that affected the area since Pleistocene and a subsequent
Holocene fluvial response since 0.1 Ma. The investigation
methods are: microseismic surveys, geodetic data, field work and
aerial photo interpretation in order to identify the
geomorphological markers of neotectonic activity. The results are
input in a GIS project to collect a GeoDB comparable with
different terrain data. From geologic survey three principal
depositional cycles are identified: i) the first one (early
Pleistocene) with prevalent clay sedimentation; ii) the second one
(early-middle Pleistocene) with prevalent conglomeratic
sediments and sandy interbodies; iii) the last one (middle-late
Pleistocene and Holocene) with heterogenic deposits, only in
narrow areas. The Quaternary deposits are displaced by several
fault segments related to the activity of the basin-bounding faults.
On the basis of the oldest ages of the quaternary deposits
cropping out within the basins it is possible to infer that the faults
have been active at least since lower Quaternary (1.8 Ma).
However, the great thickness of the basins infill (1.000 m)
may suggest that within the basins depocenter in the subsurface,
older deposits might be present and the faults have been active
since a longer time period. The paper is focused on drainage
network response in order to establish possible variations in
activity of Quaternary ATF splays that shaped the basin. The
differences, on the basis of the topographic sections and on the
positions of the terraces are related to local subsidence and
SESSIONE 18

SESSIONE 18
Fig. 1 – The study area and the division in the three sub-basins (on the right) and the related local subsidence and regional uplift (on the left).
regional uplift. We interpret the along strike changes of Tiber
river incision marked by the different presence/absence and
distribution of the river terraces as the result of the interference
between the regional uplift and the local extensional tectonics.
According to this approach the target area can be divided into
three thresholds-separated coalescing basins (early Pleistocene in
age), the Sansepolcro, the Umbertide and the Ponte Pattoli subbasins
(Fig. 1). Sansepolcro sub-basin is the widest part and it is
characterized by the overall absence of fluvial terraces. Previous
studies highlighted that it is located at the foot-wall of one of the
basin-bounding ATF splays (CATTUTO et alii, 1995) with a low
or absent incision of the river. Due to this fact, the northwestern
San Sepolcro sub-basin appears to be dominated by local
subsidence. South of the Sansepolcro sub-basin threshold, in the
Umbertide one, two orders of well-recognizable fluvial terraces
which rest on top of the quaternary deposits are recognized. The
distribution and elevation changes of these surfaces are not the
same all along the valley and marks several difference in local
incision by the river. This part is characterized by a decrease of
incision in the central part and by higher incision towards the
threshold. On the other hand the southeastern Umbertide subbasin
is characterized by incision and suggest that uplift
dominates on the foot-wall subsidence and promotes river
incision. Within the southeastern Ponte Pattoli sub-basin a
progressive decrease of incision is recognizable. These
differences are also reflected by the distribution of the historical
seismicity which displays many events in the northwestern
628
Sansepolcro area and is silent in the Umbertide area, suggesting a
continuity in the faults activity in the last 1.8 MA. Such setting
suggests that the present-day fluvial incision depicts a continuity
in the tectonic processes through time, in that the same faults
responsible for the formation of the quaternary basins are still
active but also that faults activity seems to be faster in the
northwestern area than in the southeastern one
REFERENCES
BARCHI M., DE FEYTER A., MAGNANI M., MINELLI G., PIALLI G. &
SOTERA B. (1998) - Extensional tectonics in the Northern
Apennines (Italy): evidence from the CROP03 deep seismic
reflection line. Mem. Soc. Geol. It., 52, 528-538.
BONCIO P., BROZZETTI F. & LAVECCHIA G. (2000) - Architecture and
seismotectonics of a regional Low-Angle Normal Fault Zone in
Central Italy. Tectonics, 19, 1038-1055.
BURBANK D. & ANDERSON R. (2000) – Tectonic Geomorphology.
Wiley-Blackwell, 288 pp.
CATTUTO C., CENCETTI C., FISAULI M. & GREGORI L. (1995) -I bacini
pleistocenici di Anghiari e Sansepolcro nell'alta valle del Tevere.
Il Quaternario, 8, 119-128.
ENGLAND P. & MOLNAR P.A. (1990) - Surface uplift, uplift of rocks,
and exhumation of rocks. Geology, 18 (12), 1173-1177.

Quaternary lacustrine sedimentation in the Sant’Arcangelo Basin
(Southern Apennines)
Key words: Quaternary, San Lorenzo lacustrine succession,
Sant’Arcangelo Basin, southern Italy.
Quaternary lacustrine sedimentation (Fig. 1) represents one of
the more recent steps in the evolution of the northern part of the
Sant'Arcangelo Basin, that is one of the wider and deeper
Pliocene to Pleistocene satellite basins of southern Apennines
(Italy) (PIERI et alii, 1994; 1996) (Fig. 2 and 3).
The lower to middle Pleistocene lacustrine deposits (San
Fig. 1 – Quaternary lacustrine deposits. San Lorenzo succession.
LUISA SABATO (*), MARCELLO TROPEANO (*) & VINCENZO ONOFRIO (*)
Fig. 2 – Geological features of the Sant'Arcangelo Basin (after SABATO, 2000).
_________________________
(*) Dipartimento di Geologia e Geofisica, Università "Aldo Moro" di Bari,
l.sabato@geo.uniba.it
629
Lorenzo succession), up to 200 m thick, are composed of
siltstone and claystone interbedded with sandstone, carbonate and
volcaniclastic beds, mainly arranged in fining-upward sequences
(SABATO, 1997; 2000; SABATO et alii, 2005) (Fig. 1). The overall
stratigraphical, sedimentological, and structural data collected
demonstrate that the lacustrine deposits formed when the northern
sector of the Sant'Arcangelo Basin was undergoing tectonic
deformation. In fact, it is possible to observe evidence of
syntectonic sedimentation, from small soft-sediment deformation
structures, induced either by earthquakes or by instability of lake
margin slope deposits (MORETTI &SABATO, 2007), to basinscale
tectonic growth structures, forming endorheic areas for lake
development (Fig. 4). In particular, the main tectonic structures
observed in the field are faults and folds that may be related to a
left-lateral transpressive regime (ONOFRIO, 2008).
Furthermore, the inferred age of tectonic structures derived
from the ages of the syntectonic deposits suggests that the
transpressive regime was active in the area at least from the early
Pleistocene (ONOFRIO et alii, 2009) (Fig. 4).
Integrated stratigraphical and structural analyses of
Quaternary continental deposits, which here basically record the
end of the sedimentary infilling of a Plio-Pleistocene satellite
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SESSIONE 18
basin along the Apennines fold-thrust belt, are necessary in order
to constrain the more recent tectonics in this still active chain.
Fig. 3 – Main structural features of the Sant'Arcangelo Basin and surroundings.
Note the position of the "San Lorenzo" lacustrine succession (after ONOFRIO,
2008).
REFERENCES
ONOFRIO V. (2008) - Evoluzione tettono-stratigrafica del settore
settentrionale del Bacino di Sant'Arcangelo nel Plio-
Pleistocene (Appennino meridionale). PhD Thesis, Bari
University, Italy, 119 pp.
ONOFRIO V., TROPEANO M., FESTA V., MORETTI M. & SABATO L.
(2009) - Quaternary transpression and the San Lorenzo
lacustrine sedimentation in the Sant’Arcangelo Basin.
Sediment. Geol., 222, 78-88.
PIERI P., SABATO L., LOIACONO F. & MARINO M. (1994) - Il
bacino di piggyback di Sant'Arcangelo: evoluzione tettonicosedimentaria.
Boll. Soc. Geol. It. 113, 468–481.
PIERI P., SABATO,L.&MARINO M. (1996) - The Plio-Pleistocene
piggyback Sant'Arcangelo Basin: tectonic and sedimentary
evolution. Notes Mem. Serv. Geol. Maroc, 387, 195–208.
SABATO L. (1997) - Sedimentary and tectonic evolution of a
lower-middle Pleistocene lacustrine system in the
Sant'Arcangelo piggyback basin (southern Italy). Geol. Rom.,
33, 137–145.
SABATO L. (2000) - A lower-middle Pleistocene lacustrine system
in late evolutionary stages of the Sant'Arcangelo Basin
(southern Italy). In: E.H. Gierlowski-Kordesch and K. Kelts
(Eds.) - Lake Basins Through Space and Time. AAPG Stud.
Geol., 46, 543–552.
630
SABATO L., BERTINI A., MASINI F., ALBIANELLI A., NAPOLEONE
G. & PIERI P. (2005) - The lower and middle Pleistocene
geological record of the San Lorenzo lacustrine succession in
the Sant'Arcangelo Basin (Southern Apennines, Italy).
Quatern. Int., 131, 59–69.
Fig. 4 – Block diagrams showing the stratigraphycal development of the
northern part of the Sant'Arcangelo Basin from early to middle
Pleistocene due to left-lateral transpressional tectonics. The activity of
this system of faults allowed the formation of the San Lorenzo
lacustrine system. (after ONOFRIO et alii, 2009).

SESSIONE 19
I vulcani attivi della Campania
CONVENERS
Roberto Santacroce (Università di Pisa)
Alessandro Sbrana (Università di Pisa)
Paola Marianelli (Università di Pisa)
631
SESSIONE 19

SESSIONE 19
Key words: Magnetics, Naples Bay, reflection seismics, Torre del
Greco, Vesuvius, volcanic structure.
INTRODUCTION
The integrated geologic interpretation of densely spaced
multichannel seismic and magnetic profiles, acquired on the
continental shelf adjacent to the Vesuvius volcanic edifice has
allowed to carry out a three-dimensional magneto-seismic
reconstruction of a wide volcanic structure. The structure has
been individuated offshore the town of Torre del Greco (Naples)
and represents the seaward prolongation of the volcanic edifice.
The complex Late-Quaternary archictecture of the Naples Bay
is controlled by the interactions between volcanic and
sedimentary processes. Rapid lateral variations between
acoustically-transparent seismic units frequently occur on
reflection profiles. These units correspond to volcanic deposits
erupted during the multiphase activity of the Phlegrean Fields,
Somma-Vesuvius and Ischia and Procida volcanic complexes
(AIELLO et alii, 2004; 2005; 2009; MILIA et alii, 1998; 2008;
D’ARGENIO et alii, 2004; RUGGIERI et alii, 2007). In the study
area the magnetic properties allow to confirm the volcanic nature
of the geologic units identified through the reflection seismics. A
semi-quantitative interpretation of seismic and bathymetric data,
resulting in a topographic and seismic reconstruction of the
submerged volcanic structure off Torre del Greco is here
presented.
GEO-VOLCANOLOGIC SETTING
The Vesuvius volcano has been intensively studied, mainly
regarding its eruptive events, the recent seismicity, the
geochemistry, the ground movements and the related geologic
hazard (CASSANO &LA TORRE, 1987; SANTACROCE et alii, 1987;
CASTELLANO et alii, 2002; ESPOSTI ONGARO et alii, 2002;
MASTROLORENZO et alii, 2002; SACCOROTTI et alii, 2002;
_________________________
Three-dimensional magnetic and seismic reconstruction of the
“Torre del Greco” volcanic structure (Vesuvius, Naples Bay)
(*) Istituto per l’Ambiente Marino Costiero (IAMC), CNR, Napoli,
gemma.aiello@iamc.cnr.it
GEMMA AIELLO (*), ENNIO MARSELLA (*) & STEFANO RUGGIERI (*)
632
SCARPA et alii, 2002; TODESCO et alii, 2002).
The eruption of the pyroclastic flux deposits of the
“Campanian Ignimbrite”(37 ky B.P.; ROSI &SBRANA, 1987) has
covered the whole Campania Region and part of the adjacent
offshore with thick deposits of grey tuffs, over which the Mt.
Somma volcanic edifice started to grow. The eruptive activity is
comprised between the main eruptions of the “Pomici di Base”
(18 ky) and of the “Pomici Verdoline”, triggering the collapse of
the Somma edifice and the consequent calderization, with the
formation of a new volcanic edifice, i.e. the Vesuvius (SHERIDAN
et alii, 1981; 1982; SIGURDSSON et alii, 1982; SANTACROCE et
alii, 1987).
INTEGRATED INTERPRETATION OF THE
GEOPHYSICAL DATA AND THREE-DIMENSIONAL
RECONSTRUCTION
The integrated interpretation of the magnetic, seismic and
bathymetric data suggests the correlation of the magnetic
anomalies with three main peaks of a wide volcanic structure,
located offshore of the Torre del Greco town, along a NNW-SSE
direction, at water depths ranging between – 80 m and – 110 m.
The seismo-stratigraphic evidences are represented by
acoustically-transparent seismic facies and high contrasts of
acoustic impedance, relatively to those ones of the overlying
deposits, mounded depositional geometries and average
kilometric dimensions. The base of the volcanic bodies is not
acoustically evident, because they overlie a seismic unit
correlated with the pyroclastic fluxes of the “Campanian
Ignimbrite”. The top of the structures, irregularly eroded, may
show several culminations, as it happens in the case of the Torre
del Greco volcanic structure. The thickness of the overlying
Holocene deposits is significantly reduced in correspondence to
the volcanic structures, while other mounds have been fossilised
by Late Pleistocene-Holocene sediments.
The three-dimensional reconstruction of the Torre del Greco
structure has been carried out by using the constraints of the
reflection seismics and the correlation of the volcanic structure to
bathymetry. The bathymetric data have been processed with the
application of a median filter to remove the sea bottom
irregularities with a smoothing of the sea bottom topographic
surface. In the three-dimensional reconstruction (Fig. 1) the sea
bottom topography has been compared to the top of the Torre del

Greco structure, represented by the contour depth of the
corresponding seismic horizons. A good correspondence between
the sea bottom topographic surface and the top of the volcanic
structure, which does not crop out at the sea bottom, exists. The
uprising of the volcanic structure is testified by the occurrence of
topographic undulations of the sea bottom in the order of ten
meters. This is confirmed by the interpretation of seismic
profiles, showing three main culminations of the volcanic
structure, where the overlying sedimentary drape is significantly
reduced. These culminations are related to the peaks of magnetic
anomaly, with values in the order of 250-350 nT. A striking
coincidence between the elongated topographic high of the sea
bottom (towards east) and the high in the top of the underlying
volcanic structure may be explained as a consequence of the sea
bottom deformation due to the overlying volcanic culminations.
Fig. 1 – 3D magneto-seismic reconstruction of the volcanic structure.
REFERENCES
AIELLO G., ANGELINO A., MARSELLA E., RUGGIERI S. &
SINISCALCHI A. (2004) – Carta magnetica di alta risoluzione
del Golfo di Napoli (Tirreno meridionale). Boll. Soc. Geol.
Ital., 123, 333-342.
AIELLO G., ANGELINO A., D’ARGENIO B., MARSELLA E., PELOSI
N., RUGGIERI S. & SINISCALCHI A. (2005) – Buried volcanic
structures in the Gulf of Naples (southern Tyrrhenian sea,
Italy) resulting from high resolution magnetic survey and
seismic profiling. Annals of Geophysics, 48, 1-15.
AIELLO G., MARSELLA E. & PASSARO S. (2009) – Submarine
instability processes on the continental slopes off the
Campania region: the case history of Ischia island (Naples
Bay). Boll. Geof. Teor. Appl., 50 (2), 193-207.
CASSANO E. & LA TORRE P. (1987) – Geophysics. Quaderni De
La Ricerca Scientifica, CNR.
633
CASTELLANO M., BUONOCUNTO C., CAPELLO M. & LA ROCCA M.
(2002) – Seismic surveillance of active volcanoes: the
Osservatorio Vesuviano seismic network (OVSN – Southern
Italy). Seism. Res. Letters, 73, 177-184.
D’ARGENIO B., AIELLO G. et alii (2004) – Digital Elevation
Model of the Naples Bay and adjacent areas, Eastern
Tyrrhenian sea. In: G. Groppelli (Ed.) – Mapping Geology in
Italy. Editore De Agostini.
ESPOSTI ONGARO T., NERI A., TODESCO M. & MACEDONIO G.
(2002) – Pyroclastic flow hazard at Vesuvius from numerical
modelling II. Analysis of local flow variables. Bull. of
Volcanol., 64, 178-191.
FINETTI I. & MORELLI C. (1973) – Esplorazione sismica per
riflessione dei Golfi di Napoli e Pozzuoli. Boll. Geof. Teor.
Appl., 16, 175-222.
MASTROLORENZO G., PALLADINO D., VECCHIO G. & TADDEUCCI
J. (2002) – The 472 AD Pollena eruption at Somma-Vesuvius
(Italy) and its environmental impact at the end of Roman
Empire. J. Volcanol. Geotherm. Res., 113, 19-36.
MILIA A., MIRABILE L., TORRENTE M.M. & DVORAK J.J. (1998) –
Volcanism offshore of Vesuvius volcano (Italy): implications
for hazard evaluation. Bull. of Volcanol., 59, 404-413.
MILIA A., MOLISSO F., RASPINI A., SACCHI M. & TORRENTE M.M.
(2008) – Syneruptive features and sedimentary processes
associated with pyroclastic currents entering the sea: the AD
79 eruption of Vesuvius, Bay of Naples, Italy. J. Geol. Soc.,
165 (4), 839-848.
RUGGIERI S., AIELLO G. & MARSELLA E. (2007) – Integrated
marine geophysical data interpretation of the Naples Bay
continental slope. Boll. Geof. Teor. Appl., 48 (1), 1-24.
SACCOROTTI G., VENTURA G. & VILARDO G. (2002) – Seismic
swarms related to diffusive processes: the case of Somma-
Vesuvius volcano, Italy. Geophysics, 67, 199-203.
SANTACROCE R. (1987) – Somma-Vesuvius. Quaderni De La
Ricerca Scientifica, CNR, Roma.
SCARPA R., TRONCA F., BIANCO F. & DEL PEZZO E. (2002) –
High resolution velocity structure beneath Mount Vesuvius
from seismic array data. Geophys. Res. Lett., 29, 2040.
SHERIDAN M.F., BARBERI F., ROSI M. & SANTACROCE R. (1981)
– A model for Plinian eruptions of Vesuvius. Nature, 289,
282-285.
SIGURDSSON H., CASHDOLLAR S. & SPARKS S.R.J. (1982) – The
eruption of Vesuvius in AD 79: reconstruction from
historical and volcanological evidence. Am. Journ. of
Archaeology, 86, 39-51.
SESSIONE 19

SESSIONE 19
Key words: Andisols, Artemisio volcano, lithologic substrate.
Here are presented the results of a study carried out on the
southern slope of Mount Artemisio (i.e.Volcano), with the aim to
put on evidence the pedologic variability and the evolutionary
tendency of soils on volcanic substrates which crop out in this
area.
The different soil profiles have been analysed at different
altitudes, starting from the base of the slope (about 600 m a.s.l.),
up to the top (about 980 m a.s.l.), on different types of vulcanite
(“Tufo Marrone dell’Artemisio”, “lapilli varicolori”, cinder).
Soils have been described on the field, sampled by pedologic
horizons, and then tested through chemical and phisycal analysis.
From the elaboration of these data comes out that all soils that
have been studied are part of the “Andisols” order (according to
“USDA” taxonomy): a soil developing in volcanic ejecta (such as
volcanic ash, pumice, cinders and lava) and in volcaniclastic
materials, the colloidal fraction of which is dominated by shortrange-order
minerals or alluminium-humus complexes.
The dominant processes in Andisols are weathering and
mineral transformation. Weathering of primary alumina-silicates
and amorphous minerals (mainly volcanic glasses, which go
through a slow alteration) has proceeded only to the point of
formation of short-range-order minerals, such as allophane,
imogolite and ferrihydrite, as pointed up from some specific
analysis (pH in NaF, Phosphate retention, etc).
The main characteristics typical of Andisols have been found
not only in soils that lay down on pyroclastities, that is substrates
easily alterable and rich in primary volcanic glass; even
unexpectedly in soils that lay down on lithotype excessively
drainy, as slags, or scarcely vitreous as lapilli, which generally,
through the alteration process become clay.
This fact suggests a probable subsequent contribution of
thinly splitted materials, rich in volcanic glass, which have
covered the internal slopes of Mount Artemisio during the
subsequent cycles of activity of the volcano.
Furthermore, we have to consider the important role carried
_________________________
Pedologic variability of soils on volcanic substrates:
the case of Mount Artemisio
(*) ISPRA (Istituto Superiore per la Protezione e la Ricerca Ambientale),
Roma, riccardo.boschetto@isprambiente.it.
(**) Dipartimento di Biologia Vegetale, Università la Sapienza di Roma.
RICCARDO G. BOSCHETTO (*) & MONICA ZANINI (**)
634
out by a constantly humid climate and by a rich plant cover, in
creating an optimum environment for the genesis and
conservation of the allophanic clays: these minerals, typical of
Andisols, in these particular conditions, achieve a stability that
allows them to persist with a very slow alteration over long
periods.

Key words: Ischia harbour, Ischia history, Bourbon Ferdinand
II, Lago del Bagno, crater lake.
We examine recent and historical sources with a view to
reconstructing the circumstances leading in 1854 to the opening
of the natural harbour of Ischia, the execution phases of the works
and the morphological changes arising. Since the late 17th
century Ischia, an active volcanic island, has been a major
European destination for spa treatment. It underwent a period of
change after the harbour was opened up, which represented not
only an outlet towards the mainland but also an important factor
of social and cultural aggregation for the island. Our analysis also
accounts of the geology of Ischia Harbour, the observations of the
current state of the island and issues concerning the increase in
volcanic and seismic risk resulting from urban expansion and the
increase in tourism since the first half of the 20th century.
On 17 September 1854, under the initiative of the Bourbon
Ferdinand II (1830-1859), King of the Two Sicilies, the opening
of the new harbour of Ischia was celebrated. It has since become
a major maritime port and marina in the Bay of Naples. The port
constituted the fundamental element connecting the island and the
mainland, providing easier access to the island and promoting the
progressive growth of the local economy.
The future harbour area, a lacustrine basin (Fig.1), just like
the rest of the island, was the product of volcanic activity which
has been distinguished by alternating explosive and effusive
eruptions. Small to moderate volcanic eruptions occurred in the
last 10,000 years, and also intense seismic activity in the past 800
years. The most recent eruption occurred in 1302, with lava flow
affected partly the east area of the harbour (VEZZOLI 1988;
VEZZOLI et alii, 2009; CARLINO et alii, 2006, 2010). The crater of
Ischia Harbour was formed several centuries BC. The volcanic
products in the eastern sector (San Pietro Hill) overlie a palaeosol
developed on top of an older trachyte containing pottery remains
from the 5th century BC and roof tiles of the 6th-5th centuries BC
(BUCHNER, 1986; VEZZOLI et alii, 2009) The Ischia Harbour
crater was formed by a phreatomagmatic eruption, during which
_________________________
The opening of the natural harbour of Ischia (Italy)
STEFANO CARLINO (*), ELENA CUBELLIS (*), ILIA DELIZIA (**) & GIUSEPPE LUONGO (°)
(*) Istituto Nazionale di Geofisica e Vulcanologia – Sezione di Napoli
Osservatorio Vesuviano, stefano.carlino@ov.ingv.it
(**) Dipartimento di Storia e Restauro, Università di Napoli “Federico II”,
ilia.delizia@unina.it
(°) Dipartimento di Scienze della Terra, Università di Napoli “ Federico II”,
giuseppe.luongo@unina.it
635
the explosive energy increased, followed by a magmatic phase
with a strombolian activity. A small positive gravity Bouguer
anomaly, close to the harbour, highlights the presence of a
shallow dense mass which can be interpreted as due to the
solidified lava lake formed during the last phase of the eruption.
This interpretation is supported by the presence of a rock block
emerging from the lake surface (CARLINO et alii., 2010).
Fig.1 - Topographic map of the Royal Topographic Office of Naples, scale
1:25,000, 1840 (IGMI source), with the crater Lago del Bagno: the future
harbour. On the western sector of the lake (sea side) the little channel for water
circulation. The lake was thus an ideal place for fishing, for the farming of
molluscs and crustaceans, but also for the hunting of coot and other waterfowl.
The works for the harbour opening involved the removal of
part of the sandbank separating the lake from the sea to the north,
with an entrance of about 500 palms (130 m). A jetty was also to
be constructed to protect the harbour mouth from the strong
NNW winter winds, about 700 palms long (182 m) consisting of
about 541 cubic canne (10,000 m 3 ) of rock obtained from a cliff
beyond the small river mouth to the west, and the bed was to be
dredged to allow access for large vessels as well (QUARANTA,
1855). The whole lake-bed was excavated, removing material
about one metre deep, amounting to 115,000 m 3
The opening of Ischia Harbour in 1854 was undoubtedly an
intervention which radically changed the hierarchical relations
between the island and the mainland. It is also a fine example of
the art of 19th-century engineering (DELIZIA, 1990; RISPOLI
2007). It was an operation which, in terms of techniques and
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SESSIONE 19
execution times, was certainly ahead of its time. Although the
reasons that drove King Ferdinand II to open up the pre-existing
Bagno Lake, to make it the island’s main port, were chiefly
personal, what lay behind the choice was the spirit of renewal in
regional policies, which was one of the hallmarks of the Bourbon
government. At that time the island was already well known for
treatments with its thermal waters, especially in Casamicciola,
where since the late 16th century many visitors had gone to enjoy
their therapeutic effects. However, the lack of safe harbours
throughout the island made access difficult, especially in winter
months when the frequency of sea storms increases considerably.
With the opening-up of Ischia Harbour, the situation radically
changed: maritime traffic and the flow of visitors shifted towards
the eastern side of the island which thus became easily accessible,
also for large steamships (Fig. 2). This produced a population
increase in the Ischia municipality, rather than elsewhere on the
island, and lead to new urban settlements.
Fig.2 - The Ischia harbour today.
The natural features of the harbour, obtained from an ancient
crater lake, are certainly singular. However, its so well-defined
shape has prevented its expansion (RISPOLI, 2007), which would
seem necessary to handle the substantial increase in maritime
traffic. During the peak tourist season, over 20 large vessels dock
and sail daily, handling about 15,000 passengers, and over 35 fast
craft handling 8,000 passengers, making a total flow of 23,000
passengers per day. It is some surprise that, in 1853, the
Provincial Council of Naples failed to approve the construction
of the new harbour of Ischia, which it considered a site
“unsusceptible to development”. Clearly, for such areas endowed
with natural, landscape and cultural attractions, interventions
resulting in better accessibility and fruition produce not only an
increase in tourist flows, but also in the resident population.
Moreover, as the economy’s organisational centre, the harbour
brings about the transition from settlement of coastal areas to that
of more inland areas. The trade taking place in the marketharbour
promotes a deep-rooted reconversion of production, from
a closed, self-consumption economy to a trade economy. In this
636
sense, Ischia harbour represented not only a window looking to
the mainland but also a key factor in the island’s social and
cultural aggregation.
Although in recent times our knowledge of the island’s
geological phenomena has improved, and special attention has
been laid on the effects of their most intense manifestations and
related risks, regrettably among the unwary communities exposed
to environmental risk few people have adopted the culture of
preventive action. In light of this fact, the level of attention to
extreme geological phenomena apparently only grows in
concomitance with catastrophic events, while political decisionmakers
limit themselves to intervening only in the emergency
phase, without any long-term programming of responsible landuse
management policies to ensure the future reduction of
geological risk.
REFERENCES
BUCHNER G. (1986) - Eruzioni vulcaniche e fenomeni vulcanotettonici
di età preistorica e storica nell’isola d’Ischia. Bibl.
de l’Institut Francais de Naples, Deuxième serie, Vol. VII.
Pubbl. du Centre Jean Berard, Naples, 145-188.
CARLINO S., CUBELLIS E., DELIZIA I. & LUONGO G. (2010) -
History of Ischia harbour (Southern Italy). In: V. Viorel
Badescu and R. B. Cathcart (Eds) - Macro-engineering
Seawater in/and Unique Environments. Arid Lowlands and
Water Bodies Rehabilitation. Springer Verlag (in press).
CARLINO S., CUBELLIS E., LUONGO G. & OBRIZZO F. (2006) - On
the mechanics of caldera resurgence of Ischia Island. In: C.
Troise, G. De Natale and C:R.J. Kilburn (Eds). Geol. Society,
London, Spec. Publ., 269, 181–193.
DELIZIA I. (1990) - Ischia d’altri tempi. Electa Napoli.
QUARANTA B. (1855) - Del nuovo porto d’Ischia aperto per
comando di Sua Maestà Ferdinando II re del Regno delle
Due Sicilie. Annali Civili, 13-17.
RISPOLI F. (2007) - Oltre il Sagrato. In : AA.VV. -Santa Maria di
Porto Salvo a Ischia 150/75. Tota Tua 75/150.
VEZZOLI L., PRINCIPE C., MALFATTI J., ARRIGHI S., TANGUY J.C.
& LE GOFF M. (2009) - Modes and times of caldera
resurgence: the

Factors controlling volcano-dynamic of large calderas: the example
of Campi Flegrei (Southern Italy)
Key words: Caldera eruption, Campi Flegrei caldera, elastic
regime, magma storage, viscous regime, yield strength, wallrock
viscosity.
A semi-quantitative evaluation of the different factors that
lead to magma storage or to its eruption in large calderas (such as
magma chamber size, wall-rock viscosity, temperature, and
regional tectonic strain rate) is reported here for elastic and
viscoelastic conditions. This study considers different scenarios
of shallow crustal behaviour, with application to Campi Flegrei
caldera (CFc), an area characterised by very high volcanic risk,
and the recurrent unrests period. The constrain of our
computation are provided by the earlier studies of CFc ground
deformation and caldera eruptions, including recent geophysical
investigations of the area. Considering the large magmatic
sources of the CFc ignimbrite eruptions (400–2,000 km 3 ) and a
wall-rock viscosity between 10 18 and 10 20 Pa s, the conditions for
eruptive failure are difficult to attain. Smaller source dimensions
(a few cubic kilometres) promote the condition for fracture
(eruption) rather than for the flow of wall rock. We also analyse
the influence of the regional extensional stress regime on magma
storage and eruptions, and the thermal stress as a possible source
of caldera uplift. The present study also emphasises the difficulty
of distinguishing eruption and non-eruption scenarios at CFc,
since an unambiguous model that accounts for the rock rheology,
magma-source dimensions and locations and regional stress field
influences is still lacking.
RESULTS
By considering previous CFc unrest models and caldera
eruptions, we have evaluated the strength of the rock for elastoplastic
behaviour and the conditions for eruption or magma
storage for both shallow and deep magmatic sources at CFc for
the viscoelastic case. When the elastoplastic conditions for the
1982–1984 uplift are considered, relative low yield strengths are
obtained (0.5–10 MPa). These values will be related to the
particular physical state of the crust below CFc, which is
_________________________
(*) Istituto Nazionale di Geofisica e Vulcanologia, Sezione di Napoli,
Osservatorio Vesuviano, stefano.carlino@ov.ingv.it
STEFANO CARLINO (*) & RENATO SOMMA (*)
637
characterised by high temperatures, intense fracturing, and
circulation of hot fluids. This allows the shallow rock to enter the
plastic domain if it is subjected to low increases in the stress.
Thus, large deformation can be expected also without eruption.
We have also considered the case of wall-rock behaviour around
a magmatic source by using the viscoelastic model obtained by
JELLINEK &DEPAOLO (2003).
This model considers two different behaviours, elastic and
viscous, and takes into account the viscosity of the wall rock, the
volume of the source and the overpressure generated by the
magma influx. Considering a magmatic source for CFc of at least
450 km 3 (WOHLETZ et alii, 1999) and a wall-rock viscosity from
10 18 –10 20 Pa s, it is difficult to attain the conditions for eruptive
failure. These conditions are further inhibited for larger magmatic
sources (2,000 km 3 ; the CI magma chamber). Since a reliable
value of wall-rock viscosity for CFc is around 1×10 19 Pa s (DE
NATALE et alii, 1991), the likelihood of eruptions for such a large
magma chamber need to be correlated with other variables, such
as, source dimension, regional stress field, and high rates of
magma influx. Considering the rheology of the rock around an
overpressurised shallower and smaller source (of about 1 km
radius; DE NATALE et alii, 2001, BATTAGLIA et al. 2006;
AMORUSO et alii, 2008), we have shown that the elastic regime of
the wall rock dominates for all of the values of viscosity (10 18 –10 20
Pa s). At CFc, this condition might have triggered eruptions, as
for instance, during the last 1970–72 and 1982–84 unrests,
whereas their present absence might be ascribed to different
factors, such as a lesser viscosity of the wall rock due to its higher
temperatures (viscous regime) or the lack of magma intrusion
according to the hypothesis of fluid migration as the source of
ground uplift.
In general, the above considerations show that the conditions
that would favour eruptions are the high viscosity of the rock
around the magmatic source and the small dimension of the
source itself. These circumstances would promote the fracturing
of the wall rock and dyke injection towards the surface. In
contrast, higher temperatures and lower viscosities of the wall
rock would inhibit the propagation of magma up to the surface;
these conditions occur for larger magma chambers (hundreds of
cubic kilometres). In addition, the extensional regime of the CFc
area would promote a rising of magma from deeper sources and a
decrease in the chamber pressure along the plane perpendicular to
the extensional direction. This overpressure within the chamber
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SESSIONE 19
can occur when the magma influx rate is sufficiently high to
overcome the negative pressure due to the extensional rate.
Finally, an alternative efficient mechanism for the periodic
inflation and deflation of CFc without eruptions can be seen as
the pore pressure increases due to thermal variations within the
deep magmatic source (thermal stress; DE NATALE et alii, 2001).
We show that temperature variations of more than 35°C within a
deep magmatic source can produce the thermal stress that is
sufficient for the uplift of the caldera. This process probably
occurs in the plastic or viscous domain and might involve the
circulation of geothermal fluids.
The present study has emphasized the difficulty of
understanding how to discriminate between the conditions for
eruption or non-eruption at CFc. For instance, the seismic,
deformation and gravity monitoring data provide the more
important evidence for volcanic activity renewal, but their
interpretation is complicated by the non-uniqueness of the
solutions that generate the CFc unrest. Otherwise, the reactivation
of volcanic activity of large calderas might take place without
Fig. 1 – Maximum magmatic source overpressure (? pmax) generated by a
steady magma influx Q = 0.002 km 3 y -1 as a function of the spherical source,
with different volumes (V) and a constant viscosity of the wall rock (μwr).
The viscosity ranges between 1×10 18 and 1× 10 20 Pa s. The more reliable
values of the viscosity for CFc are around 1×10 19 Pa s (DE NATALE et alii,
1991). The horizontal solid line represents the probable value of the yield
strength (ys) of the CFc rock above which fracturing occurs. If ? pmax > ys the
source is roughly in an elastic regime, and fracturing and magma injection
can lead to volcanic eruption. When ? pmax < ys, the wall rocks are
approximately in a viscous regime, which favours melt storage and growth of
the magma chamber (JELLINEK &DEPAOLO, 2003). The reported minimum
and maximum volumes represent the NYT and CI chamber volumes,
respectively. Dashed line: the influence of magma buoyancy on overpressure
for a density contrast of 100 kg m -3 .
638
clear precursors, as occurred during the 1994 Rabaul caldera
eruption (MCKEE et alii, 1995; DE NATALE et alii, 2001). Under
other conditions, no eruption would happen, even after long
periods of seismic activity and large deformation of the caldera,
as in the case of the 1970–1972 and 1982–1984 CFc unrest. The
complexity of the problem is related to an understanding of the
particular physical state of the crust and particularly to the
location and dimension of the magma reservoir, the rheology
around the magma reservoir, the type of magma feeding and the
influence of the regional stress field and the strain rate in the area.
The lack of a comprehensive model that can take all of these
features into account produces the uncertainties in the evaluations
of both short-term and long-term volcanic eruption forecasts.
REFERENCES
AMORUSO A., CRESCENTINI L. & BERRINO G. (2008) -
Simultaneous inversion of deformation and gravity changes
in a horizontally layered half-space: Evidence for magma
intrusion during the 1982-1984 unrest at Campi Flegrei
caldera (Italy). Earth Placet. Sci. Lett.
Doi:10.1016/j.epsl.2008.04.040.
BATTAGLIA M., TROISE C., OBRIZZO F., PINGUE F. & DE NATALE
G. (2006) - Evidence for fluid migration as the source of
deformation at Campi Flegrei caldera (Italy). Geophys. Res.
Lett., 33, doi:10.1029/2005GL024904.
CARLINO S. & SOMMA R. (2010) - Eruptive versus non-eruptive
behaviour of large calderas: the example of Campi Flegrei
caldera (Southern Italy). Bull. Volcanol. doi 10.1007/s00445-
010-0370-y.
DE NATALE G., PINGUE F., ALLARD P. & ZOLLO A. (1991) -
Geophysical and geochemical modelling of the Campi
Flegrei caldera. J Volcanol Geoth. Res., 48, 199–222.
DE NATALE G., TROISE C. & PINGUE F. (2001) - A mechanical
fluid-dynamical model for ground movements at Campi
Flegrei caldera. J. Geodyn., 32, 487–517.
JELLINEK A.M. & DEPAOLO D.J. (2003) - A model for the origin
of large silicic magma chambers: precursors to caldera
forming eruptions. B. Volcanol., 65, 363-381.
MCKEE C., TALAI B., LAUER N., STEWART R., DESAINT OURS P.,
ITIKARAI I., PATIA H., LOLOK D., DAVIES H. & JOHNSON R.W.
(1995) - The 1994 eruption at Rabaul volcano, Papua New
Guinea. General Assembly Int. Un. Geod. Geophys., Boulder,
CO.
WOHLETZ, K,CIVETTA L&ORSI, G (1999) - Thermal evolution
of the Phlegreaean magmatic system. J Volcanol. Geoth.
Res., 91, 381–414.

Eruptive processes in the Averno 2 eruption (Campi Flegrei, Italy):
constraints based on geochemistry of bulk pumices, glassy matrices
and melt inclusions
Key words: Averno 2 eruptions, Campi Flegrei.
The Averno 2 eruption (Av2) occurred 3.7 ka ago in the
northwest sector of the Campi Flegrei caldera (CFc). The
eruption is one of the youngest of the caldera, the 1538 AD
eruption of Monte Nuovo being the ultimate. Av2 represents a
moderate-magnitude event, which characterized by complex
eruptive activity with alternating plinian to surge activity that
generated a sequence of pyroclastic-fall and -ash deposits. The
Av2 eruptive products were subdivided into three members
named A through C (from the base to top) by DI VITO et alii
(2001). Member (A) emplaced during the first phase of the
eruption consists in a first thin coarse-ash bed (A0a) overlain by a
coarser fallout deposit (A0). It includes other six fallout beds
(from A1 to A5), intercalated with minor ash-surge beds, of
which we only sampled the A2 intermediate layer (samples A2b
and A2t). In contrast, member B and C are mostly dominated by
dry surge beds and minor wet surges, respectively, with
subordinate fallout beds. Samples Bt and Cmb are pumice clasts
from, respectively, the units B and C, the latter forming the
uppermost part of the sequence. Petrography and chemical
analysis (SEM-EDS, electron microprobe and FTIR
spectroscopy) were performed on pumice samples, melt
inclusions, and host minerals (here clinopyroxene) in order to
constrain the pre-eruptive conditions of magma evolution and
degassing. Pumice clasts display an alkali-trachyte composition,
and show a slight chemical variation that is mainly related to
crystal fractionation. A0 layer (from member A) is the most
evolved trachytic magma and Cmb (from Member C), the leastevolved
alkali-trachytic. The compositional variation found in
A2t and BT tephra deposits is ascribed to syn-eruptive mingling
between the two extremes. The H2O concentration determined by
FTIR measurements in melt inclusions record significant
variations (from ~5 to 1.5 wt %). All together our data les us to
propose that the Averno 2 eruption mainly results from the
_________________________
CÉLINE FOURMENTRAUX (*), NICOLE MÉTRICH (*) (**), ANTONELLA BERTAGNINI (*) & MAURO ROSI (°)
(*) Istituto Nazionale di Geofisica e Vulcanologia, Pisa,
céline.fourmentraux@pi.ingv.it
(**) Institut de Physique du Globe, Paris, France.
(°) Dipartimento di Scienze della Terra, Università di Pisa.
639
successive extrusions of independent magma batches, emplaced
at 4 and 2 km in depth, along regional fractures bordering the
Neapolitan Yellow Tuff caldera.
REFERENCES
DI VITO M.A., BRAIA G., ISAIA R., ORSI G. & PIERMATTEI M.
(2001) - The Averno 2 eruption in the northwestern sector of
the Campi Flegrei caldera (Italy). In: GNV Framework
program 2000-2002, I year results - Volcanic hazard
assessment and zonation at the resurgent Campi Flegrei
caldera and their effects on man and environment.
Osservatorio Vesuviano Ed., 101-106.
SESSIONE 19

SESSIONE 19
Caldera unrest prior to intense volcanism in Campi Flegrei (Italy) at
4.0 ka B.P.: implications for caldera dynamics and future eruptive
scenarios
Key words: Campi Flegrei caldera, ground deformations,
volcanism, magma refilling.
The Campi Flegrei caldera is one of the highest risk volcanic
areas on the Earth. Since 15 ka, about 70 intra-caldera eruptions
have occurred across CF. These eruptions have been dominated
by phreatomagmatic and strombolian activity, although few
plinian eruptions and purely effusive events have also occurred.
The erupted magmas have been predominantly K-trachytes and
K-trachyphonolites, with minor mafic compositions, such as
shoshonites and latites. The last eruption produced the cone of
Monte Nuovo in 1538. In addition to volcanic activity, CF has
been characterized by large-scale uplift and subsidence for at
least 10,500 years.
This work investigates caldera dynamics during the last 5 ka.
The new stratigraphic and geochronological data show that the
Agnano-Monte Spina plinian eruption (AMS, 4.1 ka; DE VITA et
alii, 1999) was followed by a repose interval of 100-200 years.
The repose was ended by a sequence of about 15 eruptions in 150
years. Twelve of the events were of low magnitude and involved
some combination of phreatomagmatic, strombolian and effusive
activity. All but one of the eruptions occurred in the easterncentral
part of CF. They began with an explosive event (SMG,
3970 ± 65 BP), which erupted latites derived from the mixing of
K-basaltic (40 wt%) and K-trachytic (60 wt%) magmas. After this
event, the erupted magmas evolved in composition from latite to
K-trachyte and K-trachyphonolite. The eruptions were clustered
along NW-SE-trending faults at the boundary of the minor AMS
caldera. The exception to the clustering was the Averno event, in
the western sector of the caldera. Tephra from the Averno 2
eruption was deposited while Solfatara was still active and
provides the first direct evidence that concurrent explosive
activity has occurred in two different sectors of the caldera.
Recognition of a new, caldera-wide level of marine deposits
between the products of the MS and following eruptions shows
_________________________
(*) Istituto Nazionale di Geofisica e Vulcanologia, sezione di Napoli
Osservatorio Vesuviano, roberto.isaia@ov.ingv.it
(**) Dipartimento di Scienze della Terra, Università degli Studi di Pisa,
marianelli@dst.unipi.it, sbrana@dst.unipi.it
ROBERTO ISAIA (*), PAOLA MARIANELLI (**) & ALESSANDRO SBRANA (**)
640
that subsidence and uplift (by as much as about 30 m in the zone
of Pozzuoli) must have occurred during the post-AMS repose
interval. The emission of the SMG latites (mixing-derived)
concomitant with the uplift suggest that deformation was
triggered by the replenishment of a K-trachytic reservoir with less
evolved K-basalts. From melt-inclusion data the depth of the
reservoir is estimated to have been less than 3 km. Reservoir
replenishment and magma mixing has also been proposed to
explain the 1994 eruption and preceding uplift at Rabaul caldera
(ROGGENSACK et alii, 1996). At CF, shoshonites and latites have
also been erupted between 10 and 8.2 ka BP. It is thus possible
that replenishment of a shallow magmatic system with mafic
magma is a regular precursor to extended episodes of volcanic
activity. In this case, a future eruptive crisis is expected be
preceded by several meters of ground deformation as
replenishment occurs. The current trend of uplift across the
central sector of the caldera since 1969 may thus represent the
unrest expected before a renewal of volcanism within an interval
of decades to centuries. The new data on volcanic activity at c.
4.0 ka BP confirm that eruptions may cluster at intervals of a few
years to decades. They also show that eruptions can occur at the
same time in different sectors of the caldera, perhaps in the
manner documented in 1994 during the simultaneous eruptions of
Vulcan and Tavurvur on opposite sides of Rabaul caldera. Plans
for mitigating volcanic hazard must therefore prepare for a return
to eruptions occurring at intervals of decades or less, including
the possibility of simultaneous eruptions from two or more vents
across the caldera.
REFERENCES
DE VITA S., ORSI G., CIVETTA L., CARANDENTE A., D’ANTONIO
M., DEINO A., DI CESARE T., DI VITO M., FISHER R.V., ISAIA
R., MAROTTA E., NECCO A., ORT M.H., PAPPALARDO L.,
PIOCHI M. & SOUTHON J. (1999) - The Agnano-Monte Spina
eruption (4100 years B.P.) in the restless Campi Flegrei
caldera. J. Volcanol. Geoth. Res., 91, 269–301.
ROGGENSACK K., WILLIAMS S.N., SCHAEFER S.J. & PARNELL JR
R.A. (1996) - Volatiles from the 1994 eruptions of Rabaul:
understanding large caldera systems. Science, 273, 490-493.

Key words: Ischia Island, laccolith, magma feeding, resurgence
caldera.
VOLCANIC HISTORY AND SEISMICITY
In this study we provide a general structural picture of Ischia
island shallow crust to model the processes occurring at shallow
depth, by using geological, geophysical, historical seismicity data
and analytical structural models of the island (PENTA &
CONFORTO, 1951; CUBELLIS &LUONGO, 1998; CUBELLIS et alii,
2004; CARLINO et alii, 2006; PAOLETTI et alii, 2009; VEZZOLI et
alii., 2009; SBRANA et alii, 2009). These studies support the
hypothesis of the presence of a shallow laccolith, which is
responsible of the resurgence of Mt. Epomeo, following the
Green Tuff eruption, volcanic activity and seismicity of northern
sector of the island. The occurrence of magmatic intrusion and high
geothermal gradients (180-200°C km -1 ), have produced a shallow
brittle-ductile transition (~ 2 km b.s.l.), deeper northward.
The island of Ischia was characterised by a long period of
volcanic activity: the oldest outcroppings were erupted about 150
ka ago; the last eruption occurred in the 1301-1302 A.D.
Historical records since 1228 A.D. testify the occurrence of
numerous earthquakes in the island which produced heavy
damage and fatalities (Fig. 1). The seismic events, except for one
minor earthquake, were not correlated to eruptions, but they may
be related to the episodic reactivation of the same tectonic
structure. This observation, joined with geological and
geophysical data, supports the hypothesis that the seismicity is
linked to a local stress field, probably generated by volcanic
processes. Since the active-quiescent periods of the island seem
to be marked by Mt. Epomeo uplift and subsidence respectively,
the monitoring of long term deformation of the resurgent block is
fundamental to understand the state of Ischia volcanic system.
Nowadays the island is undergoing to slow phase of subsidence.
Before this phase uplift pulses were associated to earthquakes
_________________________
Conceptual model of shallow magma feeding system for Ischia
Island (Italy)
GIUSEPPE LUONGO (*), STEFANO CARLINO (**), ELENA CUBELLIS (**) & FRANCESCO OBRIZZO (**)
(*) Dipartimento di Scienze della Terra, Università di Napoli “Federico II”,
giuseppe.luongo@unina.it
(°) Istituto Nazionale di Geofisica e Vulcanologia - Sezione di Napoli
Osservatorio Vesuviano, elena.cubellis@ov.ingv.it
641
occurred between 1228 and 1883 years, generated by the stress
field due to short-term magmatic impulses. On the other hand, an
enduring inversion of the present Mt. Epomeo movement could
represent an important long term precursor of volcanic activity
Fig. 1 - The island of Ischia and main features related to its recent dynamic;
red dots represent the main hot springs and fumaroles fields.
reactivation.
DYNAMICS OF THE ISLAND AND MAGMA SYSTEM
The uplift/subsidence of the Mt. Epomeo is controlled by the
increase/decrease of pressure in the shallow laccolith (CARLINO et
alii, 2006) (Fig.2). During eruptions the uplift stopped, because
the magma founded feeder dykes and no longer exerted pressure
exceeding the overburden; on the contrary the earthquakes
occurred during the resurgence of Mt. Epomeo.
The whole island is subject to subsidence for the stretching of
the crust in Tyrrhenian Sea and along the near continental margin
of Italian Peninsula since 10 millions years B.P.. In addition to
this process large and rapid changes in sea level occurred in the
area during the Late Quaternary. Some authors (RAMPINO et alii,
1979; NAKADA &YOKOSE, 1992) have considered a possible
relationship of volcanic activity in the coastal and island
volcanoes to large sea level changes during the Late Quaternary.
SESSIONE 19

SESSIONE 19
If large and rapid changes of sea level at Ischia, during the
uppermost Quaternary could induce eruptive activity, remains to
be proved. Consequently the sea level data of the last 140 ka B.P.
are compared with the volcanic activity of Ischia. The oldest
outcrops in the island date back to about 150 ka B.P.; since that
time five phases of activity have been distinguished, which were
grouped in an older cycle and a younger cycle, separated by the
55 ka B.P. large eruption of Mt.Epomeo Green Tuff (MEGT).
Fig.2 - Sketch of shallow crust of Ischia island inferred by geophysical data
and historical seismicity.
At the same time of sea-level changes during the last 30 ka,
ground uplifting occurs in the island, since the MEGT caldera
resurgence, with permanent ground deformation produced by the
increase of pressure in the shallow magma reservoir. This process
overcomes largely the subsidence in the investigated period. In
the short-term, i.e. as the last 2000 yrs, it is difficult to separate
the share of the two opposite phenomena for lack of data. Today
we observe Greeck and Roman ruins along the coast of the island
submerged about 2 m b.s.l.. Geographers comparing historical
and current maps of the island infer sinking of the coast since the
sixteenth century at a rate of 2.5 mm/years (NIOLA BUCHNER,
1965). During the time lapse from 1892 to 1912 years,
GRABLOVITZ (1920-21) measured at the tide gauge of Ischia
harbour a subsidence with a velocity of 3 mm/y. Afterwards
measurements of sea levels carried out in the island by
FRIEDLAENDER (1938) confirmed the results obtained by
GRABLOVITZ. Precise leveling data collected since the early
twentieth century show the lowering of the southern part of the
island which resembles a bowl-shaped sinking.
In the neighboring active caldera of Campi Flegrei the uplift
in historical times was accompanied by seismicity at which
sometimes explosions (Solfatara, 1198), or eruptions (Mt. Nuovo,
1538) follow it. If a similar process takes place at Ischia, we
should expect that significant seismicity will occur only in case of
new uplift phase of Mt. Epomeo block. Empirical data show that
642
to predict incoming eruptions the occurrence of earthquakes is a
necessary but not sufficient condition.
REFERENCES
CARLINO S., CUBELLIS E., LUONGO G. & OBRIZZO F. (2006) - On
the mechanics of caldera resurgence of Ischia Island. In: C.
Troise, G. De Natale and C.R.J. Kilburn (Eds.) - Geol. Soc.
London Special Pubblication, 269, 181-193.
CUBELLIS E. & LUONGO G. (1998) - Il Terremoto del 28 luglio
1883 a Casamicciola nell’Isola d’Ischia ‘Il contesto fisico’,
Monografia 1 – Servizio Sismico Nazionale, Roma, 49–123.
CUBELLIS E., CARLINO S., IANNUZZI R., LUONGO G. & OBRIZZO F.
(2004) - Management of Historical Seismic Data Using GIS:
The Island of Ischia (Southern Italy). Nat. Hazard, 33, 379-393.
FRIEDLANDER I. (1938) - Sui bradisismi dell'isola d'Ischia e sulla
Grotta del Mago. Boll . Soc. Geogr. It, 7, 3, 44-54.
GRABLOVITZ G. (1920-21) - Sul sospetto bradisismo appenninico
1900-1908. BSSI, 21, 147 - 191, 1922, Roma.
NAKADA M. & YOKOSE H. (1992) - Ice age as a trigger of active
Quaternary volcanism and tectonism. Tectonophysics, 212,
321-329.
NIOLA BUCHNER D. (1965) - L’isola d’Ischia. Studio geografico.
Napoli.
PAOLETTI V., DI MAIO R., CELLA F., FLORIO G., MOTSCHKA K.,
ROBERTI N., SECOMANDI M., SUPPER R., FEDI M. & RAPOLLA
A. (2009) - The Ischia volcanic island (Southern Italy):
Inferences from potential field data interpretation. J. Volcanol.
Geotherm. Res., 179 (1-2), 69-86.
PENTA F. & CONFORTO B. (1951) - Risultati di sondaggi e di
ricerche geominerarie nell’isola d’Ischia dal 1939 al 1943 nel
campo di vapore, delle acque termali e delle forze endogene in
generale. Annali di Geofisica, 4, 159–191.
RAMPINO M.R., SELF S., FAIRBRIDGE R.W. (1979) - Can rapid
climate change cause volcanic eruptions. Science, 206, 826-
829.
SBRANA A,. FULIGNATI P., MARIANELLI P., BOYCE A.J. &
CECCHETTI A. (2009) - Exhumation of an active magmatichydrothermal
system in a resurgent caldera environment: the
example of Ischia (Italy). J. Geol. Soc. London, 166, 1016-
1073.
VEZZOLI L., PRINCIPE C., MALFATTI J., ARRIGHI S., TANGUY J.C. &
LE GOFF M. (2009) - Modes and times of caldera resurgence:
the

Key words: Eruption dynamics, Mercato, pulsating eruption,
Somma-Vesuvius.
New volcanological studies allowed reconstruction of the
eruption dynamics of the Pomici di Mercato eruption (ca. 8900
cal. yr B.P.) of Somma-Vesuvius.
Three main Eruptive Phases were distinguished based on two
distinct erosion surfaces that interrupt stratigraphic continuity of
the deposits, indicating that time breaks occurred during the
eruption. Absence of volcaniclastic deposits on top of the erosion
surfaces suggests that quiescent periods between eruptive phases
were short and probably lasted several days to weeks. Each of the
Eruptive Phases was characterised by deposition of alternating
fall and pyroclastic density current (PDC) deposits.
The fallouts blanketed a wide area toward the east, while the
more restricted PDC deposits inundated the volcano slopes.
Eruptive dynamics were driven by brittle magmatic
fragmentation of a phonolitic magma, which, because of its
mechanical fragility, produced a significant amount of fine ash.
External water did not significantly contribute either to
fragmentation dynamics or to mechanical energy release during
the eruption. Column heights were between 18 and 22 km,
corresponding to mass discharge rates between 1.4 and 6 x 10 7 kg s -1 .
The estimated on land volume of fall deposits ranges between a
minimum of 2.3 km 3 and a maximum of 7.4 km 3 .
Calculation of physical parameters of the dilute pyroclastic
density currents yields speeds of a few tens of m s -1 and densities
of a few kg m -3 , resulting in dynamic pressures lower than 3 kPa.
These data suggest that the potential impact of pyroclastic density
currents of the Pomici di Mercato eruption was smaller than other
Plinian and sub-Plinian eruptions of Somma-Vesuvius, especially
those of 1631 AD and 472 AD eruptions, which represent a
reference for the Vesuvian emergency plan.
The pulsating and long-lasting behaviour of the Pomici di
Mercato eruption is unique to whole history of large explosive
_________________________
Stratigraphy and eruptive dynamics of a long-lasting Plinian
eruption of Somma-Vesuvius: the Pomici di Mercato
(8900 years B.P.)
DANIELA MELE (*), ROBERTO SULPIZIO (*), PIERFRANCESCO DELLINO (*) & LUIGI LA VOLPE (*)
(*) CIRISIVU, c/o Dipartimento Geomineralogico, Università di Bari,
d.mele@geomin.uniba.it
643
eruptions of Somma-Vesuvius.
We suggest an eruptive scheme in which discrete magma
batches rise from the magma chamber through a network of
fractures. The injection and rise of the different magma batches
was controlled by the interplay between magma chamber
overpressure and local stress.
The intermittent discharge of magma during a large explosive
eruption is unusual for Somma-Vesuvius, as well as for other
volcanoes worldwide, and yields new insights for improving our
knowledge of the dynamics of explosive eruptions.
SESSIONE 19

SESSIONE 19
Key words: Campi Flegrei caldera, CGPS data, ground
deformation and sources, tide gauges data.
INTRODUCTION
Campi Flegrei caldera is located just west of the city of
Naples, within the central-southern sector of a large graben called
Campania Plain. It is an active volcanic area marked by a quasicircular
caldera depression, probably formed by a huge
ignimbritic eruption occurred about 39000 years ago. This
caldera was generated by collapses produced by strong explosive
eruptions. The only eruption in historical times occurred in 1538,
building a spatter cone called Mt. Nuovo. Campi Flegrei area
periodically experiences significant deformation episodes, with
uplift phenomena reaching more than 3.5 m in 15 years (from
1970 to 1984), which caused during 1983-84 the temporary
evacuation of about 40000 people from Pozzuoli town.
The structural complexity of the Campi Flegrei area, together
with the evidence of a strong interaction between magmatic
chamber and shallow geothermal system, calls for a detailed
characterization of the substructure and of the magma-water
interaction processes.
The Campi Flegrei caldera is characterized by high volcanic
risk due to the explosivity of the eruptions and to the intense
urbanization of the surrounding area, and has been the site of
significant unrest for the past 2000 years (DE NATALE et alii,
2006). The caldera floor was raised to about 1.7 meters between
1968 and 1972; then a subsidence phase of about 0.2 m occurred
between 1972 and 1975 followed by a stable period until 1981.
Between 1982 and 1985 new uplift occurred and the caldera rose
about 1.8 m, without eruptive phenomena. Then a long-term
subsidence phase began, with small and fast mini-uplifts
superimposed (1989, 1994 and 2000). This behaviour was
observed until the end of 2004 when the subsidence stopped and
a new uplift phase started, different from previous ones for rate,
_________________________
Unrest at Campi Flegrei Caldera (Southern Italy)
during the last decade
FRANCESCO OBRIZZO (*), PROSPERO DE MARTINO (*), GIUSEPPE DE NATALE (*), FOLCO PINGUE (*),
UMBERTO TAMMARO (*), CLAUDIA TROISE (*) & PAOLO CAPUANO (**)
(*) INGV - Osservatorio Vesuviano, francesco.obrizzo@ov.ingv.it
(**) Dipartimento di Matematica e Informatica, Università di Salerno,
pcapuano@unisa.it
644
duration and amplitude, which, with a variable trend, still lasts.
CGPS AND TIDE GAUGES DATA
CGPS network (Fig. 1) and data analysis, during last decade,
allowed continuous and accurate tracking of ground deformation
affecting Campi Flegrei area, both for the vertical component
(also monitored continuously by tide gauge and periodically by
leveling surveys) and for the planimetric components, providing a
3D displacement field, allowing to better constrain the
inflation/deflation sources responsible for ground movements.
The vertical ground displacements at Campi Flegrei are also
tracked by the sea level using tide gauges (Fig. 1) located at the
Nisida (NISI), Port of Pozzuoli (POPT), Pozzuoli South- Pier
(POPT) and Miseno (MISE), in addition to the reference one
(NAPT), located in the Port of Naples. The data allowed to
monitor all phases of Campi Flegrei bradyseism since 1970,
providing results consistent with those obtained by geometric
leveling and, more recently, by the CGPS network.
Fig. 1 – The activity of Campi Flegrei is monitored by of 13 permanent GPS
and 5 tide gauge. The data are downloaded and analyzed automatically.
Removing, by deconvolution, the differential behavior of the
sea-level at a reference station provides an estimation of the local
ground level change.
The deformation field obtainable by CGPS and tide-gauge
stations plays an important role for the modeling and
interpretation of volcanic phenomena, as well as for forecasting
purposes. Since the deployment of CGPS, three small uplift
episodes occurred. The first one occurred from March to October

2000 and was partial recorded by CGPS stations that were
installed on May. This event was followed by a subsidence until
October 2002 with a maximum value over than 7 cm. After a
period of substantial stability a second uplift episode occurred
from November 2004 to November 2007 with a maximum uplift
of over 4 cm, followed by a subsidence period up to October
2007 with a maximum value of nearly -2 cm. In late 2007, finally,
the ground has once again reversed the movement direction with
an uplift that, in October 2009, has reached about 3 cm. After
that, a new phase of substantial stability seems to be started, even
if in presence of an oscillating trend.
Fig. 2 – Time series of weekly coordinates changes from 2000 to present along
North, East and Up directions at a CGPS station (RITE, see Fig. 1) and vertical
displacement inferred by deconvolution at Pozzuoli Port tide gauge POPT (see
Fig. 1), with the levelling data (red crosses) superimposed.
Fig. 3 – a) Different sources for uplift and subsidence events; b) Theoretical
maximum horizontal vs maximum vertical displacement ratios, as computed for
three source shapes: prolate ellipsoid with 2:1 axis ratio, sphere, oblate ellipsoid
with 1:2 axis ratio.
BATTAGLIA et alii, 2006 and DE NATALE et alii, 2006 put in
evidence, from joint inversion of displacement and microgravity
data, two different sources (Fig. 3a) responsible for the first phase
of uplift and for the subsidence. Uplift is ascribed to overpressure
in a sharply oblate ellipsoidal reservoir of magmatic fluids
exsolved from the magma chamber; subsidence to the lateral
drainage of overpressured water from geothermal system, having
a prolate ellipsoidal shape. There must be, then, a phase in which
magmatic fluids are injected in the geothermal system, causing
water pressurization which strongly amplifies the surface
displacement. Starting from the previous mini-uplift of 2000,
horizontal to vertical displacement ratios (R), calculated by
CGPS data, shows a rather constant low value indicating a rather
deep and sharply oblate source geometry. This model is
compatible (Fig. 3b) with the activation of the deeper source of
645
magmatic fluids inferred from BATTAGLIA et alii, 2006 and
TROISE et alii, 2006.
CONCLUSION
Data from the recent uplift, compared with data from 2000
episode and with results of BATTAGLIA et alii (2006) about 1982-
1984 unrest, indicate that both large and small uplift episodes
start with a pressure increase within a relatively deep (3-5 km)
reservoir, likely to contain magmatic fluids exholved from the
magma chamber. Eventually, the fracturing of rocks separating
this reservoir from the shallow aquifers causes injection of
magmatic fluids into the shallow geothermal system, with a
progressive strong increase of ground deformation typical of
large unrests like 1969-1972 and 1982-1984. Increase of pressure
in magmatic fluids and injection in shallow aquifers is also
suggested by the observed peaks in CO2 flux, following both
small and large uplift episodes of some months (CHIODINI et alii,
2003).
If pressure pulses in magmatic fluids represent inflow of new
magma at shallow depths, the occurrence of repeated uplift
episodes represent progressive increase in the magma chamber
pressure which, when overcoming the rock strength, gives rise to
eruptions. This is what likely occurred in the century of uplift
preceding the 1538 Mt. Nuovo eruption.
REFERENCES
BATTAGLIA M., TROISE C., OBRIZZO F., PINGUE F. & DE NATALE
G., (2006) - Evidence for fluid migration as the source of
deformation at Campi Flegrei caldera (Italy), Geophys. Res.
Lett., 33, L01307.
CHIODINI G., TODESCO M., CALIRO S., DEL GAUDIO C.,
MACEDONIO G. & RUSSO M. (2003) - Magma degassing as a
trigger of bradyseismic events: the case of Phlegrean Fields
(Italy), Geophys. Res. Lett., 30(8), 1434.
DE NATALE G., TROISE C., PINGUE F., MASTROLORENZO G.,
PAPPALARDO L., BATTAGLIA M. & BOSCHI E. (2006) - The
Campi Flegrei caldera: unrest mechanisms and hazards. In:
C. Troise, G. De Natale & C.R.J. Kilburn (Eds.) -
Mechanisms of activity and unrest at large calderas. Geol.
Soc., London, Spec. Publ., 269, 25–45.
TROISE C., DE NATALE G., PINGUE F., OBRIZZO F., DE MARTINO
P., TAMMARO U. & BOSCHI E. (2007) - Renewed ground
uplift at Campi Flegrei caldera (Italy): New insight on
magmatic processes and forecast, Geophys. Res. Lett., 34,
L03301.
SESSIONE 19

SESSIONE 19
Fast exhumation of a magmatic-hydrothermal system in a resurgent
caldera environment. The example of Ischia Island (Italy)
ALESSANDRO SBRANA (*), PAOLO FULIGNATI (**) & PAOLA MARIANELLI (°)
Key words: Ischia, magmatic-hydrothermal system, melt and
fluid inclusions, resurgent caldera.
INTRODUCTION
Ischia Island represents a rare case of well-exposed, young,
and ongoing caldera resurgence. Resurgence is a quite common
feature in large caldera depressions, with an increase in pressure
in the magmatic system and the inflation of the magma chamber
Fig. 1: Schematic geological map of Ischia with the location of sampling
points.
generally being considered as the triggering mechanism for the
doming of the caldera floor. The depressions formed by caldera
structures typically host active high temperature geothermal
systems, which are exploited for electrical energy production all
_________________________
(*) Dipartimento di Scienze della Terra, Università di Pisa,
sbrana@dst.unipi.it, fulignati@dst.unipi.it, marianelli@dst.unipi.it
Lavoro eseguito nell’ambito del progetto CAR.G con il contributo
finanziario della Regione Campania e dell’ISPRA.
646
around the world. Furthermore, caldera structures are often
associated with epithermal precious and base metal
mineralization that represent the "fossil" equivalent of the active
geothermal systems. Ischia Island offers an unique opportunity to
examine the hydrothermal system's 3-dimensional anatomy
because of its exposure related to Mt Epomeo uplift. This work
fills a gap in the knowledge of the magmatic-hydrothermal system
of Ischia and, more generally, offers an important contribution to
the knowledge of the magmatic-hydrothermal processes that
occur inside a resurgent caldera environment characterized by
shallow and active magmatic system.
RESULTS AND DISCUSSION
Ischia Island is located in the northern part of the Gulf of
Naples, and, with the Campi Flegrei and Mt. Vesuvius,
constitutes a most important Quaternary volcanic area of
Mediterranean region (Fig. 1).
The volcanic activity on Ischia started before 150 kyr ago
with the emplacement of lava flows, domes, tuff and scoria cones
that formed a huge volcanic field, the 1302 Arso eruption ended
the volcanic activity on the island. Between 73 and 56 kyr ago
Ischia experienced a period of intense explosive volcanic activity
characterized by numerous trachytic Plinian and ignimbritic highmagnitude
eruptions (including "Green Tuff) that provoked the
formation of a poly-phase caldera depression. This was followed
by the resurgence of Mt. Epomeo block, the major uppermost
relief of the island (787 m a.s.l).
For our study, juvenile fractions of Ischia volcanic deposits
were selected to provide samples suitable for melt inclusion
studies. Melt inclusion studies provide a fundamental tool for the
reconstruction of the P-T-X conditions of the magmatic reservoir.
Selected pumices shows variable vesicularity and crystal content
( ~1 to 15 vol. %). Their mineralogical assemblage is formed by
K-feldspar, plagioclase, clinopyroxene biotite, oxides, apatite and
titanite in varying proportions. Well-quenched primary glassy
melt inclusions (MIs) (20–60 μm in size) are found in
clinopyroxene of pumices of the juvenile fraction. The MIs are all
of similar trachytic composition and FT-IR investigation revealed
that their dissolved water content ranges from 1.6 and 3.1 wt.%
with a strong mode between 2 and 3 wt.%, indicating that melt
inclusions formed within a magmatic storage region located at

about 2 km. Microthermometry of the MIs provided a range
homogenization temperatures between 960 °C and 1050 °C, with
a mode of 1010°C.
Holocrystalline, non-equigranular xenoliths of syenitic
subvolcanic rocks are composed of primary K-feldspar,
plagioclase, clinopyroxene, K-pargasitic amphibole, biotite and
accessory titanite and apatite. Fluid inclusions (FIs) in K-feldspar
were examined in both hydrothermally altered and fresh
xenoliths. The mixture of non-silicate daughter minerals observed
in these inclusions is suggestive of a complex composition of the
entrapped fluid, in which anions such as sulfate and fluoride are
present in significant amounts in addition to chlorides.
Samples from the intracaldera tuff units, forming the Mt.
Epomeo uplifted block, reveal the occurrence of different
hydrothermal mineralogical assemblages that substitute the
original primary phases and glasses. They span (from top to
bottom of the sequence) from mixed layer illite/smectite (I/S) ±
zeolites (natrolite and phillipsite) (Facies 1, related to the argillic
alteration facies that characterizes the upper impermeable cover
of geothermal systems) to phengite + illite + albite + adularia ±
mixed layers chlorite/smectite (C/S) (Facies 2). This suggests that
the tuff sequence was affected by hydrothermal alteration zoning
typical of geothermal systems. Furthermore, several syenitic
xenoliths are pervasively altered by hydrothermal mineralogical
assemblages different from those observed in the hydrothermally
altered intracaldera tuff units. The mineralogical assemblages that
characterize these samples are: chlorite + albite + adularia + illite
(Facies 3), and hydrothermal biotite + epidote + adularia + albite
+ illite (Facies 4; this Facies coupled with Facies 2 and 3
correspond to propylitic alteration that characterizes geothermal
reservoirs).
CONCLUSIONS
The multidisciplinary approach of investigation carried out in
this study led to the development of an integrated model
concerning the evolution of the magmatic-hydrothermal system of
Ischia island (Fig. 2). At Ischia volcanic field, after high volume
caldera forming eruptions (60-56 kyr ago), a very important
resurgence affected the center of the caldera floor exposing a
thick pile of caldera filling deposits. The investigation of these
thick ignimbrite deposits highlighted that these rocks were
subjected to strong hydrothermal circulation mainly carried out
by fluids of marine origin. This allowed the development of a
geothermal system with argillized units forming the impermeable
cover of the system and the underlying propylitized units that can
be considered the geothermal reservoir.
The high uplift rate of Mt Epomeo block induced negligible
effects of superimposition of lower temperature hydrothermal
alteration processes. We have clear evidence that fluids of the
deepest part of the hydrothermal system penetrated the most
647
external parts of subvolcanic bodies, present in the deeper parts
of the island, to a depth of at least 1 km. The engine of the high-T
hydrothermal system of Ischia can be identified in the shallow
(top at around 2 km of depth) and wide magmatic system that
hosted hot (around 1000°C) trachytic melts. The results of this
work fill a gap in the knowledge of Ischia volcanic system and
can therefore be used as a dissected analog for the architecture of
active hydrothermal systems that are inaccessible at present.
Fig. 2. Schematic sequence summarizing the evolution of Ischia magmatichydrothermal
system. 1) Caldera filling eruptions (60-56 kyr); 2)
Development of seawater-dominated hydrothermal system inside cauldron;
heat energy was supplied by the shallow (~ 2km of depth) magmatic system;
3) Resurgence and exhumation of part of the hydrothermal system, which
remains active today in the footwall sectors of the caldera. Red arrows =
hydrothermal fluids; blue arrows = surficial waters.
SESSIONE 19

SESSIONE 19
RENATO SOMMA (*), THOMAS WIERSBERG (**), ALESSANDRO FEDELE (*) & GIUSEPPE DE NATALE (*)
Key words: Fluids, geochemistry, phlegrean fields.
In late 2009, a new continuous gas monitoring research
initiative started at a fumarole field located about 1 km south-est
from Solfatara volcano named “Pisciarelli”. The primary goal of
the experiments was to prove that monitoring is possible with the
set-up described below, and to compare the new data obtained at
Pisciarelli with those of the complete literature record obtained
by discrete gas monitoring at the investigated site (Fig.1)
Solfatara
crater
At Pisciarelli, a continuous gas flow was adjusted with a
diaphragm pump, and the gas piped through a 200 m Teflon©
tube away from the emission point. The temperature was
measured periodically in the fumarole with a K-type
thermocouple (inserted 30 cm into the fumaroles monitored)
The released gas phase primary consists of water gas, which
was trapped in a refrigerator and then further cooled into a
second refrigerator (Fig.2).
Continuous in situ measurements of gases at
Pisciarelli - Phelgrean Field
Fumarole "Soffinonissimo"
Fig. 1 – Map of study area at Pisciarelli fumarole field.
_________________________
Monitoring station
Fumarole "Pisciarelli"
(*) Istituto Nazionale di Geofisica e Vulcanologia, Sezione di Napoli,
Osservatorio Vesuviano, renato.somma@ov.ingv.it
(**) GeoForschungsZentrum Potsdam, Section 4.2 Potsdam, Germany
648
The remaining, almost water-free gas phase was continuously
analysed with a quadrupole mass spectrometer for the following
components: H2, H2S, CH4, N2, O2, Ar, He, and CO2. The gas line
was also connected to a tuneable diode laser spectrometer for
CO2 concentration measurements. Little surprising, the dry gas is
dominated by CO2 (> 97 vol%), followed by H2S, H2, CH4, and
He. Due to the experimental set-up, the gas phase generally
shows a varying contribution of atmospheric gases (O2, N2, Ar).
For which the data where correct as air-free. During the time of
investigation (about 7 months) clear differences in the gas
compositions of the investigate fumaroles were observed within
the analytical uncertainties of the experiment, confirming the
possibility to use this continuous gas monitoring set up for long
term monitoring. This is in good agreement with the available gas
composition in literature and also with two episodes of small size
emission of gases occurred during the monitoring time.
Fig.2 – Sketch of the actual gas monitoring set-up at Pisciarelli
PRELIMINARY RESULTS AND DISCUSSION
The concentration and the deviation (in percent) from its
starting value on Jan 23, 2009 is as follow: CO2 (98.4 vol. %),
H2S (0.24 vol. %), N2* (1.13 vol. %), CH4 (65 ppmv), H2 (0.089
vol. %), and He (7.3 ppmv) at Pisciarelli. O2 and most Ar is
related to atmospheric contamination of the gas line After a short
phase with no significant variations in the gas composition, the
concentrations of H2 and He began to rise at around Feb 1,
followed by an increase of CH4 that starts about one week later.

By now (March 30), the amount of CH4 at Pisciarelli has more
than doubled; H2 and He increased more than 50% (Fig. 2).
Within this time interval, CO2, H2S and N2* do not show
significant variations.
Two off-line gas samples taken at “Bocca Nuova” also
demonstrate an increase in He from 11 ppmv on Dec 11, 2008 to
17 ppmv on Jan 23, 2009. Isotope data of these samples reveal an
almost pure crustal origin of the additional helium: the aircorrected
3 He/ 4 He ratio decreases from 2.989 ± 0.043 R/Ra for
the December sample to 1.818 ± 0.028 R/Ra for the sample taken
in January (R/Ra is the 3 He/ 4 He ratio relative to the atmospheric
ratio of 3 He/ 4 He = 1.39 × 10 -6 ).
It is remarkable that gases showing increasing concentrations
derive from different sources (He is radiogenic, H2 and CH4 is
produced by hot fluid-rock interaction), but show all a relatively
low water solubility. This suggests that the process responsible
for the relative increase in concentrations is maybe linked with
abundant water at depth.
649
SESSIONE 19

SESSIONE 19
Evaluating the regional volcanic ash hazard of Neapolitan volcanoes
from geological data
ROBERTO SULPIZIO (*), GIOVANNI ZANCHETTA (**), BENOIT CARON (**), PIERFRANCESCO DELLINO (*),
DANIELA MELE (*), DONATELLA INSINGA (°), MARTINE PATERNE (°°),
GIUSEPPE SIANI (§) & ROBERTO SANTACROCE (**)
Key words: Neapolitan volcanoes, tephrostratigraphy, volcanic
ash, volcanic hazard.
The explosive activity of the Neapolitan Volcanoes (Somma-
Vesuvius, Ischia and Campi Flegrei) produced and dispersed
large amount of volcanic ash, which pose a threat to environment,
economy and human health over a large part of the Mediterranean
area. Volcanic ash (diameter < 2 mm) is the result of intense
magmatic or phreatomagmatic fragmentation during explosive
volcanic eruptions. After injection into the atmosphere, the ash is
dispersed as convective columns and umbrella clouds, which are
subject to the combined effects of gravity and wind speed, or are
transported close to the ground as pyroclastic density currents
(PDCs; e.g. SULPIZIO et alii, 2008).
Irrespective of the eruptive mechanism or intensity, ash
particles usually affect wide areas around volcanic centres, and
can cause severe damage and casualties in both proximal and
medial areas. The accumulation of ash can induce roof collapses,
interruption of lifelines (roads, railways, etc.), closure of airports
and damage to communication or electric lines (e.g. BLONG,
1984).
The injection of ash into the atmosphere can cause damage to
aircraft or can impact public health causing, for example,
respiratory problems (e.g. HORWELL & BAXTER, 2006). Ash
deposition decreases soil permeability, increases surface runoff,
and promotes floods (e.g. FAVALLI et alii, 2006). Ash leachates
can result in pollution of water resources (e.g. STEWART et alii,
2006), damage to agriculture and forest, effect pasture and
livestock health, impinge on aquatic ecosystems and alter the
_________________________
(*) CIRISIVU, c/o Dipartimento Geomineralogico, Università di Bari,
r.sulpizio@geomin.uniba.it; p.dellino@geomin.uniba.it;
d.mele@geomin.uniba.it
(**) Dipartimento di Scienze della Terra, Università di Pisa,
zanchetta@dst.unipi.it; caron@dst.unipi.it; santac@dst.unipi.it
(°) IAMC-CNR, Napoli, donatella.insinga@iamc.cnr.it
(°°) LSCE-CNRS, Gif sur Yvette, martine.paterne@lsce.cnrs.fr
(§) IDES - Université Paris Sud, Orsay, siani@ugeol.p-sud.fr
650
geochemical environment of the seafloor (e.g. HAECKEL et alii,
2001).
Therefore, the impact of fine ash can determine important
economic loss for affected communities, and can rapidly
deteriorate if no preventive measures were taken. All of these
impacts and processes have surely affected the central
Mediterranean area during past eruptions of Neapolitan
volcanoes, as testified by the abundance of ash layers in the
stratigraphic successions.
Reliable records of proximal, medial and distal ash deposits
are in fact available from outcrops, historical data, lacustrine and
marine cores. These occurrences, together with the detailed
knowledge of the eruptive history of the Neapolitan volcanoes at
least for late Pleistocene and Holocene, makes the Central
Mediterranean area an exceptional site for detailed studies on ash
dispersal.
Despite some recent advances in understanding the impact of
fine ash on environment and infrastructure, the dynamic of
dispersal of fine ash remains poorly understood, and
consideration of the associated hazards have not yet been fully
addressed and included in the mitigation plans, as recently
demonstrated by the Eyjafiallajokull eruption in Iceland.
As an example, we present and discuss the data of ash
dispersal from some explosive eruptions of Neapolitan volcanoes,
which dispersed centimetric thick ash blankets hundred of
kilometres from the source, irrespective of the more limited
dispersal of the respective coarse grained fallout and PDC
deposits.
The collected data also highlight the major role played by
lower atmosphere winds in dispersal of ash from weak plumes
and ash clouds that accompany PDC emplacement.
REFERENCES
BLONG R.J. (1984) - Volcanic hazards. A Sourcebook on the
Effects of Eruptions. Academic Press, Sydney. 424 pp.

FAVALLI M., PARESCHI M.T. & ZANCHETTA G. (2006) -
Simulation of syn-eruptive floods in the circumvesuvian plain
(southern Italy). Bull. Volcanol., 68, 349–362.
HAECKEL M., VAN BEUSEKOM J., WIESNER M.G. & KONIG I.
(2001) - The impact of the 1991 Mount Pinatubo tephra
fallout on the geochemical environment of the deep-sea
sediments in the South China Sea. Earth Plan. Sc. Lett., 193,
151-166.
HORWELL C.J. & BAXTER P.J. (2006). The respiratory health
hazards of volcanic ash: a review for volcanic risk mitigation.
Bull. Volcanol., 69, 1–24.
STEWART C., JOHNSTON D.M., LEONARD G.S., HORWELL C.J.,
THORDARSON T. & CRONIN S.J. (2006) - Contamination of
water supplies by volcanic ashfall: A literature review and
simple impact modelling. J. Volcanol. Geoth. Res, 158, 296-
306.
SULPIZIO R., BONASIA R., DELLINO P., DI VITO M.A., LA VOLPE
L., MELE D., ZANCHETTA G. & SADORI, L. (2008) -
Discriminating the-long distance dispersal of fine ash from
sustained columns or near ground ash clouds: the example of
the Pomici di Avellino eruption (Somma-Vesuvius, Italy). J.
Volcanol. Geoth. Res., doi:10.1016/j.jvolgeores.2007.11.012
651
SESSIONE 19

SESSIONE 19
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SESSIONE 19

SESSIONE 19
654

SESSIONE 20
Variazioni topografiche: cause e conseguenze
CONVENERS
Carlo Doglioni (Università Roma "La Sapienza")
Claudio Faccenna (Università Roma TRE)
655
SESSIONE 20

SESSIONE 20
Pliocene-Quaternary uplift of the Southern Apennines: constraints
from geomorphological, apatite fission tracks and (U-Th)/He data
ALESSANDRA ASCIONE (*), STEFANO MAZZOLI (*), ANTONIO PIGNALOSA (**),
ETTORE VALENTE (*) & MASSIMILIANO ZATTIN (°)
Key words: Geomorphology, low-T thermochronometry,
Southern Apennines, uplift.
The southern Apennines are characterised by an asymmetrical
topography, with maximum elevations mostly located within the
steeper southwestern flank of the chain. Also asymmetrical is the
position of the main divide, which follows neither the chain axis
nor the crest line, and develops for most of its length to the E of
the latter.
In order to unravel the relief formation history of this young
orogen, we integrated geomorphological, stratigraphical,
structural and apatite fission track and U-Th/He data useful to
constrain timing and amount of absolute and differential vertical
motions.
The southern Apennine chain is a NE-directed fold and thrust
belt, with the Apulian promontory representing the orogenic
foreland. Except for the remnants of so-called ‘internal’ tectonic
units that occur on top of the thrust pile, outcropping thrust sheets
consist of Mesozoic-Cenozoic rocks derived from the
sedimentary cover of the foreland plate. These include both
carbonate platform (Apennine Platform) and pelagic basin
(Lagonegro Basin) successions, locally covered by Neogene
foredeep and/or wedge-top basin sediments. Based on clay
mineralogy, vitrinite reflectance, apatite fission tracks (AFT) and
fluid inclusion data, exhumation of sedimentary units from depths
of a few kilometres (locally in excess of 5 km) has been
unravelled from throughout the chain.
The structure of the thrust belt is dominated, at shallow levels,
by low-angle tectonic contacts separating the carbonates of the
Apennine Platform, in the hanging wall, from the Lagonegro
Basin pelagic successions. At depth, the outcropping thrust belt
forms a displaced allochthon that has been carried onto a footwall
________________________
(*) Dipartimento di Scienze della Terra, Università degli Studi di Napoli
“Federico II”, alessandra.ascione@unina.it, stefano.mazzoli@unina.it
(**) Dipartimento di Scienze Geologiche e Ambientali, Università di
Bologna
(°) Dipartimento di Geoscienze, Università di Padova
656
of foreland strata essentially continuous with those exposed in the
Apulian promontory to the NE. Beneath the allochthon, the
western portion of the Apulian Platform was involved in the
younger shortening phases. Within the thrust belt, the tectonically
underlying Apulian Platform unit crops out in the Monte Alpi
area, providing the opportunity to obtain thermochronometric
data from these elsewhere deeply buried rocks.
Neogene thrusting was accompanied, since at least Late
Miocene times, by back-arc extension and sea-floor spreading in
the southern Tyrrhenian Sea. Crustal shortening in the southern
Apennines ceased around the early-middle Pleistocene boundary
(ca. 0.7 Ma). A new tectonic regime was established in the chain
and adjacent foothills. The structures related to this new regime,
characterized by a NE-SW oriented maximum extension, include
dominantly extensional faults that postdate and dissect the thrust
belt. Termination of crustal shortening was followed by a final
uplift also involving the Bradanic foreland basin area.
Constraints to the amount and timing of uplift and to the
reconstruction, for different time spans, of the distribution of
topographic highs and lows are provided by several geomorphicstratigraphical
evidences (e.g. distribution and elevation of
Quaternary marine terraces, elevation and amount of dissection of
Pliocene-Quaternary littoral deposits and correlative erosion
surfaces, distribution of Pliocene-Quaternary marine and
alluvial/lacustrine depocentres, features of the present-day
drainage net, etc.). Collectively, such evidences point to an
uneven, both spatially and temporally, uplift of the thrust belt–
foredeep system over a Late Miocene–Quaternary time span.
Apatite FT data indicate exhumation starting at around 10
Ma, but mostly occurring in the last 5 Ma. An older stage of fast
exhumation may be clearly distinguished from a younger stage of
substantially slower unroofing, based on apatite He data. High
exhumation rates, incompatible with erosion rates, characterized
the first, fast unroofing stage. Based on the integration with
surface evidence, which suggests that during Pliocene-early
Pleistocene times the eastern portion of the belt was affected by
repeated and diachronous large collapses, and by relatively slow
and spatially uneven coeval uplift, for the first unroofing stage a
dominant contribution of tectonic exhumation has to be invoked.
Younger (0.7 - 0 Ma) tectonic activity was dominated by: (i)
crustal extension propagating into the axial zone of the mountain

elt, producing Quaternary basins bounded by seismogenic,
master normal faults; (ii) dying out of crustal shortening; and (iii)
regional uplift, which was much stronger in the eastern belt of the
chain-foreland basin area than in the Tyrrhenian belt. These late
phenomena, although leading to dramatic changes in terms of
topography, drainage pattern and geomorphological evolution of
the mountain belt, were not so effective in producing rock
exhumation.
The overall evidence suggests a link between crustal
shortening, thrusting and tectonic exhumation in the mountain
belt. It may be envisaged that gravitational disequilibria produced
by deep-seated thrusting within the buried Apulian Platform,
triggering extension within the orogenic wedge, led to enhanced
tectonic exhumation during active crustal shortening. Slower
unroofing during the second exhumation stage most probably
resulted from tectonic exhumation slowing down as crustal
shortening was fading way, to finally cease during the
Pleistocene. In addition, such evidences suggest that the present
day large-scale geomorphic features of the southern Apennines
are largely inherited from pre-Quaternary tectonics.
657
SESSIONE 20

SESSIONE 20
Middle Miocene out-of-sequence thrusting and successive
exhumation in the Peloritani Mts, Sicily: late stage evolution
of an orogen unraveled by apatite fission-track and (U-Th)He
thermochronometry
MARIA LAURA BALESTRIERI (*), VALERIO OLIVETTI (**), FINLAY M. STUART (°),
CLAUDIO FACCENNA (**) & GIANLUCA VIGNAROLI (**)
Key words: Age pattern, thermochronology, wedge dynamics.
A detailed low-temperature thermochronological study that
coupled apatite fission-track (AFT) and (U-Th)/He (AHe)
analysis has been performed across the Peloritani Mountains belt
in eastern Sicily.
AFT and AHe analyses were carried out on apatite from
crystalline rocks from three north-south oriented transect and in
the northwestern edge of the Peloritani belt. AFT ages range
between 29.0±5.5 Ma and 5.5±0.9 Ma while AHe ages vary from
19.4 Ma to 3.3 Ma. The older AHe ages accompany the older
AFT ages.
Our older AFT ages in the Aspromonte Unit correspond to the
time of the early exhumation between 35 and 20 Ma in agreement
with the previous fission track data from (THOMSON, 1994). This
earlier exhumation occurred during or immediately after the
progressive stacking and thrusting leading to the building of the
main nappe edifice (e.g. DE GREGORIO et alii., 2003; ATZORI et
alii, 1994).
But the majority of the AFT ages post-date the deposition of
Stilo-Capo d’Orlando Formation, a late Oligocene-Burdigalian
terrigenous deposit that unconformably overlies the basement
units sealing the main tectonic contacts.
Through the coupling of the thermal modeling with the
stratigraphic record, a middle Miocene thermal event is revealed.
This event affected an inner intermediate portion of the Peloritani
Mountains and is confined by the distribution of the AFT ages

uplifted marine terraces, superimposed on the extensional
deformation accelerating the denudation rate (FERRANTI et alii,
2006).
REFERENCES
ATZORI P., CIRRINCIONE R., DEL MORO A. & PEZZINO A. (1994) -
Structural, metamorphic and geochronologic features of the
Alpine event in the south-eastern sector of the Peloritani
mountains (Sicily). Period. Mineral., 63, 113–125.
BILLI A., BARBERI G., FACCENNA C., NERI G., PEPE F. & SULLI
A. (2006) - Tectonics and seismicity of the Tindari Fault
System, southern Italy: Crustal deformations at the transition
between ongoing contractional and extensional domains
located above the edge of a subducting slab. Tectonics, 25,
TC2006, doi:10.1029/2004TC001763.
DE GREGORIO S., ROTOLO S. G., & VILLA I. M. (2003) -
Geochronology of the medium to high-grade metamorphic
units of the Peloritani Mts., Italy. Int. J. Earth Sci., 92, 852-
872.
FERRANTI L., ANTONIOLI F., MAUZ B., AMOROSI A., DAI PRA G.,
MASTRONUZZI G., MONACO C., ORRÙ P., PAPPALARDO M.,
RADTKE U., RENDA P., ROMANO P., SANSÒ P. & VERRUBBI V.
(2006) - Markers of the last interglacial sea level high stand
along the coast of Italy: tectonic implications. Quatern.
Intern., 145–146, 30–54.
FINETTI I. R., LENTINI F., CARBONE S., CATALANO S. & DEL BEN
A. (1996) - Il sistema Appennino Meridionale-Arco Calabro-
Sicilia nel Mediterraneo centrale: studio geologico-geofisico.
Boll. Soc. Geol. It., 115, 529-559.
LENTINI F., CARBONE S., CATALANO S., DI STEFANO A.,
GARGANO C., ROMEO M., STRAZZULLA S. &. VINCI G. (1995)
- Sedimentary evolution of basins in mobile orogenic belts:
examples from the Tertiary sequences of the Peloritani Mts.
(NE Sicily)., Terra Nova, 7(2), 161-170.
LENTINI, F., CATALANO S. & CARBONE S. (2000) - Carta
geologica della Provincia di Messina (scala1:50000).
LOCK, J. & WILLET S. (2008) - Low-temperature
thermochronometric ages in fold-and-thrust belts.
Tectonophysics, 456, 147–162.
THOMSON, S. N. (1994) - Fission track analysis of the crystalline
basement rocks of the Calabrian Arc, southern Italy:
evidence of Oligo-Miocene late orogenic extension and
erosion. Tectonophysics, 238, 331-352.
659
SESSIONE 20

SESSIONE 20
Late Quaternary marine terracing and fault displacement in eastern
Sicily : two distinct modes of faulting-induced deformation
Key words: Active fault, faulting-induced deformation, Late
Quaternary, marine terrace.
The relation between marine terracing and fault displacements
has been investigated along the Late Quaternary Siculo-Calabrian
Rift Zone, extending from Southern Calabria to the Eastern
Sicily. At the footwall of the major seismogenic segments of the
rift zone, the fault displacements have induced additional
components of the tectonic uplift that superimposed on the
regional signal, resulting in a local huge deformation of marine
terraces. Along the strike of faults, the strandlines of the marine
terraces commonly depict a large antiform, due to the variable
faulting-induced footwall uplift that progressively increases from
the tips to the central portion of the fault. The combination of coseismic
displacements and post-seismic rebounds generally
represents an half of the total vertical displacement along the
fault. These additional faulting-induced components of the
tectonic uplift approximate the regional signal. Along the 40 km
long Taormina Fault, in NE Sicily branch of the rift zone, they
reach the maximum values of about 0.9 mm/a which
superimposed on a regional signal of about 0.8 mm/a. As well,
along the 20 km long Avola Fault, belonging to the SE Sicily
branch of the rift zone, their values have been estimated at about
0.5 mm/a, while the regional signal has been evaluated at about
0.3 mm/a. At the footwall of the seismogenic faults, the marine
terraces are also severely deformed transversally to the direction
of the main fault segments. In the Catania area, the additional 0.7
mm/a faulting induced uplift-rate, measured at the footwall of the
coast-bounding fault segments, tapers to 0 at a distance of about
15 km from the fault plane where, as largely predicted by models,
only the regional signal (0.8 mm/a) can be recognised.
A different geometry of the marine terraces has been
recognised at the footwall of the normal faults controlling the
Late Quaternary extensional basins which developed along the
western flank of the rift zone (e.g. Augusta and Floridia Graben,
in the Hyblean Plateau, and the Peloritani-Eolie Graben, in NE
_________________________
STEFANO CATALANO (*), GIUSEPPE TORTORICI (*) & GINO ROMAGNOLI (*)
(*) Dipartimento di Scienze Geologiche – Università di Catania
catalano@unict.it
Lavoro eseguito nell’ambito del progetto S1 Convenzione INGV-DPC
2007/2009
660
Sicily). At the footwall of these faults, the strandlines of the
marine terraces are displaced at the rate of the regional signal and
still depict their original flat-lying attitude, to demonstrate the
absence of the faulting-induced deformation, either along the
strike or transversally with regards to the orientation of the fault
segments. Along these structures, in fact, the vertical fault
displacements mostly consisted of collapses of the hangingwall
that totally balanced the rate of uplifting of the footwall. As a
consequence, the uplift of the footwall of these structures has
been accompanied by relative sea-level stability in the
hangingwall, where the marine abrasion has been active at the
base of the coast-bounding fault scarp. In this case, marine
terracing represents the product of the progressive seaward
migration of the active fault-line (e.g. Peloritani Ridge) or the
effect of deactivation of the faults (e.g. Augusta Graben).
The difference in the mode of faulting-induced deformation
recognised along the Late Quaternary extensional faults of
Eastern Sicily can be related to the different significance of the
surface extensional processes. In the case of the seismogenic
segments, the surface deformation is that expected for faults
cutting the entire elastic layer and also involving mass
adjustments within deeper ductile horizons. On the other hand,
the second category of faulting-deformation seems to be linked to
shallower fault segments, which are accommodating gravitycontrolled
collapses, as response of the regional tectonic
uplifting. In particular, the occurrence of these collapsed basins is
confined within regions which are affected by high wavelength
and low amplitude doming of the Late Quaternary strandlines
that, together with seismological and geochemical data, strongly
suggest the occurrence of Mantle diapirism at depth.

Geomorphological response of fluvial and coastal terraces to
Quaternary tectonics and climate in the northern Marche coastal
area (central Italy) from geostatistical topographic analysis
Key words: Adriatic coast, central Italy, fluvial and coastal
terraces, geostatistical topographic analysis, river incision
rates, uplift rates.
INTRODUCTION
The geostatistical topographic analysis has proved to be a
useful quantitative method for the reconstruction of statistical
models of planar geomorphic markers of active tectonics
(BURBANK & ANDERSON, 2001). In fact, by collecting a
significant number of points on the remnants of a marker surface,
and applying the proper interpolation algorithm, it is possible to
delineate the statistical trend of its original surface.
In this work, we applied the geostatistical topographic
analysis to the remnants of fluvial and coastal terrace treads
exposed within the Metauro and Cesano Rivers valleys, in the
Adriatic foothills of the northern Marche Apennines (Central
Italy). Since the Middle-Late Pliocene, the Adriatic side of the
Apennines underwent regional tectonic uplift that accelerated
significantly during the Quaternary, with rates decreasing from
the Apennine chain axis towards its margins. In particular, the
rate of tectonic uplift peaked at the end of Early Pleistocene, with
an average rate of 0.3 – 0.5 mm a -1 during the last 1 Ma
(D'AGOSTINO et alii, 2001), and has continued during the
Holocene at a rate that has steadily dropped along the W-E
direction. The geodynamic processes driving the active tectonics
of the outer zones of the Northern Apennines are still strongly
debated, especially concerning the activity of the compressional
front (WEGMANN & PAZZAGLIA, 2009 and references therein).
The northern Marche trunk valleys have at least four flights of
alluvial terraces, whose deposits range in age from Middle
Pleistocene to Upper Pleistocene-Lower Holocene, named,
respectively, from the oldest and highest one as T1A, T1B, T2 and
T3 (NESCI et alii, 1990, 1995; FANUCCI et alii, 1996). This
_________________________
(*) Dipartimento di Scienze della Terra, Università degli Studi di Roma “La
Sapienza”, marta.dellaseta@uniroma1.it
(**) Dipartimento di Scienze dell’Uomo, della Natura e dell’Ambiente,
Università di Urbino “Carlo Bo”, francesco.troiani@uniurb.it
MARTA DELLA SETA (*) & FRANCESCO TROIANI (**)
661
terrace sequence is widely considered as being the result of
several complex, and for the most part climate-driven aggradation
episodes alternating with complex stages of climate- and tectonicdriven
stream downcutting (NESCI et alii, 1995; WEGMANN &
PAZZAGLIA, 2009). Close to the present coastline, at the
lowermost valley reaches, the alluvial terraces often merge with
the coeval coastal terraces.
This works is aimed at improving the geostatistical approach
used in previous papers (DELLA SETA et alii, 2008) by integrating
the surface sampling technique. Moreover, we aim at developing
a method for evaluating the incision rates of some of the major
northern Marche rivers in their lower catchments during the late
Quaternary and to compare them to previously estimated uplift
rates.
RESULTS
DTM- and GPS-based geostatistical analysis provided the
original top-surfaces of fluvial-to-coastal terrace bodies at the
Metauro and Cesano river mouths. The geometrical setting of the
depositional bodies has been better defined and constrained
through the terrain analysis of the reconstructed surface (slope
angle, profile curvature, etc.).
In agreement with the geomorphological and
stratigraphical/sedimentological data, the results of the
geostatistical topographic analysis confirmed the presence of
well-formed high-relief coastal fans, Upper Pleistocene-Lower
Holocene in age, at the Metauro and Cesano river mouth areas.
Two distinct knick zones, highlighted by well-recognizable
bumps on the reconstructed depositional top surfaces of both the
Upper Pleistocene-Lower Holocene fluvial and coastal terrace,
reflect two different late Quaternary depositional events: i) the
first one related to a major cold aggradational phase; ii) the
second related to the coastal fan development during the
Holocene sea level rise, but yet under a relative sea level
lowstand. Such data and reconstructions provided new findings
that led us to be inclined towards a climate-driven interpretation
of the above-mentioned morphological perturbations, previously
interpreted as the being of neotectonic origin (VANNOLI et alii,
2004).
The height distribution of the alluvial terrace sequences
SESSIONE 20

SESSIONE 20
exposed along the coastal sector of the major rivers of northern
Marche was correlated with the Quaternary climatic curve, in
order to obtain Height-Age diagrams for estimating the average
long-term fluvial incision rates for this area.
The obtained average incision rate of 0.20 mm a -1 over the
late Middle Pleistocene-Early Holocene time interval (between
terraces T2 and T3) is comparable to the uplift rate (0.13-0.18 mm
a -1 ) that we had previously calculated from the height difference
between the fluvial to coastal plains switch points on the
reconstructed top surfaces of diachronic coastal fans. Moreover,
the Height-Age plots of the alluvial terrace sequences highlighted
the different fluvial incision rates in adjacent valleys, which could
be related, at least in part, to differential crustal uplift that has
affected the coastal sector of the northern Marche Apennine at
least since the Middle Pleistocene (BORRACCINI et alii, 2002; DI
BUCCI et alii, 2003).
REFERENCES
BORRACCINI F., DE DONATIS M., DI BUCCI D., MAZZOLI S.,
MEGNA A., NESCI O., SANTINI S., SAVELLI D., TRAMONTANA
M. & TRIGGIANI P. (2002). Analisi della tettonica quaternaria
nel basso bacino del Fiume Metauro (Marche settentrionali)
e nell’adiacente offshore adriatico attraverso l’integrazione
di dati sismici, geomorfologici, stratigrafici e strutturali.
Studi Geol. Camerti (Nuova Serie) 2, 29-43.
BURBANK D.W. & ANDERSON R.S. (2001) - Tectonic
Geomorphology. Blackwell Science, Oxford.
DELLA SETA M., DEL MONTE M., FREDI P., MICCADEI E., NESCI
O., PAMBIANCHI G., PIACENTINI T., TROIANI F. (2008) -
Morphotectonic evolution of the Adriatic piedmont of the
Apennines: an advancement.in the knowledge of the Marche-
Abruzzo border area. Geomorphology, 102, 119-129.
D'AGOSTINO N., JACKSON J.A., DRAMIS F. & FUNICIELLO R.
(2001). - Interactions between mantle upwelling, drainage
evolution and active normal faulting: an example from the
central Apennines (Italy). Geophys. J. Int., 147, 475-497.
DI BUCCI D., MAZZOLI S., NESCI O., SAVELLI D., TRAMONTANA
M., DE DONATIS M. & BORRACCINI F. (2003). Active
deformation in the frontal part of the Northern Apennines:
insights from the lower Metauro River basin area (northern
Marche, Italy) and adjacent Adriatic off-shore. J. Geodyn.,
36, 213-238.
FANUCCI F., MORETTI E., NESCI O., SAVELLI D. & VENERI F.
(1996) - Tipologia dei terrazzi vallivi ed evoluzione del
rilievo nel versante adriatico dell'Appennino centrosettentrionale.
Il Quaternario, 9, 255-258.
662
NESCI O., SAVELLI D. & MENGARELLI D. (1990) - I terrazzi
vallivi del 1° ordine nei bacini dei Fiumi Metauro e Foglia
(Appennino Marchigiano). Geogr. Fis. Din. Quat., 13, 63-73.
NESCI O., SAVELLI D., CALDERONI G., ELMI C. & VENERI F.
(1995) - Le antiche piane di fondovalle nell’Appennino Nord-
Marchigiano. In: G.B. Castiglioni and P.R. Federici (Eds.) -
Assetto Fisico e Problemi Ambientali delle Pianure Italiane.
Mem. Soc. Geogr. It., 53, 293-312.
VANNOLI P., BASILI R. & VALENSISE G. (2004) - New
geomorphic evidence for anticlinal growth driven by blindthrust
faulting along the northern Marche coastal belt (central
Italy). J. Seismol., 8, 297–312.
WEGMANN K.W. & PAZZAGLIA F.J. (2009) - Late Quaternary
fluvial terraces of the Romagna and Marche Apennines, Italy:
Climatic, lithologic, and tectonic controls on terrace genesis
in an active orogen. Quatern. Sci. Rev., 28, 137-165.

Thermochronological modeling of the western Lepontine Dome
Key words: Exhumation history, Lepontine Dome, numerical
modeling, thermochronology.
We present results of forward and inverse thermal numerical
modeling of thermochronological data from the western part of
the Lepontine Dome. We aim to establish the landscape evolution
and the tectonic history of the Central Alps over the last 10 Myrs.
The Lepontine Dome is a major core complex of the Central
Alps which is bounded in the westernmost part by the Simplon
fault, an extensional fault that influenced its exhumation over the
last 25-30 Ma (STECK &HUNZIKER, 1994, MANCKTELOW, 1985).
The forward modeling is achieved using PECUBE (BRAUN,
2003) and we inverted the data to obtain variable exhumation
rates using GLIDE (FOX et alii, 2010). PECUBE computes the
evolution of the thermal field in 3D, including the effects of
changing topography. GLIDE employs a formal linear inverse
procedure, based on the concept of a “closure temperature”, to
resolve spatial and temporal variations in exhumation rates.
The model parameters are well constrained by a dense suite of
(U-Th)/He in apatite and apatite fission track ages collected
through the Lepontine Dome along the Simplon railway tunnel,
and across the corresponding surface transect (PIGNALOSA et alii,
2010). The assumed scenario, based on the literature, is
decreasing topographic amplitude through time, with rock uplift
rate of the considered crustal block, increasing to the present.
Results from PECUBE suggest that: a) the activity on the
Simplon fault has not influenced the exhumation of the Lepontine
Dome over the last 10 Ma; b) between 5 Ma and today the relief
decreased, after the Messinian salinity crisis and during the onset
of the Northern hemisphere glaciations. Simulations indicate a
reasonable fit between modeled and measured temperatures
through the tunnel (SCHARDT, 1905), as do the derived surface
and tunnel ages.
________________________
(*) Department of Earth and Geo-Environmental Sciences, University of
Bologna, giorgio.difiore@gmail.com
(**) Geologisches Institut, ETH-Zentrum, Zürich, CH frederic@erdw.ethz.ch,
matthew.fox@erdw.ethz.ch
(°) Department of Geosciences, University of Padua,
massimiliano.zattin@unipd.it, matteo.massironi@unipd.it
Work made for the project TOPOALPS with the financial support of the
University of Bologna
GIORGIO DI FIORE (*), MATTHEW FOX (**), FREDERIC HERMAN (**),
MATTEO MASSIRONI (°) & MASSIMILIANO ZATTIN (°)
663
However, in the southern part of the section the temperatures
are overestimated. This could be due to water circulation along
extensional faults, which is not considered by the model (Fig. 1).
Fig. 2a shows that the modeled fission track ages profile is
younger than the observed one in its southern part. This
underestimation happens where the modeled temperature profile
showed in Fig. 1 is higher than the observed one. Age-elevation
relationship in Fig. 2b shows a vertical behavior of the modeled
data. Apatite (U-Th)/He show, in Fig. 2c-d, a good fit whith the
observed data. Fig. 2e-f show that tunnel data are overestimated
in many points of the profiles.
Results from GLIDE show an increasing exhumation rate
through the last 10 Ma, with higher exhumation rates in the
within the center of the Lepontine Dome.
Fig. 1 – Simulated temperature profile along the the Simplon railway tunnel (modified
from PIGNALOSA et et alii, 2010). The tunnel cuts cuts the the partial retention zone zone of of the the
Apatite Helium closure system, while it it is is about 2000 m m above the the fission track track
partial retention zone. In In the the lower part the the comparison between the the observed
temperatures during the tunnel drilling and and the the simulated temperatures using using
PECUBE is is shown (see the text for for comments).
CONCLUSIONS
Activity at the Simplon Fault is constrained by a dense suite
of thermochronometric ages, distributed in time and space.
Preliminary results suggest that activity on the Simplon Fault has
had no influence on the exhumation rate in the last 10 Ma.
Another important result is the evidence that major changes in
topography have taken place in the last 5 Ma, after the Messinian
SESSIONE 20

SESSIONE 20
Fig. 2 – Simulated thermochronological data compared to the observed ones. On the left are surface data. Fission tracks show a younger age for the southernmost part of
the dataset, while (U-Th)/He show a better fit. On the right panel are the tunnel age profiles, in both diagrams the simulated ages are older than the observed ones.
salinity crisis and during the Quaternary glaciations. In fact, for
this period, the most important topographic variations occurred
within the Central Alps, arguing a link between the latest climatic
changes and the morphological evolution of this part of the chain.
REFERENCES
BRAUN J. (2003) - Pecube: a new finite-element code to solve the
3D heat transport equation including the effect of a finite
amplitude surface topography - Comp. & Geosci. 29. 787-
794.
FOX M., HERMANN F. & WILLETT S. (2010) - The Inversion of
Low-Temperature Thermochronometry to Extract Spatially
Varying Exhumation Rates. Geoph. Res. Abs. 12. EGU2010-
11667, 2010 EGU General Assembly 2010.
MANCKTELOW N. S. (1985) - The Simplon Line: a major
displacement zone in the western Lepontine Alps. Eclog.
Geol. Helv. 78. 73–96.
PIGNALOSA A., ZATTIN M., MASSIRONI M. & CAVAZZA W. (2010)
- Thermochronological evidence for a late Pliocene climateinduced
erosion rate increase in the Alps. - Int. J. Earth Sci.,
99, DOI10.1007s00531-010-0510-9.
664
SCHARDT H. (1905) - Les résultats scientifiques du percement du
Tunnel du Simplon. Géologie - hydrologie – thermique. -
Bull. tec. de la Sui. rom. Tirage à part, 1-56.
STECK A. & HUNZICKER J. (1994) – The tertiary structural and
thermal evolution of the Central Alps – Compressional and
extensional structures in an orogenic belt. Tectonophysics,
254, 229-254.

Dynamic Topography and microplate motion in the Mediterranean
Key words: Dynamic topography, seismic tomography,
subduction.
Mobile belts are long-lived deformation zones composed of
an ensemble of crustal fragments, distributed over hundreds of
kilometers inside continental convergent margins.
The Mediterranean represents a remarkable example of this
tectonic setting: the region hosts a diffuse boundary between the
Nubia and Eurasia plates comprised of a mosaic of microplates
that move and deform independently from the overall plate
convergence.
Surface expressions of Mediterranean tectonics include deep,
subsiding backarc basins, intraplate plateaux and uplifting
orogenic belts.
Although the kinematics of the area are now fairly well
defined, the dynamical origins of many of these active features
are controversial and usually attributed to crustal and lithospheric
interactions.
However, the effects of mantle convection, well established
for continental interiors, are expected to be particularly relevant
in a mobile belt, and modeling may constrain important
parameters such as slab coherence and lithospheric strength.
Here, we compute global mantle flow based on recent, highresolution
seismic tomography, to investigate the role of
buoyancy-driven and plate-motion induced mantle circulation for
the Mediterranean.
We show that mantle flow provides an explanation for much
of the observed dynamic topography and microplate motion in
the region.
More generally, vigorous small-scale convection in the
uppermost mantle may also hold the key for understanding other
complex mobile belts such as the North American Cordillera or
the Himalayan-Tibetan collision zone.
_________________________
(*) Dipartimento di Scienze Geologiche, Università Roma Tre,
faccenna@uniroma3.it
(**) Department of Earth and Planetary Sciences, Harvard University,
Cambridge, MA, USA
CLAUDIO FACCENNA (*) & THORSTEN W. BECKER (**)
665
SESSIONE 20

SESSIONE 20
Spatial extent of vertical tectonic motions in northern Sicily using
Holocene and Last Interglacial sea level markers: a case study
between Acquedolci and Capo d’Orlando.
MAURIZIO GASPARO MORTICELLI (*), VALERIA LO PRESTI (*), FABRIZIO ANTONIOLI (**) , CARMELO MONACO (°),
ATTILIO SULLI (*) & AGNESE ZUCCARELLO (°°)
Key words: Marine terraces, Sicily, vertical movements.
Vertical position of sea-level, related deposits and
morphologies (e.g., last interglacial, LIG, 125 ka,) provide useful
markers to utilize with this purpose (LAMBECK et alii, 2004;
FERRANTI et alii, 2006, ANTONIOLI et alii, 2009). Using
published (ANTONIOLI et alii, 2006) and new data we provide a
review of the northern coast of Sicily uplift rates. The markers
used in this study are: terraces inner margin, tidal notches, etc.,
and, for the last millennia archaeological markers and fossil
beaches and vermetid reef.
Data on vertical movements calculated for the coastal area
developing in the north-Sicilian continental margin indicate that,
from East to West, a strong variation of vertical rates of uplift are
recognized during both middle-late Pleistocene and Holocene.
Uplift rates derived from the LIG markers decrease from east to
west from 0.8 mm\yrs (Messina) to 0.2 mm\yrs (Cefalù) The
same trend is observed for Holocene markers showing rates still
higher (until 2 mm\yrs) than in the LIG. The variations mainly
correspond to coastal segments separated by a main regional
tectonic feature, the Vulcano-Tindari Fault system (LANZAFAME
& BOUSQUET, 1997; BILLI et alii, 2006) with predominantly
right-lateral transcurrent (partly extensional and/or contractional)
kinematics that dissects transversally the south-western sector of
the Calabrian Arc. These structures, which are sub-vertical, crosscut
the whole lithosphere and therefore can act as discontinuities
separating crustal blocks characterized by different vertical
motion.
Here we focus our attention on the eastern sector of the
Sicilian northern coast and particularly the area immediately to
the west of the Vulcano-Tindari fault system, where several
evidences of vertical movements during the Pleistocene-Holocene
666
have been recognized. Here, the occurrence of several oblique
and normal fault segments and the alternation of rocks with
different competence, that is the Hercynian metamorphic
basement, its Meso-Cenozoic carbonate and Oligocene-Miocene
terrigenous cover and Pleistocene deltaic sands and gravels
(CARBONE et alii, 1998), determine a complex geomorphologic
setting. Our analysis was devoted to the coastal sector from Capo
d'Orlando to Acquedolci towns, where a well preserved flight of
marine terraces occurs.
Geomorphologic survey allowed to recognize four orders of
marine terraces located at elevations of 200 m, 120-90 m, 60-40
m, and 35-10 m a.s.l.. At Rocca Scodoni, between Acquedolci
and Capo d’Orlando, the terrace located between 40 m and 60 m
is characterized by the presence of a marine deposit up to 10 m
thick, constituted by coarse polygenic conglomerates,
microconglomerates and cross-laminated sands in a finingupward
sequence. Here, the inner margin of the terrace has been
recognized between 45 m and 50 m a.s.l. and it is constituted by a
cliff showing several Lithodomus holes, sometimes preserving
fossilized shell inside, and other biological remains. A shell of
Spondylus s.p. (Fig. 1) in physiologic position has been collected
from this terraced deposit at Rocca Scodonì (Fig. 2) in order to
perform geochronological analyses.
The preliminary U/Th analysis on Spondylus shell, provides
_________________________
(*) Dipartimento di Geologie e
mgasparo@unipa.it.
Geodesia, Università di Palermo,
(**) ENEA, Casaccia, Roma., fabrizio.antonioli@enea.it.
(°) Dipartimento di Scienze Geologiche, Università di Catania,
cmonaco@unict.it.
(°°) Dipartimento di Fisica e Astronomia, Università di Catania. Fig. 1 – The insitu Spondylus of Rocca Scodoni (see Fig. 2).

an age (with large error bar) on MIS 5 (between 100 and 125 ka).
Based on the eustatic level for Mediterranean sea during Last
Interglacial (6 metres ± 3), the altitude of the inner margin (50 m)
we estimate the tectonic uplift rate between 0.36-0.5 mm/a.
Archaeological markers occurring along the coastal area located a
few kilometers east of Rocca Scodonì suggest similar tectonic
uplift rates for the Holocene.
The new chronological data allow us to calibrate, with respect
to the Stage 5, the distribution of marine terraces recognized in
this coastal area at different altitudes.
Fig. 2 – Geomorphological map of Rocca Scodoni outcrop.
REFERENCES
ANTONIOLI F., KERSHAW S., RENDA P., RUST D., BELLUOMINI G.,
RADTKE U. & SILENZI S., (2006) - Altitude of the last
interglacial highstand in Sicily (Italy) and its implications for
tectonic. Quatern. Int., 145–146, 3–18.
ANTONIOLI F., FERRANTI L., FONTANA A., AMOROSI A., M.,
BONDESAN A, BRAITENBERG C., DUTTON A., FONTOLAN G.,
FURLANI S., LAMBECK K., MASTRONUZZI G., MONACO, C.,
SPADA G. & STOCCHI P. (2009) - A review of the Holocene
sea-level changes and tectonic movements along the Italian
coastline. Quatern. Int., 206, 102-133.
BILLI A., BARBERI G., FACCENNA C., NERI G., PEPE F. & SULLI A.
(2006) - Tectonics and seismicity of the Tindary Fault System,
southern Italy: crustal deformations at the transition between
ongoing contractional and extensional domains located
above the edge of a subducting slab. Tectonics, 25, 1–20.
667
BONFIGLIO L., MANGANO G. & PINO P. (2010) - The contribution
of mammal bearing deposits to timing late Pleistocene
tectonics of cape Tyndari. Riv. It Pal. Strat., 116, 1-16.
CARBONE S., LENTINI F. & VINCI G. (1998) - Carta geologica
del settore occidentale dei Monti Peloritani (Sicilia nordorientale).
S.EL.CA., Firenze.
FERRANTI L., ANTONIOLI F., AMOROSI A., DAI PRÀ G.,
MASTRONUZZI G., MAUZ B., MONACO C., ORRÙ P.,
PAPPALARDO M., RADTKE U., RENDA P., ROMANO P., SANSÒ
P. & VERRUBBI V. (2006) - Elevation of the last interglacial
highstand in Italy: A benchmark of coastal tectonics.
Quatern. Int., 145–146, 30–54.
LAMBECK K., ANTONIOLI F., PURCELL A. & SILENZI S., (2004) -
Sea level change along the Italian coast for the past 10,000
yrs. Quatern. Sci. Rev., 23, 1567-1598.
LANZAFAME G. & BOUSQUET J.C. (1997) - The Maltese
escarpment and its extension from Mt. Etna to the Aeolian
Islands (Sicily): importance and evolution of a lithosphere
discontinuity. Acta Vulcanol., 9, 113–120.
SESSIONE 20

SESSIONE 20
Landslide volumes and evaluation of landslide mobilization rates in
an area in Umbria, central Apennines
Key words: Central Apennines, erosion, landslide, mobilization
rate.
INTRODUCTION
Landslides are common geomorphological processes that
contribute to shape landscapes in all continents. To determine
erosion rates in landscapes dominated by slope wasting
processes, chiefly landslides, one needs to know: (i) the
geographical distribution and abundance of landslides, (ii) the
temporal frequency or the average landslide mobilization rates,
and (iii) the volume of material mobilized by individual
landslides. Information on landslide abundance and frequency
can be obtained from multi-temporal landslide inventory maps,
which can be prepared through the systematic interpretation of
multiple sets of stereoscopic aerial photographs, high and veryhigh
resolution, mono- and stereoscopic satellite images, and
dedicated field campaigns executed after events that have
resulted in landslides (event landslide inventory maps)
(MALAMUD et alii, 2004; GALLI et alii, 2008).
Determining the volume of a single landslide is a complex
problem that requires information on the surface and subsurface
geometry of the slope failures, which is difficult to obtain.
Deciding the volume of individual landslides in a large
population of failures comprising hundreds or thousands of
landslides is an even more difficult task (MALAMUD et alii, 2004)
that, at present, can only be achieved adopting empirical
relationships to link the volume (VL) of a landslide to geometrical
measures of the slope failure, chiefly landslide area (AL)
(SIMONETT, 1967; RICE et alii, 1969; INNES, 1983; HOVIUS et
alii, 1997; GUTHRIE &EVANS, 2004; KORUP, 2005; TEN BRINK et
alii, 2006; IMAIZUMI &SIDLE, 2007; GUZZETTI et alii, 2008,
2009; IMAIZUMI et alii, 2008).
_________________________
FAUSTO GUZZETTI (*), FEDERICA FIORUCCI (**), FRANCESCA ARDIZZONE (*), MAURO CARDINALI (*),
MAURO ROSSI (*), ALESSANDRO CESARE MONDINI (*) (**), PAOLA REICHENBACH (*),
MICHELE SANTANGELO (*) & DANIELA VALIGI (**)
(*) CNR IRPI, f.guzzetti@irpi.cnr.it
(**) Università degli Studi di Perugia, valigi@unipg.it
668
LANDSLIDE VOLUME
From a global catalogue of 5800 mass movements for which
landslide area (AL) and volume (VL) are known independently,
we selected 677 landslides of the slide type (CRUDEN &VARNES,
1996), and we used the geometrical measurements to define an
empirical relationship to link AL (in m 2 ) to VL (in m 3 ). The
relationship takes the form of a power law with a scaling
exponent a = 1.450 (standard error = 0.0086), and holds for eight
orders of magnitude of AL and twelve orders of magnitude of VL,
and is in good agreement with similar relationships in the
literature (SIMONETT, 1967; RICE et alii, 1969; INNES, 1983;
HOVIUS et alii, 1997; GUTHRIE &EVANS, 2004; KORUP, 2005;
TEN BRINK et alii, 2006; IMAIZUMI &SIDLE, 2007; GUZZETTI et
alii, 2008; IMAIZUMI et alii, 2008).
The limited dispersion of the empirical data around the power
law equation VL = 0.074 AL 1.450 (R 2 = 0.971), and the observation
that the landslides occurred in different geological settings and
climatic environments, and were caused by different triggers
(chiefly rainfall and earthquakes), suggest that the dependency of
VL on AL is independent of the physiographical setting,
essentially.
LANDSLIDE MOBILIZATION RATES
We used the empirical relationship discussed in the previous
section to determine the volume of landslide material (landslides
of the slide type) in the Collazzone area, central Umbria,
extending for 78.9 km 2 , and for which a detailed multi-temporal
landslide inventory covering the period 1937-2005 is available.
In this 69-year period, the total volume of landslide material was
determined VLT = 4.78×10 7 m 3 , corresponding to an average
mobilization rate f L = 8.8 mm∙yr -1 .
In the period 1937-2005, landslides mapped in the multitemporal
inventory range in volume VL from 1.3×10 1 m 3 to
8.7×10 5 m 3 , with the most abundant landslides in the range 5×10 1
m 3 < VL < 3×10 2 m 3 . In the multi-temporal inventory, the seven
landslides with the largest volume (0.3% of the total number of
landslides) represent 10% of the total landslide volume, and 4%
of the total landslide area; and the 110 landslides with the largest

volume (5.5% of the total number of landslides) represent 50% of
the total landslide volume, and 32% of the total landslide area.
These figures confirm the importance of large volume landslides
in controlling the total volume of mobilized landslide material in
an area (HOVIUS et alii, 1997; GUZZETTI et alii, 2008, 2009).
Using the temporal information in the multi-temporal
inventory, we determined the volume of material mobilized by
new landslides and reactivations, for different periods. A period
of accelerated landslide activity was singled out between 1937
and 1941. In this 5-year period, slope failures mobilized a
volume of landslide material equivalent approximately to 45% of
the total landslide volume mobilized in the 69-year period 1937-
2005. This corresponds to a mobilization rate in the 5-year period
f L = 54 mm∙yr -1 , six times larger than the long-term average
mobilization rate in the period 1937-2005.
Even excluding the period 1937-1941, the majority of the
landslide material was mobilized during specific landslide events,
or particularly active landslide periods. Landslide mobilization
rates during landslide events, or periods, are 9 to 11 times larger
than the average rates for the inter-periods.
MAGNITUDE OF LANDSLIDE EVENTS
In the literature, we do not have an accepted definition for the
magnitude of a landslide event (MALAMUD et alii, 2004). We
defined the magnitude of a landslide event (or period) mL as the
logarithm (base 10) of the total volume of landslide material
mobilized during the event (or period), mL = log10(VLT). Based on
this definition, an event that has resulted in 1×10 5 m 3 of landslide
material is a magnitude 5 event, and a period during which 1×10 6
m 3 of landslide material were mobilized, is a magnitude 6 period.
Using this scale, the period of augmented landslide activity
between 1937 and 1941 has mL = 7.3.
CONCLUSIONS
The results obtained in the Collazzone area, central Umbria,
are relevant for the definition of landslide hazard and the
assessment of landslide risk, and for an improved understanding
of the evolution of landscapes dominated by landslides in central
Italy.
REFERENCES
CRUDEN D.M. & VARNES D.J. (1996) - Landslide types and
processes. In: A.K., Turner, R.L., Schuster (Eds.) -
Landslides, Investigation and Mitigation, Transportation
Research Board Special Report 247, Washington D.C., 36-75.
GALLI M., ARDIZZONE F., CARDINALI M., GUZZETTI F. &
REICHENBACH P. (2008) - Comparing landslide inventory
maps. Geomorphology, 94, 268-289.
669
GUZZETTI F., ARDIZZONE F., CARDINALI M., ROSSI M. & VALIGI
D. (2009) - Landslide volumes and landslide mobilization
rates in Umbria, central Italy. Earth Planet. Sci. Lett., 279,
222-229.
GUTHRIE R.H. & EVANS, S.G. (2004) - Analysis of landslide
frequencies and characteristics in a natural system, coastal
British Columbia. Earth Surf. Proc. Land., 29, 1321-1339.
GUZZETTI F., ARDIZZONE F., CARDINALI M., GALLI M.,
REICHENBACH P. & ROSSI M. (2008) - Distribution of
landslides in the Upper Tiber River basin, central Italy.
Geomorphology, 96, 105-122.
GUZZETTI F., GALLI M. REICHENBACH P., ARDIZZONE F. &
CARDINALI M. (2006) - Landslide hazard assessment in the
Collazzone area, Umbria, central Italy. Nat. Hazards Earth
Sys. Sci., 6, 115-131.
HOVIUS N., STARK C.P. & ALLEN P.A. (1997) - Sediment flux
from a mountain belt derived by landslide mapping. Geology,
25, 231-234.
IMAIZUMI F. & SIDLE R.C. (2007) - Linkage of sediment supply
and transport processes in Miyagawa Dam catchment, Japan.
J. Geophys. Res., 112, F03012.
IMAIZUMI F., SIDLE R.C. & KAMEI R. (2008) - Effects of forest
harvesting on the occurrence of landslides and debris flows
in steep terrain of central Japan. Earth Surf. Proc. Land., 33,
827-840.
INNES, J.N. (1983) - Lichenometric dating of debris-flow deposits
in the Scottish Highlands. Earth Surf. Proc. Land., 8, 579-588.
MALAMUD B.D., TURCOTTE D.L., GUZZETTI F. & REICHENBACH
P. (2004) - Landslide inventories and their statistical
properties. Earth Surf. Proc. Land., 29, 687-711.
RICE R.M., CORBETT E.S. & BAILEY R.G. (1969) - Soil slips
related to vegetation, topography, and soil in Southern
California. Water Resour. Res., 5, 647-659.
SIMONETT D.S. (1967) - Landslide distribution and earthquakes
in the Bewani and Torricelli Mountains, New Guinea. In: J.N.
Jennings and J.A. Mabbutt (Eds.) - Landform Studies from
Australia and New Guinea, Cambridge University Press,
Cambridge, 64-84.
TEN BRINK U.S., GEIST E.L. & ANDREWS B.D. (2006) - Size
distribution of submarine landslides and its implication to
tsunami hazard in Puerto Rico. Geophys. Res. Lett., 33,
L11307.
SESSIONE 20

SESSIONE 20
Key words: Holocene, Sicily, sea level rise, tectonics.
VALERIA LO PRESTI (*), MAURIZIO GASPARO MORTICELLI (*), FABRIZIO ANTONIOLI (**),
ATTILIO SULLI (*) & RAIMONDO CATALANO (*)
The north-eastern Sicily coast reflects the effects of Holocene
active tectonics associated to subduction system of Ionian crust
beneath the Calabrian arc (CAPUTO et alii, 1970; WESTAWAY,
1993, DOGLIONI et alii, 1999). The latter, characterized by a stack
of crystalline rock and its sedimentary cover, is the highest
structural element in the Sicily chain.
The Calabrian arc is a region that records one of the major
Quaternary vertical tectonic movement in the whole
Mediterranean basin. This uplift, well documented from Last
Interglacial, is expressed as vertical variation of the height of the
Quaternary marine terraces inner margin that characterize the
north-eastern Sicily coast. The uplift can be divided into a
"continuous" regional component and in an "episodic"coseismic
component (FERRANTI et alii, 2007). The northwest Sicily coast
shows as the uplift rates estimated for the Holocene have values
greater than those estimated at the same point from Last
Interglacial (ANTONIOLI et alii, 2006). At the regional scale it is
Fig. 1 – The marine conglomerate containing fossils.
_________________________
(*) Dipartimento di Geologia e Geodesia, Università di Palermo,
valeria.lopresti@unipa.it.
(**) ENEA, Casaccia, Roma.
The Brolo Island, a lentil in the “Ocean”
670
possible to observe a decrease in uplift rates from Cape Peloro
(1.1 mm / year) to Palermo and Capo S. Vito (stable).
In north-eastern Sicily, between Capo d'Orlando and Capo
Calavà, we studied the Brolo Stack, located in the central part of
a small bay along the coast facing Brolo village. This area
pertains to the northwestern sector of Peloritani Mountains
(western portion of the Calabrian arc), which extend in E-W
direction from Messina Straits to S. Agata di Militello village. In
particular the tectonic style is characterized by tectonically
overlapping bodies, generally dipping toward the northern
quadrants.
The Brolo coastal area is characterized by a wide coastal
alluvial plain fed by two big rivers. On this plain rises a
metamorphic salient, a sub-circular cylindrical structure, about 50
m high, placed inshore at 250 m from the coastline.
In particular, the Brolo Stack is an outcrop of a residual block
of impure, medium grain, marble interspersed with Paleozoic
paragneiss and mica schists, which largely outcrops in the
hinterland. These lithotypes are the crystalline substrate on which
develops the current depositional sequence. The Brolo Stack
constitutes a "lentil" of metamorphic rock emerging above the
14-18 m deep seafloor at 450 m from the coastline.
The objective of this study is to calculate the potential vertical
movements and assume when they could have occurred. To do
this a detailed geomorphological subaerial and an underwater
survey were conducted, which led to discovery a fossils bearing
conglomerate (Fig. 1), in protected trays at 3.5 m from sea level,
Fig. 2 – Uplifted lithophaga holes.

and well preserved lithophaga holes (Fig. 2) at about 70 cm from
sea level.
The Brolo stack show a particular morphological feature,
different in the emerged and submerged parts (Fig. 3). The
emerged portion strikes along the E-W trend for a length of about
43 m, being 29 m wide and about 15 m high. It has a mushroom
shape with the submerged part more closely than the emerged, the
result of combined physical and chemical processes triggered by
both sea level rise and tectonic vertical movements.
Fig. 3 – The mushroom shape of the submerged portion of Brolo island.
A system of schistosity gives to the white-to-gray stack an
apparent stratification organized in decimetric beds with lying
005/60°. The whole structure is fractured along multiple
directions often containing dark poorly consolidated volcanic
rock.
Large angular blocks are found on the seabed at the base of
the submerged cliffs; their collapse is the result of mechanical
erosion due to the high energy waves and the schistosity and
intensely fractured structure of the rocks.
The underwater survey allowed us to recognize little terraces
at different depth recognized as structural surfaces. We used
radiocarbon analysis on a gastropod found in the marine
conglomerate (Fig. 4). We provide an age of 4745 +/- 59, ( 4965
years +-70 cal BP using Calib 5 program, STUIVER et alii, 2005).
Based on the data obtained and morphological considerations,
it is difficult to envisage the formation of this beach deposit on
the stack if we do not consider a very different morphological
feature, probably more flared with greater lateral continuity and
less inclined slopes.
If we compare the age of the deposit and the height that was
found with the predicted local sea level curves, this is above the
curve, indicating a uplift rate about 1.5 mm / years that is higher
than that calculated in the same field for last interglacial.
671
Fig.4 – Gastropod found in the marine conglomerate.
REFERENCES
ANTONIOLI F., ANZIDEI M., LAMBECK K., AURIEMMA R., GADDI
D., FURLANI S., ORRÙ P., SOLINAS E., GASPARI A., KARINJA
S., KOVACIC V. & SURACE, L. (2007) - Sea level change
during the Holocene in Sardinia and in the North-eastern
Adriatic (Central Mediterranean sea) from archaeological
and geomorphological data. Quatern. Sci. Rev., 26, 2463–
2486.
CAPUTO M., PANZA G.F. & POSTPISCHL D. (1970) - Deepapple
structure of the Mediterranean basin. J. Geophys. Res., 75,
4919-4923.
DOGLIONI C., HARABAGLIA P., MERLINI S., MONGELLI F.,
PECCERILLO A. & PIROMALLO C. (1999) - Orogens and slab
vs their direction of subduction. Earth Sci. Rev., 45, 167-208.
FERRANTI L., MONACO C., ANTONIOLI F., MASCHIO L., KERSHAW
S. & VERRUBBI V. (2007) - The contribution of regional uplift
and coseismic slip to the vertical crustal motion in the
Messina Straits, Southern Italy: evidence from raised Late
Holocene shorelines. J. Geophys. Res., 112, B06401, DOI:
10.1029/2006JB004473.
STUIVER M., REIMER P.J. & REIMER R. (2005) - CALIB
Radiocarbon Calibration, execute version 5.0.2 html.
http://calib.qub.ac.uk/calib.
WESTAWAY, R. (1993) - Quaternary uplift of Southern Italy. J.
Geophys. Res., 98 (B12), 21741-21772.
SESSIONE 20

SESSIONE 20
Key words: Carpathians, mantle dynamics, morphometry,
tectonic geomorphology, topography.
INTRODUCTION
Tectonic processes and dynamic mantle flow impart a unique
imprint on topography and geomorphic responses over time
scales of 10 4 to 10 6 yr. So first-order topographic features in a
tectonically active landscape including relief, drainage patterns,
watershed location, and stream gradient slope represent ways to
quantitatively characterize the interaction between crustal
tectonics, mantle dynamics, and geomorphology, providing a
basis for modeling landscape evolution. We analyzed the
topographic features of the Romanian Carpathians, a mountain
range characterized by two straight segments connected by a
narrow curvature zone (Fig. 1). Since late Cretaceous, the
deformation history of Carpathians includes three phases that
progressively affected the southern segment, the eastern one, and
finally the curvature zone. This is mirrored in the fission tracks
data that record not only an older exhumation in the southern
Carpathians, but also a progressively younger one from north to
south in the eastern portion of the chain.
DATA AND DISCUSSION
We examined the tectonic geomorphology of the Romanian
Carpathians focusing on regional and local topographic settings,
drainage pattern and stream long profiles. Our main data base is
composed of DEM-based topographic analysis, supplemented
with field investigations in the Slanic R. basin, a drainage located
in the Carpathian curvature (Fig. 1).
The longitudinal profiles of streams draining the southern
_________________________
The topography of the Romanian Carpathians: the interaction of
mantle dynamics, crustal tectonics and surface processes
PAOLA MOLIN (*), SIMONE SPERINI (*), VALENTINA N. SCOTTI (*) & FLOARE GRECU (**)
(*) Dipartimento di Scienze Geologiche, Università degli Studi Roma Tre,
p.molin@uniroma3.it.
(**) Faculty of Geography, Bucharest University.
This work represents the result of a collaborative contribution to an
agreement on research and teaching between Dipartimento di Scienze
Geologiche, Università degli Studi Roma Tre and Faculty of Geography,
Bucharest University.
672
Carpathians are more concave and characterized by knickpoints
generated by changes in rock-type. Their profiles more close to
the equilibrium shape well fit with the older emersion of the
chain. The longitudinal profiles of the streams draining the
eastern Carpathians and the curvature are less concave,
presenting a knickpoint at 500-600 m of elevation that records a
regressive erosion wave produced by a regional change in base
level. Upstream, in some longitudinal profiles, a second
knickpoint indicates fluvial capture phenomena at least partially
driven by the back-arc extensional tectonics.
Fig. 1 – The topography of the Romanian Carpathians. The study streams and
the location of the area investigated on the field are included.
Filtering the topography at different wavelengths, we
observed a relative depression in correspondence with the
Carpathian curvature, where mantle seismicity data indicate a
narrow but still active Wadati-Benioff zone. On the contrary, in
correspondence with the Transylvanian extensional basin, the
filtered topography presents a relief. In the same location,
tomography data show a low velocity area, interpreted as an
upwelling of hot asthenospheric material. On this basis, we
hypothesized that local mantle convection dynamically supports
the generation of a topographic “high” in the Transylvanian basin

and of a depression in the Carpathians curvature.
In the Slanic River basin (Fig. 2), we surveyed four orders of
strath terraces and low relief upland surfaces located on
interfluves and interpreted as relicts of an old landscape. The
projection of terrace elevation on the Slanic R. longitudinal
profile shows a downstream diverging pattern, that suggests an
increase of the uplift rate towards the mountain front. A 14 C
dating of a bone found in a forth order terrace close to the
mountain front allow us to calculate a Holocene incision rate of
1.4 mm/yr. This values coincides exactly with the uplift rate
obtained by the GPS data on vertical movement in the very same
area of the mountain front, where is located the regional buried
structure called “Peri-Carpathians Thrust”.
Fig. 2 – First order terrace close to Sirbesti village. The unconformity on the
underlying bedrock and the boundary between gravel and sand in the terrace
deposits are reported.
CONCLUSION
The obtained results are consistent with a landscape
dominated by a regional diachronous and differential uplift
superimposed on crustal tectonics, extensional on the internal
side and compressive on the external one. The differential uplift
of the Romanian Carpathians influenced the chain topography, its
local relief, the shape of stream long profiles, the formation and
pattern of strath terraces. Moreover, crustal tectonics dominated
the hydrographic net organization and induced river captures in
the axial sector of the chain.
In correspondence with the Carpathians curvature and the
Transylvanian basin, mantle flow driven by the subducting slab
produced a respectively negative and positive dynamic
topography.
673
SESSIONE 20

SESSIONE 20
Key words: Calabria, dating, depositional terraces.
Twelve samples of the coastal depositional sequence from a
marine terrace preserved along the Ionian coast of Northern
Calabria (Fig. 1) were collected to assess their exposure age using
in situ produced 36 Cl cosmonuclide. This region is located on the
northeastern tip of the Calabrian Arc, which experienced rapid
Late Quaternary uplift due to a combination of lithospheric and
crustal processes. Consequently, a spectacular flight of marine
terraces is preserved along the coast, as a result of the
combination between glacio-hydro-isostatic Quaternary cycles
and tectonic uplift. Difficulty in relative dating of terraces arises
from the absence of ‘‘Senegalaise fauna’’ assemblage, and
specifically of Strombus bubonius specimens, which are
indicative of the MIS 5.5 in the Mediterranean area (FERRANTI et
alii,, 2006). Also absolute ages were not resolute (CUCCI, 2004;
FERRANTI et alii,, 2009; SANTORO et alii, 2009). Based on the
poor chronological constraints on marine terrace ages, different
uplift rate estimates were proposed varying from ~1 to ~2 mm/yr
(CUCCI &CINTI, 1998; CUCCI, 2004; SANTORO et alii, 2009;
CAPUTO et alii, 2010).
We used the cosmogenic nuclide exposure method to improve
the marine terraces chronology. The cosmogenic nuclides ( 3 He,
21 26 36 14
Ne, 10Be, Al, Cl, C), also called terrestrial in situ
cosmogenic nuclides (TCNs), stable or radioactive, derive from
the interaction between cosmic rays of extra-terrestrial origin
(electrically charged particles, between which the more abundant
are protons and a-particles) and minerals present in the first
meters of the lithosphere. The maximum TCNs concentration is
time-dependent being linked to: a) exposure age; b) erosion rates;
c) radioactive cosmogenic nuclides half-life. Principal factors that
can influence the TCNs production rates are: a) sample chemical
composition; b) latitude, since the cosmic flux particles are
deflected by the earth magnetic field; c) elevation, due to the flux
interaction and consequent loss of energy with the atmosphere; d)
shielding of the cosmic flux by surrounding mountain peaks; e)
_________________________
Dating marine depositional terraces along the Ionian coast of
Northern Calabria with 36 Cl surface exposure dating
ENRICO SANTORO (*), LUIGI FERRANTI (**), CARMELO MONACO (*) & LUCILLA BENEDETTI (°)
(*) Dipartimento di Scienze Geologiche, Università degli Studi di Catania,
enrico.santoro@hotmail.it.
(**) Dipartimento di Scienze della Terra, Università degli Studi di Napoli
“Federico II”
(°) CEREGE – UMR CNRS, Université Aix-Marseille, IRD, France
674
geometry of the surface; f) soil and sample thickness, g) density
of the sample.
Between the different TCNs, we used the 36 Cl (half-life: 301
ka) that is principally produced by the calcium, potassium and
Fig. 1 – a) Samples position and river incision index map; b) study area
geographic position (grey rectangle).
chlorine atoms through various production pathways (STONE et
alii, 1996; SCHIMMELPFENNIG et alii, 2009) mainly concentrated
in the first three meters of the lithosphere, decreasing
exponentially with depth.
We sampled four different remnants of a marine terrace (T4 in
Fig. 1, following SANTORO et alii, 2009 nomenclature) preserved
along the Pollino coastal sector. This terrace, which has an
average inner margin elevation of 114 m, was previously
attributed to the MIS 5.5 (124 Ka) based on ESR (FERRANTI et
alii, 2009) and amino acid racemization (CUCCI, 2004) dating.
The four sampled marine terraces are characterized by a constant
35 m thick coastal deposit and, based on sedimentological
analysis (SANTORO et alii, 2009), it was not affected by
significant erosion. However, to better understand the erosion
processes that have interested the marine terraces surfaces, five
different superficial samples were collected along the upper level
of the fluvial-coastal depositional sequence (transitional
conglomerates between beach and river systems). Generally, we
preferred to collect the samples close to the terrace inner margin
(Fig. 1), being the outer margin of the terrace more exposed to

erosional processes, above all during the marine transgression
related to the lower terrace. However, the samples CLJ1/2/6 were
collected close to the outer margin (after checking the integrity of
the depositional sequence) because the presence of thick colluvial
covers (~10 m) in the inner margin area that can shield the
deposit from the cosmic ray flux and greatly influence the TCNs
production rates. Besides, seven samples were collected, at a
distance of 50 cm along a depth profile, 3 m high, to obtain the
36 Cl depth distribution and, through comparisons with theoretical
depth distributions yield both exposure age and erosion rates as
well as a possible inherited 36 Cl component, derived from the predepositional
history of the sampled material and assumed to be
equal to the 36 Cl concentrations in the deepest part of the depth
profile (BRAUCHER et alii, 2009). Each sample, with a weight
of 1 Kg, was collected along levels not thicker than 15 cm and
preceded by a detailed sedimentological description. Finally,
latitude, elevation, shielding and soil thickness data were
collected for each sample because of the influence that they can
have on production rates (see above discussion).
The samples were chemical prepared at the CEREGE (Centre
Européen de Recherche et d’Enseignement des Géosciences de
l’Environnement, Aix en Provence, France) laboratory following
the scheme proposed by BENEDETTI et alii (2003) and STONE et
alii (1996). 36Cl and Cl were measured by isotope dilution
accelerator mass spectrometry at ASTER-CEREGE (France).
Preliminary exposure ages with an assumed steady erosion rate of
0.25 mm/a are between 35 and 89 ka. Between the proposed ages
we prefer the 84-89 Ka range on the base of the following
considerations: a) below the sampled T4 terrace four terrace
orders are preserved and can be at most attributed to the MIS 3
eustatic peaks; b) the sample CLJ2, yielding an exposure age of
35 ka, was characterized by a 0.1 m soil thickness cover,
unusually low for the studied area (soil thickness is normally
between 1 and 10 meters; SANTORO et alii, 2009). This can be
indicative of a greater erosion rate; c) the river incision index
map shows a potentially higher river vertical erosion near to the
CLJ3 (~45 ka) and CLJ4 (~60 ka) sampled areas. The erosion
index (EI) was evaluated on the base of the equation: EI =
Q 5/8 S 19/16 , where Q is the discharge (product between the
upstream drainage area and mean annual rainfalls distribution)
and S is the river gradient (MONTGOMERY &STOLAR, 2006).
Based on the EI distribution it therefore seems reasonable to
suggest that CLJ3 and CLJ4 samples have been exposed to higher
erosion rates; d) two different and independent dating of the
CLJ1 sample give very comparable results.
Based on the preferred exposure ages we obtain an average
uplift rate of ~1.6 mm/a, higher than estimates of CUCCI (2004)
and FERRANTI et alii (2009; ~1 mm/a), but in agreement with
CAPUTO et alii (2010) estimates for the coastal sector to the north
(~1.7-1.8 mm/a). The determination of the chemical composition
of each sample as well as the density along the depth profile will
allow to finalize those preliminary results.
675
REFERENCES
BENEDETTI L., FINKEL R., KING G., ARMIJO R., PAPANASTASSIOU D.,
RYERSON F.J., FERIT F., FARBER D. & STVRAKAKIS G. (2003) -
Motion on the Kaparelli fault (Greece) prior to the 1981
earthquake sequence determined from 36Cl cosmogenic dating.
Terra Nova, 15, 118-124.
CAPUTO R., BIANCA M. & D’ONOFRIO R. (2010) – Ionian marine
terraces of Southern Italy: insights into the Quaternary tectonic
evolution of the area. Tectonics, doi:10.1029/2009TC002625.
CUCCI L. & CINTI F.R. (1998) - Regional uplift and local tectonic
deformation recorded by the Quaternary marine terraces on the
Ionian coast of northern Calabria (southern Italy).
Tectonophysics, 292, 67–83.
CUCCI L. (2004) – Raised marine terraces in the Northern Calabrian
Arc (Southern Italy): a ~600 kyr-long geological record of
regional uplift. Ann. Geophys., 47 (4), 1391-1406.
FERRANTI L., SANTORO E., MAZZELLA M.E., MONACO C. & MORELLI
D. (2009) - Active transpression in the northern Calabria
Apennines, southern Italy. Tectonophysics, 476(1-2), 226-251.
FERRANTI, L.,ANTONIOLI,F.,MAUZ, B., AMOROSI,A.,DAI PRA,G.,
MASTRONUZZI, G.,MONACO, C., ORRÙ, P.,PAPPALARDO, M.,
RADTKE, U.,RENDA, P.,ROMANO, P.,SANSÒ, P.,VERRUBBI, V.
(2006) - Markers of the last interglacial sea level highstand along
the coast of Italy: tectonic implications. Quatern, Int.., 145-146,
30-54.
MONTGOMERY D.R. & STOLAR D.B. (2006) – Reconsidering
Himalayan river anticlines. Geomorphology, 82, 4-15.
SANTORO E., MAZZELLA M.E., FERRANTI L., RANDISI A.,
NAPOLITANO E., RITTNER S. & RADTKE U. (2009) - Raised
coastal terraces along the Ionian Sea coast of northern Calabria,
Italy, suggest space and time variability of tectonic uplift rates.
Quatern. Int.., 206, 78–101.
STONE J.O., ALLAN G.L., FIFIELD L.K. & CRESSWELL R.G. (1996) -
Cosmogenic chlorine-36 from calcium spallation. Geochim.
Cosmochim. Acta, 60(4), 679-692.
BRAUCHER R., DEL CASTLLO P., SIAME S., HIDY A.J. & BOURLÈS
D.L. (2009) - Determination of both exposure time and
denudation rate from an in situ-produced 10Be depth profile: A
mathematical proof of uniqueness. Model sensitivity and
applications to natural cases. Quatern. Geochronol., 4(1), 1-82.
SCHIMMELPFENNIG I., BENEDETTI L., FINKEL R., PIK R., BLARD P.H.,
BOURLÈS D.L., BURNARD P. & WILLIAMS A. – (2009). Sources of
in-situ 36 Cl in basaltic rocks. Implications for calibration of
production rates. Quatern. Geochronol., 4, 441-461.
SESSIONE 20

SESSIONE 20
Key words:, Earth rheology, glacial isostatic adjustment, ice
rheology.
The glacio-hydro-isostatic adjustment (GIA) is the globalscale
process describing the solid Earth deformations and the
gravitational variations which accompany and follow the climaterelated
mass redistributions between the continental ice reservoirs
and the oceans. The GIA is formally described by the so called
”gravitationally self-consistent” Sea Level Equation (SLE) which
accounts for the effects of gravitational interactions and anelastic
Earth rheology upon sea-level change (FARRELL &CLARK, 1976).
Solving the SLE requires therefore two main ingredients, i.e., a
spatio-temporal discretization of the land-based ice sheets and a
rheological law for the solid Earth (MITROVICA & PELTIER,
1991). Since its original formulation the SLE has been widely
employed to model the linear viscoelastic response of a radially
stratified Earth (1D) to the melting of the Late Pleistocene ice
sheets (SPADA &STOCCHI, 2007). Due to the memory effects of
mantle minerals the GIA is still operating today in the form of
slow crustal deformations and gravity ?eld variations which may
significantly affect the land-based and space geodetic
observations (PELTIER, 2004).
The occurrence of a large number of palaeo sea-level
indicators, combined with the availability of present-day
instrumental observations like tide-gauges, GPS stations and
satellite gravimetry, make Fennoscandia one of the key regions
for GIA investigations (MILNE et alii, 2001). In this work we
combine the most recent results from the ice-sheet and Earth
rheology modeling to improve our understanding of the Holocene
and present-day relative sea-level changes, vertical and horizontal
crustal deformations and geoid height variations in Fennoscandia.
We first consider the results from the solution of the SLE
obtained by employing a reasonable mantle viscosity profile for
the region and by applying a realistic ice chronology. The latter
has been created by assuming a viscoplastic rheology for the ice
and by applying local to regional geological and glaciological
_________________________
Glacio-hydro-isostatic adjustment in Fennoscandia:
a review about numerical approaches, Earth rheology
and ice-sheet modeling
PAOLO STOCCHI (*), WOUTER VAN DER WAL (*), BERT VERMEERSEN (*) & RODERIK VAN DER WAL (**)
(*) DEOS - Faculty of Aerospace Engineering, TU Delft (NL),
p.stocchi@tudelft.nl
(**) IMAU - Utrecht University (NL)
676
constraints for the ice margins through time (EHLERS &GIBBARD,
2004).
Successively we solve the GIA problem by applying the ice
chronology to a 3D Finite Elements Method-based Earth model
characterized by lateral variations of rheological parameters and
non linear rheologies (WU, 2004).
We finally compare the results of the two different numerical
approaches (1D SLE and 3D FEM) and discuss the importance of
an improved regional model based on realistic ice and Earth
rheologies.
REFERENCES
EHLERS J. & GIBBARD P. L. (2004) - Quaternary Glaciations -
Extent and Chronology: Part I: Europe. Elsevier Science, pp.
488.
FARRELL W. E. & CLARK J. A. (1976) - On postglacial sea level.
Geophys. J. Royal Astronom. Soc., 46, 647-667.
MILNE G.A., DAVIS J.L., MITROVICA J.X., SCHERNECK H.G.,
JOHANSSON J. M., VERMEER M. & KOIVULA H. (2001) -
Space-Geodetic Constraints on Glacial Isostatic Adjustment
in Fennoscandia. Science, 96, 2381-2385.
MITROVICA J. X. & PELTIER W. R. (1991) - On post-glacial geoid
subsidence over the equatorial ocean. J. Geophys. Res., 96,
20053- 20071.
PELTIER W. R. (2004) - Global glacial isostasy and the surface of
the ice-age earth: the ICE-5G (VM2) model and GRACE.
Ann. Rev. Earth Planet. Sci., 32, 111-149.
SPADA G. & STOCCHI P. (2007) - SELEN: A Fortran 90 program
for solving the ’sea-level equation’. Comp. & Geosci., 33,
538-562.
WU P. (2004) - Using commercial finite element packages for the
study of earth deformations, sea levels and the state of stress.
Geophys. J. Int.., 158, 401-408.

SESSIONE 21
Processi deformativi nella tettonica attiva
CONVENERS
Luigi Ferranti (Università di Napoli)
Riccardo Caputo (Università di Ferrara)
Carmelo Monaco (Università di Catania)
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SESSIONE 21

SESSIONE 21
Deformation of Mount Etna substrate: hints from offshore seismic
reflection profiles
Key words: Marine geology, Mount Etna, reflection seismic
profiles, volcano flank dynamics.
INTRODUCTION AND RATIONALE
Mount Etna is a large volcano that Originated in its present
form ca. 15 kyr ago, following a complex magmatic history that
began ca. 600 kyr ago (BRANCA et alii, 2008).
Despite the clear evidence of active flank dynamics that is
affecting the eastern side of Mount Etna, the contribution of
tectonic processes has not been yet understood. So far, the
various models proposed to explain the observed flank
deformation have been based on onshore structural data, coming
from the volcanic edifice. The flank deformation of Mount Etna
appears to be laterally confined by two tectonic guidelines,
trending roughly E-W, located to the north and south of the
deforming flank; the northern guideline, in particular, takes the
surface expression of a sharp fault (Pernicana Fault). Though
often assumed that these boundary structures continue offshore as
linear features, connected to a frontal thrust ramp (i.e., BORGIA et
alii, 1992; RUST &NERI, 1996), the occurrence of this simple
offshore structural system has not yet been proven. Previous
reflection seismic surveys, in fact, mostly aimed at investigating
the crustal structure underneath the volcano (NICOLICH et alii,
2000). In the last few years the Ionian offshore of Mount Etna has
been investigated using multichannel seismic profiles; these new
data offer the opportunity to image the structural features of the
substrate of the unstable flank of the volcano. This contribution
aims at describing the deformation located offshore Mount Etna
using these recently acquired multichannel seismic profiles.
This work is based on a data set of multichannel seismic
profiles which is composed by there different surveys, carried out
between 2001 and 2006 (ARGNANI &BONAZZI, 2005; PARESCHI
et alii, 2006; ARGNANI et alii, 2009). These surveys total over
800 km of high resolution seismic profiles, with record length
_________________________
(*) ISMAR-CNR, Bologna, andrea.argnani@ismar.cnr.it
(**) Istituto Nazionale di Geofisica e Vulcanologia, Pisa
Lavoro eseguito nell’ambito del progetto FLANK, INGV-DPC
ANDREA ARGNANI (*), FRANCESCO MAZZARINI (**), MARINA BISSON (**),
CLAUDIA BONAZZI (*) & ILARIA ISOLA (**)
678
ranging between 3 and 6 seconds and spatial coverage varying
from 16 to 48 folds. The INGV 2005 survey has shallower
penetration and slightly higher resolution with respect to the
ISMAR-CNR surveys (MESC 2001 and TAORMINA 2006).
Besides contributing to improve the comprehension of the
flank dynamics of Mout Etna, the results obtained from our data
have also broader implications, and can help understanding the
complex active tectonics of this part of Eastern Sicily (e.g.,
ARGNANI, 2009 and references therein).
Fig. 1 – Structural map of Etna offshore. The morphologic high adjacent
to Mount Etna appears bounded by thrust faults. In its northern part a
thick package of strata has been thrust and folded (see Fig. 2); this
deformation likely started before the main building stage of the volcano.
PRELIMINARY RESULTS
Seismic data show a remarkable degree of structural
complexity offshore Mount Etna (Fig. 1). The Pernicana Fault,
for instance, is not continuing offshore as a sharp feature; rather,
the deformation is expressed as ENE-WSW folds located very
close to the coastline. It is likely that these tectonic structures

Fig. 2 – N-S composite line – The region marked as structural high display a thick stratigraphic cover above a poorly reflective substrate. Well stratified
sedimentary packages occur on either side of the high. Stratigraphic relationships suggest that the sedimentary strata onlapped a pre-existing high. As the strata
span at least the whole of the Quaternary, it is believed that the high pre-existed the formation of Mount Etna. The sedimentary package to the north has been
heavily folded, subsequently.
might have affected the offshore of Mount Etna before the
Pernicana Fault system was developed, less than 15 kyr ago. The
southern guideline of the collapsing eastern flank of the volcano
is poorly expressed onshore, and does not show up offshore; in
fact, seismic data indicate that the Catania canyon, a remarkable
E-W-trending feature, does not reflect a tectonic control.
Moreover, the Timpe Fault system does not continue towards the
Malta Escarpment, although a left-lateral offset along the same
fault trend cannot be disregarded.
Seismic interpretation also shows the occurrence of a
structural high located just offshore the edifice of Mount Etna
(Fig. 2). Whereas a complex deformation affects the boundary of
this tectonic element, it shows only limited internal deformation.
Preliminary results led to interpret this structural high as the
northernmost extent of the Hyblean foreland. The role of this
element in the volcano-tectonic evolution of the region is
currently under investigation.
REFERENCES
ARGNANI A. (2009) - Evolution of the southern Tyrrhenian slab
tear and active tectonics along the western edge of the
Tyrrhenian subducted slab. In: Van Hinsbergen D. J. J.,
Edwards M. A. and Govers R. (Eds) - Collision and Collapse
at the Africa–Arabia–Eurasia Subduction Zone. Geol. Soc.,
London, Spec. Publ., 311, 193–212.
ARGNANI A. & BONAZZI C. (2005) - Tectonics of Eastern Sicily
Offshore. Tectonics, 24, doi:10.1029/2004TC001656.
ARGNANI A., BRANCOLINI G., BONAZZI C., ROVERE M, ACCAINO
F., ZGUR F. & LODOLO E. (2009) - The results of the
Taormina 2006 seismic survey: Possible implications for
679
active tectonics in the Messina Straits. Tectonophysics, 476,
159-169.
BRANCA S., COLTELLI M., DE BENI E. & JAN WIJBRANS J. (2008)
- Geological evolution of Mount Etna volcano (Italy) from
earliest products until the first central volcanism (between
500 and 100 ka ago) inferred from geochronological and
stratigraphic data. Int J. Earth Sci., 97, 135–152.
BORGIA A., FERRARI L. & PASQUARÈ G. (1992) - Importance of
gravitational spreading in the tectonic and volcanic evolution
of Mount Etna. Nature, 357, 231-235.
NICOLICH R, LAIGLE M., HIRN A., CERNOBORI L. & GALLART J.
(2000) - Crustal structure of the Ionian margin of Sicily: Etna
volcano in the frame of regional evolution. Tectonophysics,
329, 121-139.
PARESCHI,M.T.,E.BOSCHI,F.MAZZARINI &FAVALLI M. (2006)
- Large submarine landslides offshore Mt. Etna. Geophys.
Res. Lett., 33, doi:10.1029/2006GL026064.
RUST D. & NERI M. (1996) – The boundaries of large-scale
collapse on the flanks of Mount Etna, Sicily. In; W.J.
McGuire, A.P. Jones & J. Neuberg (Eds.) – Volcano
instability on the Earth and Other Planets. Geol. Soc.,
London, Spec. Publ., 110, 193–208.
SESSIONE 21

SESSIONE 21
Microstructural and petrophysical characterization of a coseismic
(?) fault zone in poorly lithified sands from the Crotone basin
Key words: Cataclasis, coseismic rupture, fault core
microstructures, fault permeability, poorly lithified sediments.
Diagnostic features of coseismic ruptures are well established
in many lithologies such as crystalline basement rocks, clay-rich
materials in accretionary prisms and, recently, in limestones.
Few attempts have been made to establish comparable criteria
for coseismic ruptures in poorly lithified sediments.
We studied an extensional fault zone with 1.36 m of
displacement developed in poorly lithified, quartz-rich high
porosity sandy sediments of the seismically active Crotone basin
(southern Italy).
The fault zone cuts across fine- to coarse-grained sands and
consists of a cm-thick, discrete fault core embedded in virtually
undeformed wall sediments. Consequently, it can be described as
“structurally oversimplified” due to the lack of footwall and
hanging wall damage zones.
We acquired microstructural, grain size, grain shape, porosity,
mineralogical and permeability data to constrain deformation
mechanisms and to investigate the influence of initial
sedimentological characteristics of sands on the final faulted
granular products and related hydrologic properties.
Faulting evolves by a general grain size and porosity
reduction with a combination of intragranular fracturing, spalling,
and flaking of grain edges, irrespective of grain mineralogy.
The dominance of cataclasis, also confirmed by fractal
dimensions >2.6, is generally not expected at a deformation depth

Ionian marine terraces of Southern Italy:
insights into the Quaternary tectonic evolution of the area
Key words: Pleistocene; morphotectonics; paleo-shorelines
RICCARDO CAPUTO (*), MARCELLO BIANCA (**) & ROCCO D'ONOFRIO (°)
New detailed morphotectonic analyses of a well exposed
flight of marine terraces along the Ionian coast of Southern Italy
has been carried out. The area represents a key transect for
investigating the middle-late Quaternary evolution of the
Southern Apennines chain-foredeep-foreland geodynamic system.
The present research is essentially grounded on a systematic,
completely new, mapping of a wide coastal sector (ca. 1500 km 2 )
between northern Calabria and Puglia (Southern Italy) allowing
to recognize and reconstruct in detail the 3D geometry of a flight
of marine terraces. A major result of the research is the
reconstruction of a virtually complete 3D geometry of the marine
surfaces along a coastal sector of ca. 70 km, which i) documents
the occurrence of 18 paleo-shorelines and ii) provide evidence for
a strong regional uplift affecting the investigated area (Fig. 1).
Following a systematic critical review of available
geochronological data, the different terraces are correlated to as
many highstand sea level peaks, dating the oldest terrace to ca.
600 ka (MIS 15). The vertical and horizontal distribution of the
terraces show a general convergence of the paleo-shorelines
towards NNE, which indicates a decreasing trend in differential
uplift in that direction ranging from almost 2 mm/a (SW) to about
0.2 mm/a (NE).
Based on i) the general trend of the whole terrace sequence
(Fig. 1), ii) the critically revised chronological correlations
(CAPUTO et al., 2010) and iii) the relatively constant (for each
coast-perpendicular profile) uplift-rates during the last 600 ka, it
is thus possible to suggest the partitioning of the area into three
distinct sectors characterized by different tilting rates. This
behavior is likely caused by the combined role and activity of
three major tectonic structures working at different scales and
rates (Fig. 2) including i) the reactivation of an out-of-sequence
thrust, ii) sliding along the basal detachment of the external
Apennines wedge and iii) a lithospheric-scale duplexing (crustal
or deeper). In a geological time-scale perspective, the
contemporaneous activity of the three processes (fold-related,
_________________________
(*) Dipartimento di Scienze della Terra, Università di Ferrara
rcaputo@unife.it
(**) Di.S.G.G., University of Basilicata, Potenza, Italy
(°) Laurenzana (PZ), Italy
681
wedge-rotation and lithospheric duplexing) concur to the
regional uplift and tilting in different ways and could be
considered as a typical effect of the strain partitioning that always
characterizes large rock bodies undergoing deformation.
Although it is commonly assumed that shortening in the
Southern Apennines ceased at the beginning of the Middle
Pleistocene and the frontal blind thrust (viz. basal detachment)
also de-activated, our results clearly indicate the persistence
throughout the whole Quaternary and probably till Present of a
regional compression and a contractional tectonic regime
affecting the external sector of the Southern Apennines chain and
its foredeep. The estimated cumulative shortening along a NE-
SW direction across the investigated area during the last 600 ka
could be in the range 3-8 km, thus providing a mean regional
long-term convergence-rate of 5-10 mm/a.
Based on the differential uplift estimated separately for the
three processes, it is possible to analyse the most recent activity
(latest Pleistocene-Holocene) of each tectonic structure. As
discussed in CAPUTO et al. (2010), the fold-related process
probably ceased its contribution well before the Holocene (ca. 30
ka BP). In contrast, for the other two processes the tilt versus
time distribution suggests that the associated structures still
contribute to the general uplift and tilting (viz. differential uplift)
Fig. 1 – Longitudinal projection profile of the marine terraces mapped in the
investigated area and traced parallel to the present-day coast line. The dotted
lines correlate the marine terraces across the major valleys. The black circles
are the sites for which absolute ages are available from the literature (see a
review and critical analysis in CAPUTO et al., 2010). Note that both Ponte del
Re and San Teodoro II sites belong to the San Basilio terrace; both San
Teodoro I and La Maddalena sites to the San Teodoro terrace, while both La
Petrulla and Piano San Nicola sites to the Policoro terrace.
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Fig. 2 –Simplified geological section crossing the Southern Italy chainforedeep-foreland
system and running parallel to the investigated coastal
sector. Inset (a) shows the location of the mapped marine terraces with respect
to the profile below. The tectonic structures responsible of the three differentscale
processes are marked with thick lines in the profile, while the superficial
sectors potentially affected by the three tilting processes are indicated on top
of the profile. 1) Apulian continental crust; 2) Apulian carbonate sequence; 3)
Apennines orogenic wedge including all undifferentiated tectonic units; 4)
Quaternary deposits of the Bradanic Foredeep
of the region hence suggesting their persisting activity.
Three further arguments support the conclusion of a recent
(latest Quaternary) compressional activity. First, it is the
Holocene age of the youngest involved inner edge. Second, GPS
velocities presented by FERRANTI et al. (2008) for the region are
in perfect agreement with our estimated values contributed by the
two deeper tectonic structures. Third, just few kilometers offshore
the investigated coastal sector, seismic profiles clearly document
that the frontal thrust of the Apennines accretionary wedge is
active and deforms the sea bottom (e.g. PIERI et al., 1997). At this
regard, unpublished seismic profiles for hydrocarbon exploration
carried out within the Gulf of Taranto provide additional
evidence of contractional structures deforming the sea bottom
along the frontal sector of the basal detachment thus confirming
its very recent activity.
As a final comment, a direct consequence of the above
conclusion is probably of primary importance for the seismic
hazard of the region. At this regard, it is useful to consider
separately the activity along the basal detachment and the
lithospheric duplex. The relevant information and inferences for
the basal detachment could be summarized as follows: i) possible
fault dimensions are tens of kilometers-long by tens of
kilometers-wide (for example, 70 x 40 km 2 ), ii) the long-term
slip-rate ranges between 1.0 and 2.8 mm/a, iii) the corresponding
682
maximum magnitude could be around 7.5, iv) associated coseismic
displacements about 2-4 m and hence v) mean repeat
time for major characteristic earthquakes between ca. 700 and
4000 years. Notwithstanding the completeness of the Italian
seismic catalogues for such strong events for the last thousand
years, no record exists for the investigated area. Taking also into
account that the focal depth would be relatively shallow (Fig. 2),
the potential seismic hazard associated with the basal detachment
(wedge-rotation process) is possibly high.
As concerns ths lithospheric duplexing process and though
the amount of cumulative shortening is possibly larger, the
internal strain partitioning typical of these contractional structures
characterized by multiple subparallel low-angle faults generally
reduces the slip-rate on each sliding plane. However, a major
uncertainty in assessing the seismic hazard of this shear zone
follows the difficulty to define the current mechanical behavior of
the affected rock volume, which strongly depends on the real
depth of the duplex structure. Indeed, if it occurs in the lower
crust below the brittle-ductile transition (as tentatively suggested
in Fig. 2), a viscous rheology prevails and deformation likely
takes place aseismically. In contrast, if the uppermost lithospheric
mantle is involved, the rheological profiles of the area suggest a
brittle behavior characterized by a typical stick-slip mechanism.
In the former case, the corresponding seismogenic potential is
low, while it would be much larger if the latter hypothesis holds.
Further investigations and geological constraints will probably
help in unravelling the situation.
REFERENCES
CAPUTO R., BIANCA M. & D'ONOFRIO R. (2010) - Tectonics, doi:
10.1029/2009TC002625.
FERRANTI L., OLDOW J.S., D’ARGENIO B., CATALANO R., LEWIS
D., MARSELLA E., AVELLONE G., MASCHIO L., PAPPONE G.,
PEPE F. & SULLI A. (2008) - Boll. Soc. Geol. It., 127(2), 299-
316.
PATACCA E. & SCANDONE P. (2004) - In: Crescenti U., D'Offizi
S., Merlino S. & Sacchi L. (Eds.), Geology of Italy. Spec. vol.
It. Geol. Soc. for the IGC 32 Florence-2004, 93-129.
PIERI P., VITALE G., BENEDUCE P., DOGLIONI C., GALLICCHIO S.,
GIANO S.I., LOIZZO R., MORETTI M., PROSSER G., SABATO L.,
SCHIATTARELLA M., TRAMUTOLI M. & TROPEANO M. (1997) -
Il Quaternario, 10, 2, 535-542.

The timescale and spatial extent of vertical tectonic motions in Italy:
insights from coastal tectonic studies
Key words: Coastal tectonics, , GPS, Holocene, Italy, Late
Pleistocene, tide gauges, vertical motion.
INTRODUCTION
Although caught in between the steady-state relative
convergence of the African and European continental landmasses,
the Neogene history of the Central Mediterranean Sea features
smaller-scale orogenic segments where rapid thrust-belt motion,
crustal thickening and back-arc thinning occurred in laterally
discrete areas and often overwhelmed the plate-scale signature.
Depending on the timescale of observation and on the
appropriate analytical tool, however, modes and rates of
deformation can be established with variable uncertainty in
individual crustal segments. Tectonic events occurring at the
million-yr timescales have left their record in the geological
archive of Italy, and rates of orogenic belt migration are relatively
well established. Similarly, the pattern of contemporary
deformation is well depicted by instrumental data including
seismicity and geodetic analysis. Unfortunately, geologic and
modern motions are not always reconciled with ease.
In this contribution, we supply an overview of the
intermediate- and short-term (100 to 1 Ka BP) vertical tectonic
displacement pattern drawn from coastal analysis, and, together
with instrumental observations (contemporary scale), allow to
bridge the gap with events recorded in the geologic (1 Ma)
archive. Integration of morphotectonic, structural,
geoarcheological, tide-gauge and GNSS data helps establishing
the appropriate spatial extent, and timescale of rate change of
vertical tectonic motion within individual crustal segments. In
addition, we place constraints on the contribution to
displacements coming from regional (deep) and local (shallow-
_________________________
(*) Dipartimento di Scienze della Terra, Università di Napoli Federico II,
lferrant@unina.it
(**) ENEA, Casaccia, Rome, Italy.
(°) INGV, Centro Nazionale Terremoti, Rome, Italy.
(°°) Dipartimento di Scienze Geologiche, Università di Catania, Italy.
(§) DEOS, Faculty of Aerospace Engineering, TU Delft, The Netherlands.
LUIGI FERRANTI (*), FABRIZIO ANTONIOLI (**), MARCO ANZIDEI (°),
CARMELO MONACO (°°) & PAOLO STOCCHI (§)
683
crustal) sources, with the aim to provide clues on the depth
significance and driving mechanisms of deformation.
RESULTS
In this contribution, the distribution of the 125 ka and of the
Late Holocene coastal markers will be presented, supplemented
by tide-gauge and other instrumental data (for details and
previous reviews, see: BORDONI &VALENSISE, 1998; ANTONIOLI
et alii, 2009; LAMBECK et alii, 2004; LAMBECK et alii, 2010).
Results are here briefly summarized. The central and northern
Tyrrhenian Sea and the Ligurian Sea margins show stability at all
scales, except for subsidence in coastal basins and uplift, at
places extraordinarily high, at volcanic centres. The southwestern
part of the area centered on western Sicily is
characterized by a slow deformation signal fragmented in limited
structural compartments, but is currently experiencing whole
uplift that might be related to coherent block relative convergence
with Sardinia.
On the contrary, large (~300 km wavelength) and spatially
homogeneous uplift coincides with the Calabrian forearc terrane,
and is also detected in the instrumental record. A deep-seated
contribution to uplift, highlighted by the spatial coincidence with
a NW-dipping lithospheric slab, is embedded in a regional
component, and the remaining fraction is ascribed to local
sources, including extensional and contractional faults. A wealth
of morphological and archaeological data documents that shortterm
uplift was up to two-times larger than that averaged over
intermediate time-scales, but the locations of fastest Late
Pleistocene, Holocene, and contemporary uplift rates spatially
coincide. At several locales, the recent increase in uplift rate can
be related to temporal clustering of slip on active faults and rapid
fold growth. The more efficient strain release might indicate a
contemporary tectonic wave, which we suggest might have been
triggered by regional isostatic response to deglaciation.
Oppositely to Calabria, a weak deformation signal is recorded
on the central Adriatic coastline and may record slow thrust belt
migration at the front of the Apennines. Finally, the pattern of
vertical tectonic motions in the northern Adriatic Sea records the
aggregate effects of displacement in the oppositely facing
orogens of the southern Alps, internal Dinarids and northern
Apennines, but flexure of the Adriatic (micro-)plate beneath the
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SESSIONE 21
Northern Apennines appears the dominating contributor. Along
the northern Adriatic Sea margins, rates and spatial extent of
displacements remains unchanged from the 100 ka to the
contemporary timescale, suggesting a steady control exercised by
the plate dynamics.
IMPLICATIONS
Accurate and precise determination of intermediate-scale
markers of deformation is of paramount importance in active
orogens with relatively low displacement rates, such as those
encountered in the Central Mediterranean Sea, where a
straightforward comparison between the geological record and
the current deformation pattern supplied by geodesy and
seismicity is difficult. This analysis provides vital information of
the extent of seismic cycles and the relative role of seismogenic
versus regional processes, with profound implications on seismic
potential determination and coastal hazards.
REFERENCES
ANTONIOLI, F.,FERRANTI, L.,FONTANA, A.,AMOROSI, A.,M.,
BONDESAN, A.,BRAITENBERG, C., DUTTON, A.,FONTOLAN,
G., FURLANI, S.,LAMBECK, K.,MASTRONUZZI, G.,MONACO,
C., SPADA, G.&STOCCHI, P. (2009) - Holocene relative sealevel
changes and vertical movements along the Italian and
Istrian coastlines. Quatern. Int., 206, 102-133.
BORDONI, P.&VALENSISE, G. (1998) - Deformation of the 125
ka marine terrace in Italy: tectonic implications. In: I.S.
Stewart and C. Vita-Finzi, (Eds.) - Coastal Tectonics. Geol.
Soc., London, Spec. Publ., 46, 71-110.
FERRANTI, L.,ANTONIOLI, F.,MAUZ, B., AMOROSI, A.,DAI PRA,
G., MASTRONUZZI, G.,MONACO, C., ORRÙ, P.,PAPPALARDO,
M., RADTKE, U., RENDA, P., ROMANO, P., SANSÒ, P. &
VERRUBBI, V. (2006) - Markers of the last interglacial sea
level highstand along the coast of Italy: tectonic implications.
Quatern. Int., 145-146, 30-54.
LAMBECK,K.,ANTONIOLI,F.,PURCELL,A.&SILENZI, S. (2004) -
Sea level change along the Italian coast for the past 10,000
yrs. Quatern. Sci. Rev., 23, 1567-1598.
LAMBECK K., ANTONIOLI F., ANZIDEI M., FERRANTI L., LEONI G.,
SCICCHITANO G., SILENZI S. (2010) - Sea level change along
the Italian coast during the Holocene and projections for the
future. Quatern. Int., doi:10.1016/j.quaint.2010.04.026.
684

Integration of structural and geomorphological data from the
Western Ligurian Alps: creation of a GIS database and inferences
for the morphotectonics of the area
Key words: Ligurian Alps, Morphotectonics, Tectonic
lineaments, GIS .
We constructed a GIS supported database integrating surface
data (such as river networks, wind gaps, hillslopes morphology)
and structural data (encompassing both faults measured in the
field and lineaments identified on aerial photographs).
Currently, several years of independent researches leaded to
the collection both of a hydrographical (FERRARIS, 2009;
SPAGNOLO & FIRPO, 2007) and a structural data set for the
Ligurian sector of the Western Alps. The use of GIS software
provided a powerful tool for handling large data sets and to
incorporate and compare a wide variety of information (such as
lithology, tectonics, river networks etc.). In particular, in this
study, a GIS environment has been chosen with the aim to collect
all of the available scattered data and to offer a starting point for
further studies.
The study area is located between the Ligurian Sea to the
south, the Po plain to the north and straddles the Alps-Apennine
boundary area. It is characterized by a complex fault network;
azimuth of faults have been analyzed with a statistical approach.
When possible, a time sequence between the different fault set
has been established in the field by checking cross-cutting
relationships.
We identified some structural domains, characterized by fault
population with different dominant orientation, that have been
compared to existing bibliographic data (SPAGNOLO, 2006); each
domain can be referred to a different dominant tectonic regime.
The present day morphology of Ligurian Alps reflects this
complex tectonic setting as well as erosional processes that vary
from the coast to the chain, and, there, from the marine flank to
the northern one.
The main divide is located just 10 km inland from the
coastline and separates a short and steep flank, facing South,
from a wide and gentle one, facing North. Anomalous streams
networks affect the whole area: asymmetric basins, trellis pattern
and abrupt changes in channels longitudinal profiles characterize
both flanks.
The influence either of local and regional tectonics on the
_________________________
(*) Dipteris, Università degli Studi di Genova,
francesca.ferraris@dipteris.unige.it.
FRANCESCA FERRARIS (*), LAURA FEDERICO (*) & LAURA CRISPINI (*)
685
morphology of the area has long been inferred but at the moment
no detailed studies exist in which this link has been tested or
quantified.
Being tectonics and rock structure reflected in the overall
Fig. 1 – Shaded relief of Western Alps with the location of the study area
(white box).
arrangement of streams forming regional drainage networks, the
comparison of independent data allowed to detect the tectonic
signature in drainage pattern and, therefore, to define its
influence in the overall aspect of the area.
We therefore test and discuss the link between the different
structural domains and the main geomorphological features at a
regional scale.
REFERENCES
FERRARIS F. (2009) – Morphotectonic analysis and Plio-
Quaternary evolution of the eastern Ligurian Alps. Unpubl.
PhD Thesis, University of Genova.
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SPAGNOLO C., (2006) - Late-orogenic tectonics in the eastern
sector of the Ligurian Alps. Unpubl. PhD Thesis, University
of Genova.
SPAGNOLO M. & FIRPO M. (2007) – Geomorphic evolution of the
seaward escarpment in the NE Ligurian Alps (Italy). Z.
Geomorphol., NF 51(1), 115-134
686

Active deformation in southern Italy from GNSS velocities:
updated results of the PTGA
MARIA ENRICA MAZZELLA (*), LUIGI FERRANTI (*), MIMMO PALANO (**), MARIO MATTIA (**), JOHN S. OLDOW (°),
RAIMONDO CATALANO (°°), BRUNO D’ARGENIO (§), ERWAN GUEGUEN (§§), ENNIO MARSELLA (§),
CARMELO MONACO (#), PAOLO ORRÙ (##), GIUSEPPE AVELLONE (°°), MAURIZIO GASPARO MORTICELLI (°°),
LAURA MASCHIO (*), ENRICO SANTORO (#), CECILIA RITA SPAMPINATO (#) & GIOVANNI SCICCHITANO (#)
Key words: Active deformation, GNSS velocities, Sicily, southern
Italy, southern Sardinia.
The PTGA network consists of 72 sites installed in southern
Italy with the aim of detecting the orogenic interseismic strain,
which were measured during 1995, 1997, 2000 e 2008. Results of
the last measurement session, presented here, provide new
insights into active deformation processes detected in previous
analysis (FERRANTI et alii, 2008).
Data were processed using the GAMIT/GLOBK (version
10.35) software developed at the Harvard Smithsonian Center of
Astrophysics of the MIT, and at the Institute of Oceanography,
University of California. The software involves multi-step
routines for processing and modeling of GNSS observations
(HERRING et alii, 2006). Firstly we created and processed the
double differenced iono-free observables that were used to
estimate the daily loose-constrain solutions with the stations
coordinates, the orbits and the atmospheric delays, and the
variance-covariance matrix. For a better estimate of the
parameters of each solution we used precise ephemerides
calculated by the International GNSS Service (IGS) and the earth
rotation parameters provided by the International Earth Rotation
Service. We inserted in the processing the data of ten IGS
permanent sites (AJAC, CAGL, GRAS, GRAZ, LAMP, MATE,
MEDI, NOT1, NOTO e ZIMM). Then, the loose constrained
daily solutions were combined (on a daily base) with the regional
solution (IGS1, IGS2, IGS3, IGS4, EURA and EUREF) provided
by SOPAC (Scripps Orbit and Permanent Array Center) and EPN
_________________________
(*) Dipartimento di Scienze della Terra, Università degli Studi di Napoli
“Federico II”, ikeira82@hotmail.com
(**) Istituto Nazionale di Geofisica e Vulcanologia, sezione di Catania.
(°) Department of Geosciences, University of Texas at Dallas, USA.
(°°) Dipartimento di Geologia e Geodesia, Università di Palermo.
(§) Istituto di Geologia Marina, Consiglio Nazionale delle Ricerche, Napoli.
(§§) Istituto di Metodologie per l’Analisi Ambientale, C.N.R., Tito Scalo
(PZ).
(#) Dipartimento di Scienze Geologiche, Università degli Studi di Catania.
(##) Dipartimento di Scienze della Terra, Università di Cagliari.
687
(EUREF Permanent Network) by a Kalman filter GLOBK to
create an unconstrained daily net solution. Using the GLORG
Fig. 1 - GNSS velocities of the PTGA network relative to stable Europe.
module of GLOBK, the solutions were aligned into the
International Terrestrial Reference Frame (ITRF) 2005
(ALTAMIMI et alii, 2007) by a Helmert transformation (estimate
of 3 rotation parameters, 3 translation parameters and 1 scale
factor) to generate time series of the Nord, East and Up
components of each station and the velocity field. This ITRF2005
velocity field was aligned with a stable Europe reference frame
(NOCQUET & CALAIS 2003) by a further Helmert transformation.
Relative to Europe, all the sites of the net, except for Sardinia,
move toward the northern quadrants, with a significant internal
variability that underline the existence of different deformation
domains (Fig. 1). For a better understanding of distributed
deformation, velocities were referred to permanent IGS sites
(Matera for the southern Apennines, Noto for Sicily and Cagliari
for Sardinia). In southern Italy (Fig. 2), the updated GNSS
velocities confirm the presence of two adjacent deformation
zones (FERRANTI et alii, 2008): an extensional domain in the
west, where Campania and Calabria sites move away from
MATE with increasing westerly velocities from 2 to 5 mm/a; and
a transpressional domain in the east, Adriatic and Ionian area of
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SESSIONE 21
Fig. 2 - GNSS velocities of the PTGA network in southern Appennines
relative to permanent IGS site Matera.
Fig. 3 - GNSS velocities of the PTGA network in Sicily relative to
permanent IGS site Noto.
Puglia, Basilicata and Calabria, more markedly between Gargano
and northern Murge, where sites show convergence or oblique
movement relative to MATE, consistent with a right lateral
displacement between the two blocks.
In Sicily, motion relative to NOTO (Fig. 3) suggests right
lateral transpression between the frontal thrust belt and the
northern Hyblean margin. In central-western Sicily a broad
contractional belt is detected. Sicily sites convergence with
Sardinia sites (Fig. 1), in agreement with the seismic activity
between the islands. In southern Sardinia (Fig. 4), site residuals
velocities relative to CAGL are small and very close to the
associated error. On the whole, the western side of the
Campidano moves toward W-SW, while the eastern site (VISI)
moves toward NW. These data are consistent with a shear
deformation related to a NNW-SSE shortening.
By interpolation, we derived the horizontal strain field
starting from the velocity values, the net geometry and the
688
associated covariance matrix. Significant compressional strains
(up to 0.04 μstrain/a) are found in northern Calabria and Puglia,
and similar values of extensional strain occur in western
Campania. The compressional strain axes are oriented NW-SE
between Gargano and Murge and NE-SW in northern Calabria.
Tensile axes are oriented NE-SW in western Campania,
consistent with the seismic record, and NW-SE in north-eastern
Basilicata. Similar-magnitude, non uniaxial strain (NW-SE
compression and NE-SW extension) are found between
Campania and Molise, consistent with recent earthquake.
Fig. 4 - GNSS velocities of the PTGA network in southern Sardinia relative
REFERENCES
ALTAMIMI Z., COLLILIEUX X., LEGRAND J., GARAYT B. &
BOUCHER C. (2007) - ITRF2005: a new release of the
International Terrestrial Reference Frame based on time
series of station positions and Earth Orientation Parameters.
J. Geophys. Res., 112, B09401, doi: 10.1029/2007JB004949.
FERRANTI L. et alii (2008) - Active deformation in Southern Italy,
Sicily and southern Sardinia from GPS velocities of the Peri-
Tyrrhenian Geodetic Array (PTGA). Boll. Soc. Geol. It.,
127/2, 299-316.
HERRING T.A., KING R.W. & MCKLUSKY S.C. (2006) - GAMIT
Reference Manual: GPS Analysis at MIT, Version 10.3;
GLOBK Reference Manual: Global Kalman Filter VLBI and
GPS Analysis Program, Version 10.3. Massachusetts Institute
of Technology, Cambridge, MA.
NOCQUET J.M. & CALAIS E. (2003) – Crustal velocity field of
western Europe from permanent GPS array solutions, 1996-
2001. Geophys. J. Int., 154, 72-88.

Key words: Coseismic deformation, sea level, southern Italy,
tectonic uplift.
Sea level is the general reference for detecting ongoing
vertical crustal movement and assessing short- and long-term
tectonic instability in coastal areas (LAJOIE, 1986). Short term
estimations include analysis of tide-gauge data and historical and
archeological information that may indicate apparent sea-level
change, whereas long-term crustal movements can be detected by
mapping and dating marine strandlines and separating the
tectonic component from the eustatic and hydro-glacio-isostatic
components of the relative sea level change (LAMBECK et alii,
2010).
Data on relative sea level change occurred during the
Holocene along the coast of north-eastern Sicily and southeastern
Calabria (Fig. 1) have been obtained
using precise measures and radiometric dating of raised
shorelines in the Milazzo peninsula (see also RUST &KERSHAW,
2000), Messina Straits (see also FERRANTI et alii, 2007) and
Taormina area (see also STEWART et alii, 1997; ANTONIOLI et
alii, 2003; DE GUIDI et alii, 2003), the fastest uplifting sectors of
the central Mediterranean region. These strongly uplifted coastal
regions are located along a main seismogenic system which
affects the Tyrrhenian side of southern Calabria and the Ionian
coast of eastern Sicily.
The analysis indicate that vertical displacement occurred as an
alternation of steady and episodic motions. Precise compensation
for eustatic changes and hydro- glacio-isostatic adjustments
(LAMBECK et alii, 2010) constrains Late Holocene total uplift at
~ 2.0 mm/yr, almost equally balanced between the steady and the
stick-slip components. Late Holocene steady uplift during the
interseismic intervals at 1.0 mm/yr is consistent with long-term
_________________________
The contribution of coseismic deformation to relative sea level
change during the Holocene: examples from the coastal areas of
north-eastern Sicily and southern Calabria
(*) Dipartimento Scienze Geologiche, Università di Catania,
cmonaco@unict.it.
(**) ENEA, Casaccia, Roma.
(°) Dipartimento Scienze della Terra, Università di Napoli Federico II.
Lavoro eseguito con il contributo finanziario dell’Università di Catania e
Napoli Federico II.
CARMELO MONACO (*), FABRIZIO ANTONIOLI (**), LUIGI FERRANTI (°),
CECILIA RITA SPAMPINATO (*) & GIOVANNI SCICCHITANO (*)
689
(0.1-1 Ma) estimates (WESTAWAY, 1993). Abrupt displacements
are attributed to co- and post-seismic footwall uplift along normal
faults (Scilla, Taormina, Capo d’Armi) or transpressive structures
(Milazzo), which are inferred to run immediately offshore the
studied coastal outcrops.
REFERENCES
ANTONIOLI F., KERSHAW S., RUST D. & VERRUBBI V. (2003) –
Holocene sea-level change in Sicily an its implications for
tectonic models: new data from the Taormina area, northeast
Sicily. Mar. Geol., 196, 53-71.
ARGNANI A., SERPELLONI E. & BONAZZI C. (2007) - Pattern of
deformation around the central Aeolian Islands: evidence
from multichannel seismics and GPS data. Terra Nova, 19,
317–323.
DE GUIDI G., CATALANO S., MONACO C. & TORTORICI L. (2003)
– Morphological evidences of Holocene coseismic
deformation in the Taormina area (NE Sicily). J. Geodynam.,
36, 193-211.
FERRANTI L., MONACO C., ANTONIOLI F., MASCHIO L., KERSHAW
S. & VERRUBBI V. (2007) – The contribution of regional uplift
and coseismic slip to the vertical crustal motion in the
Messina Straits, southern Italy: evidence from raised Late
Holocene shorelines. J. Geophys. Res., 112, B06401,
doi:10.1029/2006JB004473.
LAJOIE K.R. (1986) - Coastal Tectonics. In: Geophysics Studies
Committee, Commission on Physical Sciences, Mathematics
and Resources, Active Tectonics. National Academy Press,
Washington, 95-124.
LAMBECK K., ANTONIOLI F., ANZIDEI M., FERRANTI L., LEONI G.,
SCICCHITANO G., SILENZI S. (2010) - Sea level change along
the Italian coast during the Holocene and projections for the
future. Quatern. Int., doi:10.1016/j.quaint.2010.04.026.
RUST D. & KERSHAW S. (2000) - Holocene tectonic uplift
patterns in northeastern Sicily: evidence from marine notches
in coastal outcrops. Mar. Geol., 167, 105 – 126.
SESSIONE 21

SESSIONE 21
Fig. 1 - Regional tectonic map of the southern part of the Calabrian Arc. Double arrows show extension direction in Western Calabria and Eastern Sicily and
contraction direction offshore. The broad uplifted areas between Capo Milazzo and Vulcano (from ARGNANI et al., 2007) are indicated in grey pattern (VF,
Vulcano fold; CMF, Capo Milazzo fold).
STEWART I., CUNDY A., KERSHAW S. & FIRTH C. (1997) –
Holocene coastal uplift in the Taormina area, north-eastern
Sicily: implications for the southern prolongation of the
Calabrian seismogenic belt. J. Geodynam., 24, 37-50.
WESTAWAY, R. (1993) - Quaternary uplift of southern Italy. J.
Geophys. Res., 98, 21741-21772.
690

Key words: Capo d’Orlando fault, luminescence dating, marine
terraces, OSL, SAR protocol.
The coastal sector of Sant’Agata di Militello (NE Sicily) is
characterized by a flight of raised Upper-Middle Pleistocene
marine terraces occurring at different heights with respect to
present sea level. In particular, the field geomorphologic survey
and the analysis of stereo-pairs of aerial photographs allowed to
recognize at least five main orders of well preserved Quaternary
surfaces and relative deposits mostly located at the hangingwall
and at the footwall of a Pleistocene northwest-dipping normal
fault, named Capo d’Orlando fault, that controlled the
geomorphologic evolution of the coast.
The marine terraces show an overall good morphological
continuity and are formed by marine platforms overlain by littoral
deposits. The wave-cut surfaces are carved on Middle Pleistocene
deltaic marine gravels and sandy deposit (Sabbie e Ghiaie di
Messina), on Mesozoic carbonate successions and/or on their
Paleozoic metamorphic basement (CARBONE et alii, 1998). The
raised palaeo-shorelines are represented by remnants of the inner
edges, lithophaga hole bands and/or other biological sea level
markers. The terraced deposits are made up of yellow littoral
sand and gravels in a sandy matrix. The complete sequence of
marine terraces outcrops only in the area of Sant’Agata di
Militello where the Capo d’Orlando fault disappears. To the east,
at the hanging wall of the Capo d’Orlando fault, the terraced
sequence is incomplete, probably due to the fault activity.
The continental sedimentary cover of the second order
terrace, outcropping at Acquedolci, contains mammal-bearing
deposits (Hyppopotamus Pentlandi) that have been dated
200±40ka BP by isoleucine epimerization method (BADA et alii,
1991), allowing to relate them to the MIS 7.1. high-stand.
In order to better define the terrace chronology, samples of
_________________________
Luminescence chronology of Pleistocene marine terraces of the
Sant’Agata di Militello coastal sector (north-eastern Sicily)
SILVIA ORIOLI (*), GLORIA M. RISTUCCIA (**)(°), CARMELO MONACO (°), ANNA M. GUELI (**),
GIUSEPPE STELLA (**), SEBASTIANO O. TROJA (**) & GIUSEPPE GIUNTA (*)
(*) Dipartimento di Geologia e Geodesia, Università di Palermo,
silviaorioli@unipa.it
(**) Dipartimento di Fisica ed Astronomia, Università di Catania,
gloria.ristuccia@ct.infn.it
(°) Dipartimento di Scienze Geologiche, Università di Catania,
cmonaco@unict.it
691
terraced deposits are analyzed in this occasion by Optically
Stimulated Luminescence (OSL) technique, a conventional SAR
protocol was used with sand-sized quartz (MURRAY &WINTLE,
2003). New dating, together with detailed morphostructural
analysis allowed us to reconstruct the tectonic evolution of this
coastal area and to constrain the activity of the Capo d’Orlando
fault in a precise time range.
REFERENCES
BADA J.L., BELLUOMINI G., BONFIGLIO L., BRANCA M., BURGIO
E. & DELITALA, L. (1991) - Isoleucine epimerization ages of
Quaternari mammals from Sicily. Il Quaternario, 4(1a), 49-54.
CARBONE S., LENTINI F. & VINCI G. (1998) – Carta geologica del
settore occidentale dei Monti Peloritani (Sicilia nordorientale).
S.EL.CA., Firenze.
MURRAY A.S. & WINTLE A.G., (2003) – The single aliquot
regenerative dose protocol: potential for improvements in
reliability. Rad. Measur., 37, 377-381.
SESSIONE 21

SESSIONE 21
Uplift and folding of Pleistocene marine terraces along the Ionian
Sea coast of northern Calabria: field analysis and model results.
ENRICO SANTORO (*), LUIGI FERRANTI (**), CARMELO MONACO (*), PIERFRANCESCO BURRATO (°),
MARIA ENRICA MAZZELLA (**) & DANILO MORELLI (°°)
Key words: Folding, marine terraces, numerical fault
modeling, transpressional faults, uplift rates.
A detailed study of uplifted Middle-Late Pleistocene marine
terraces on the eastern side of northern Calabria and Basilicata
provides insights into the temporal and spatial scale variability of
vertical displacement rates over a time span of ~600 ka, and
allowed to model the recent activity of transpressional faults in
the area.
This region is located on the northeastern tip of the Calabrian
arc, which experienced rapid Late Quaternary uplift due to a
combination of lithospheric and crustal processes (WESTAWAY,
1993; WORTEL &SPAKMAN, 2000; GVIRTZMAN &NUR, 2001).
Ten terrace orders were mapped up to 663 m a.s.l., and were
correlated between the coastal slopes of Pollino and Sila
mountain ranges across the Sibari Plain (Fig. 1).
Radiometric (ESR and 14C) dating of shells have provided a
chrono-stratigraphic scheme for the Late Pleistocene terraces
(SANTORO et alii, 2009). The age of higher terraces is poorly
constrained, but, based on the average uplift rate (~1 mm/a)
deduced from the Tyrrhenian marker (~125 ka BP) and
highlighted by several authors (CUCCI, 2004), conceivably is
tracked back to MIS 15 (~620 ka; see Fig. 1 legend).
Based on the terrace chronology, uplift in the last ~600 ka
was characterized by the alternation of more rapid (~2.2 mm/a)
and slower (~0.6 mm/a) periods of displacement. Besides, spatial
variability in uplift rates is recorded by the deformation profile of
terraces parallel to the coast, which document small-wavelength
(~2-10 km) and amplitude (~10-50 m) local undulations
superposed to the regional uplift pattern, which is the dominant
tectonic signal ((SANTORO et alii, 2009).
The local structures spatially coincide with the last generation
folds and locally with southward-directed left-transpressional
faults mapped in bedrock (CATALANO et alii, 1993; MONACO et
_________________________
(*) Dipartimento di Scienze Geologiche, Università degli Studi di Catania,
enrico.santoro@hotmail.it.
(**) Dipartimento di Scienze della Terra, Università degli Studi di Napoli
Federico II.
(°) INGV, Roma.
(°°) Dipartimento di Scienze Geologiche, Ambientali e Marine, Università
di Trieste.
692
alii, 1998) and locally in Early-Middle Pleistocene fan-delta
deposits, striking orthogonal to the coastline, and involving the
sea-bottom along their offshore extension (Fig. 1; FERRANTI et
alii, 2009). Structural analysis and appraisal of local network
seismicity and regional GPS geodesy suggests that the area is
experiencing transpressional deformation in response to NE-SW
shortening; this explains the origin of the local-scale undulations
in the deformation profile of paleo-shorelines as due to faultrelated
crustal folds (FERRANTI et alii, 2009).
Likewise, based on a morphotectonic analysis of fluvial and
marine terraces, BIANCA &CAPUTO (2003) and CAPUTO et alii
(2010), have as well hypothesized shortening is ongoing in this
sector of the Apennines chain.
Fig. 1 - Morphological map of the Middle Pleistocene–Holocene marine
terraces on the Ionian coast of northern Calabria and eastern Basilicata. The
F75-89 seismic reflection trace is also shown.

The recent tectonic activity of the major faults was supported
by a morphotectonic analysis. We used the SL index, Vf index
and the hypsometric integral in order to identify drainage network
anomalies, and the residual topography and the swath profiles to
characterize the landscape. All the indexes are poorly linked to
lithological and climatic factors, and anomalies were found to be
spatially related to the faults inquired to cause the paleoshorelines
deformation. The greater morphotectonic anomalies
correspond to the maximum deformation zone of the paleoshorelines,
along the southern flank of the Pollino Chain.
On-shore and offshore faults were grouped in geometrically
coherent systems of faults of assigned length, dip and kinematic
parameters. This selection was the basis for a numerical modeling
of the coseismic deformation associated to the transpressional
faults which could reproduce the observed deformation profile of
paleo-shorelines. The model is based on two major assumptions:
a) the earth is assumed to be an elastic half-space; b) the faults
are assumed to be rectangular shaped. The geometrical fault
parameters (strike, plunge, dip, length, width, area, minimum and
maximum depth) were derived from geological cross sections,
offshore seismic reflection profiles and morphological evidences.
The faults rakes were derived from structural, geodetic and
seismic data. We modeled two fault zones (Amendolara Fault
Zone, AMFZ, and Valsinni Fault Zone, VFZ), that, on the base of
the seismic reflection profile F75-89 (trace in Fig. 1), have
accrued a significant vertical displacement and affect Middle
Pleistocene sediments. Pertaining to these two fault zones, 9 fault
segments that cross the marine terraces were modeled.
The good match obtained between the deformed paleoshorelines
and the coseismic model supports the contention that
transpression along the AMFZ and VFZ fault zones can
reasonably explain the marine terraces deformation. Besides, the
local fault-related vertical deformation is less than the 30% of the
total uplift suffered by the coastal area.
Basing on the fault modeling results for the other marine
terraces, we also find that fault activity not only changed through
time for individual faults (and for the cumulative fault array), but
also shifted among single faults. The fault-related uplift rate was
not constant in time but shifted between the AMFZ and the VFZ
fault zones. It seems also that in the last ~80 ka the AMFZ has
accrued the largest deformation. This could explain the greater
morphotectonic anomalies and an apparent spatial clustering of
seismicity that currently characterize the Pollino Chain and the
Amendolara Ridge southern flanks.
Finally, detailed morphometric analysis (river steepness maps
and basin asymmetry analysis) were performed along the major
rivers draining the eastern Pollino flank in order to test and to
improve the proposed deformational model.
A direct comparison with results from CAPUTO et alii (2010)
analysis further north, where uplift rates were found to be greater,
is not possible as yet. However, we remark that what is important
here is the feasibility of the invoked transpression, jointly
693
recorded by us and CAPUTO et alii (2010), in deforming even
very young terraces.
REFERENCES
BIANCA M. & CAPUTO R. (2003) – Analisi morfotettonica ed
evoluzione Quaternaria della Val D’Agri, Appennino
Meridionale. Il Quaternario, 16(2), 158-170.
CAPUTO R., BIANCA M. & D’ONOFRIO R. (2010) – Ionian marine
terraces of Southern Italy: insights into the Quaternary
tectonic evolution of the area. Tectonics,
doi:10.1029/2009TC002625.
CATALANO S., MONACO C., TORTORICI L. & TANSI C.(1993) -
Pleistocene strike-slip tectonics in the Lucanian Apennine
(Southern Italy). Tectonics, 12, 656–665.
CUCCI L. (2004) – Raised marine terraces in the Northern
Calabrian Arc (Southern Italy): a ~600 kyr-long geological
record of regional uplift. Ann. Geophys., 47 (4), 1391-1406.
FERRANTI L., SANTORO E., MAZZELLA M.E., MONACO C. &
MORELLI D. (2009) - Active transpression in the northern
Calabria Apennines, southern Italy. Tectonophysics, 476(1-
2), 226-251.
GVIRTZMAN Z. & NUR A. (2001) - Residual topography,
lithospheric structure and sunken slabs in the central
Mediterranean. Earth Planet. Sci. Lett., 187, 117–130.
MONACO C., TORTORICI L. & PALTRINIERI W. (1998) - Structural
evolution of the Lucanian Apennines, southern Italy. J. Struct.
Geol., 20, 617–638.
SANTORO E., MAZZELLA M.E., FERRANTI L., RANDISI A.,
NAPOLITANO E., RITTNER S. & RADTKE U. (2009) - Raised
coastal terraces along the Ionian Sea coast of northern
Calabria, Italy, suggest space and time variability of tectonic
uplift rates. Quatern. Intern., 206, 78–101.
WESTAWAY R. (1993) - Quaternary uplift of southern Italy. J.
Geophys. Res., 87, 21741–21772.
WORTEL M.J.R. & SPAKMAN W. (2000) - Subduction and slab
detachment in the Mediterranean–Carpathian region.
Science, 290, 1910–1917.
SESSIONE 21

SESSIONE 21
2D and 3D numerical simulations of the present-day state of stress of
the active Ferrara fold-and thrust belt
Key words: Folds, mechanical modelling, Northern Apennines,
stress field, thrust faults.
INTRODUCTION
The present-day state of stress of the active front of the
Northern Apennines buried under the Plio-Pleistocene sediments
of the eatern Po Plain (Ferrara fold-and thrust belt) is investigated
via 2D and 3D mechanical finite elements models. Our main
objective is to explain why the state of stress in the region is
characterized by variations both in depth (Fig. 1) and laterally, as
indicated by focal mechanisms and borehole breakouts
(CARMINATI et alii, 2010).
2D MODELLING
2D models are built on two regional cross sections (Fig.1)
published by CARMINATI et alii (2010) and are used to evaluate
the effects of seismic cycle on the state of stress of the Mirandola
and Ferrara growing anticlines, in order to understand if the
observed along-depth variations of the stress field can be
explained by active tectonics. For this purpose, stick-slip
behavior of the faults is reproduced in our finite element models.
The 2D models adopt, for the intact rock, an elastic rheology
under plane-strain condition. Instead, the fault planes are defined
as weak surfaces following a Coulomb failure criterion.
Geomechanical properties for each formation comprise
Young’s modulus, Poisson’s ratio, density and are assumed on
the basis of published geological data. The models are forced by
1 metre of displacement (applied onto the SW lateral boundary)
directed toward the NE. Such a displacement is expected to
accumulate in 1000 years, according to the present-day plate
kinematics of the Northern Apennines region. To avoid
_________________________
(*) Istituto di Geologia Ambientale e Geoingegneria, CNR, Roma,
v_luigi25@yahoo.it
(**) Dipartimento di Scienze della Terra, Università di Roma “La Sapienza,
eugenio.carminati@uniroma1.it
LUIGI VADACCA (*) & EUGENIO CARMINATI (**)
694
Fig. 1 – Geological cross sections used to build the 2D models (after
CARMINATI et alii, 2010). The topmost section refers to the Mirandola thrustrelated
anticline. The bottom panel depicts a regional cross section
containing both the Mirandola (centre) and the Ferrara (right) structures.
Notice the along-depth stress variation within the Mirandola structure (upper
panel).
convergence problems, tectonic displacement is applied by 0.1
metre step increments.
The stick-slip behavior of the faults is obtained with the
variation of mechanical properties along the faults. In particular,
the friction angle is varied from an unrealistically high value
during the stick (for boundary displacement lower or equal to 0.9
m) to a value near to zero during the slip phase (for boundary
displacement greater than 0.9 m). An example of the tectonic
stress field predicted for the coseismic stage by the model
simulating the regional cross section of the lower panel of Fig. 1
is provided in Fig. 2.
Our modelling results show large variations of the stress state
from preseismic to coseismic stages, both in terms of stress

Fig. 2 – Tectonic stress field predicted for the regional model (lower panel of Fig. 1) after the coseismic slip along the Mirandola structure.
magnitude and orientation. Our modelling allows us to constrain
the variations of the dilation associated with the seismic cycle.
3D MODELLING
A simple 3D numerical model of the Mirandola thrust fault is
built to evaluate the effects of thrust fault rotations on the
regional state of stress, in order to explain its lateral variation.
The geometry is characterized by a basal decollement
characterized by low dip and a ramp with a dip varying from 30°
in its frontal part to 60° in its left lateral part. In the 3D model we
adopt homogeneous mechanical rheology for the whole crust, for
computational sakes. The thrust fault is assumed to be a free
surface of sliding with zero friction. This choice allows us to
correctly simulate uplift rates and slip rates along the Mirandola
structure proposed in the literature (SCROCCA et alii, 2007; DISS
WORKING GROUP, 2009). All numerical results were validated
against active stress field maps available in the literature, built on
seismic and borehole breakout data. Our modelling results
suggest that the lateral variations of the orientation of the
principal stress axes is controlled by the geometry of the thrust
fault.
REFERENCES
CARMINATI E., SCROCCA D. & DOGLIONI C. (2010) -
Compaction-induced stress variations with depth in an active
695
anticline: Northern Apennines, Italy. J. Geophys. Res., 115,
doi:10.1029/2009JB006395.
DISS WORKING GROUP (2009) - Database of Individual
Seismogenic Sources (DISS), Version 3.1.0: A compilation of
potential sources for earthquakes larger than M 5.5 in Italy
and surrounding areas. http://diss.rm.ingv.it/diss/, Istituto
Nazionale di Geofisica e Vulcanologia.
CROCCA D., CARMINATI E., DOGLIONI C. & MARCANTONI D.
(2007) - Slab retreat and active shortening along the centralnorthern
Apennines. In O. Lacombe, J. Lavé, F. Roure and J.
Vergès (Eds) - Thrust belts and foreland basins: From fold
kinematics to hydrocarbon systems. Frontiers in Earth
Sciences, 471-487.
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SESSIONE 21
696

SESSIONE 22
Innovare la didattica delle geo-scienze per educare ad
una cittadinanza responsabile
CONVENERS
Gianfranco Battisti (Università di Trieste)
Michele Stoppa (Università di Trieste)
697
SESSIONE 22

SESSIONE 22
The “Ardito Desio” geopaleontological museum of Rocca di Cave
(Prenestini Mountains, Latium): an example of Earth science
didactics and education
Key words: Apennines, didactics, geosite, museum, Upper
Cretacic.
The “Ardito Desio” Civic GeoPaleontological Museum of
Rocca di Cave is located at the southern margin of the Prenestini
Mountains (Latium), and its geopaleontological collections are
strongly connected to the territory. The Rocca di Cave area has a
great paleogeographic significance since it stands out as the
westernmost end of Upper Cretacic neritic “laziale-abruzzese”
shelf facies. Furthermore, it is the almost unique witness for the
presence of a Cenomanian and Turonian edge in the western part
of the shelf, whose fossil reefs were characterized by typical
associations with dominant bivalves (rudists and others),
gastropods, corals, sponges and rare sea urchins.
The safeguard and the enhancement of the Rocca di Cave
geopaleontological heritage is implemented by several initiatives
and structures linked to the “Ardito Desio” Museum, dedicated
both to the younger visitors and to general public. For school
classes, in the Museum there is an oral presentation together with
direct experience in which boys can touch rocks and fossils,
reaching a higher involvement and pointing to a much wider
interactivity. Last year, almost 5000 visitors (mostly school
classes) have crowd museum’s rooms, in a tour thinked as an
imaginary travel back in time through subsequent jumps, from
recent to Pangea supercontinent age, with detail to the Upper
Cretacic. At the beginning, visitor is introduced to the use of
colours in geology, widely employed in the museum to underline
marks and indicators, so that it can be easily to orientate in the
Earth history and Apennines evolution. The integrated approach
is powered by the presence of 3D-reconstructions and
palaeogeographic globes, adding to the theoretical multimedia
lessons and several posters. The direct observation of the territory
and its morphology is enhanced by the 360°-view obtained from
the Rock’s tower: Apennine reliefs, Albani Hills volcanic
district’s deposits, Campagna Romana, all the visible landscape
elements, accompanied by most relevant toponyms, are reported
_________________________
(*) Dipartimento di Scienze Geologiche, Università degli Studi Roma Tre,
fgrossi@uniroma3.it
CHIARA AMADORI (*) & FRANCESCO GROSSI (*)
698
in a strip placed on all the terrace perimeter.
The guided tour doesn’t stop inside the museum, it continues
along a series of geopaleontological paths evidenced by signs, all
of them around Rocca di Cave. Materials given to the visitors
also include pictures, drawings, explanatory notes referable to the
paths; a part of the graphic products is dedicated to elementary
school and based on comics: representing fossils as protagonists
of funny episodes allows children to approach an unknown world
with elements which they growing up every day together.
In the near future, it’s planned to improve both the didactic
material dedicated to the outcrops, and the number of paths; this
last goal is included in a broader project provides for the
realization of a southern Prenestini Mountains natural trails map.
In advanced completion projects there is the first issue of the
scientific journal linked to the Museum, providing insights on
topics closely correlated to the Rocca di Cave geology and
paleontology, besides divulgation columns and general geological
interest topics. Again, particular attention is directed to younger
readers, with a central double page full of games, cartoons and
comics.
The geosites conservation and the knowledge organization in
museums should be flanked by the growing attempt to approach
both adult citizens and younger one to the Italian natural heritage,
thus to educate citizenship much more responsible, mature and
careful to environmental respect and to its history.

Key words: Didactics of geosciences, energy, environmental
issue, geography, geosciences, land use planning.
The headlines of the last decade have accustomed us to
understanding that the energy issue is one of the most important
challenges mankind is facing today. The debate between the
supporters of renewable and non-renewable energy sources, of
“clean” energy and of the one deriving from fossil fuels,
especially in the context of the global warming, has long gone
out the restricted circle of academic discussion to concern,
through the mass media, the man on the street.
What is clear however, beyond the clamour arisen around the
different theses, is the general disinformation on this issue. A
closer look reveals it is the consequence of a lack of basic
knowledge due to a general carelessness of the school institutions
at the various levels. Even at the top level - university - only three
faculties out of the twelve of our university system offer a range
of courses which deal in a certain way with this question, namely
the Faculty of Engineering, the Faculty of Mathematical, Physical
and Natural Sciences and the Faculty of Economics, none of
which is able to give all the competences required on its own.
The energetic sector is in fact a typical interdisciplinary sector
and as such it does not fit well into an organisation of knowledge
founded on an atomization of themes in contexts which
traditionally tend to be autonomous. Only Geography, at school
level, and to a lesser extent Ecology, at university, do aim at
covering the whole issue, although with the collective effort of
the concerned teachers and professors.
So the question is which disciplines can study the issue in the
best possible way. At school level, not considering the Industrial
Technical School, it is the teachers of Chemistry and Natural
Sciences who are usually very active and propose the topic within
their lessons or in the framework of programmes for
environmental education, often carried out with the cooperation
of external educational agencies such as WWF and the like.
As a matter of fact, however, this issue cannot be
_________________________
Teaching geography of energy, not just an educational issue
(*) Dipartimento di Scienze della Formazione e dei Processi Culturali,
Università di Trieste, gbattisti@units.it
Paper prepared within the research activity furthered by the P.I.D.D.AM. at
the Dept. of Scienze della Formazione e dei Processi Culturali under the aegis
of CIRD, University of Trieste.
GIANFRANCO BATTISTI (*)
699
encompassed solely within the realm of natural sciences since it
also comprises relevant questions of an economic character which
are of paramount importance to determine the various options.
Nowadays we can select from a wide range of technological
solutions and only in the most disadvantaged areas are we
compelled to choose the only available solution, as is the case for
example of certain African peoples who still depend solely on
burning wood.
The choice among different technologies requires the
adoption of rather complex calculation methods, with reference to
different disciplinary corpuses related to economic and social
sciences. Furthermore, the concrete choice between different
energy sources, both primary and secondary, imply the recourse
to different environments and kinds of intervention, with
consequently different results. A thermoelectric plant, for
example, can be fuelled either by coal or gas. In the latter case,
the fuel can be conveyed through a gas pipeline or a
regassificator, which in turn can be located either at sea or on the
coast. The assessment of these aspects requires the indispensable
competences not only of geologists but also of land use planners.
Owing to the wide range of problems at stake, the proposal to
create a specific teaching sector which has been put forward at a
recent presentation of an Atlas of Energy for the schools in
Rome, does not seem peculiar at all.
All things considered, integral Geography appear to have
arms wide enough to contain the whole energy issue. This in
virtue of its consolidated attitude of concerning itself with all the
phenomena which can be observed on and - if necessary - under
the surface of the earth, a characteristic which is at the same time
its strength and its weakness.
But there is a further reason to claim this role, namely the fact
that geographical phenomena represent different sets of
phenomena in increasing numbers which are to be considered as a
whole. In their interaction they contribute to describe the several
parts of the earth as consociations recognizable at different
scales, now linked by homogeneity, now by functional links.
Being able to treat simultaneously phenomena pertaining to
the physical and human life alike, Geography is a sort of linking
science between different sectors of knowledge, often more
advanced in their own scope but separated by a divide of a
conceptual nature. As such, Geography can overcome some of the
limits posed by the specialization of the different disciplines.
Some of these aspects are typical of the energy issue. Let’s
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SESSIONE 22
take the vexata quaestio of the oil reserves, very lively debated in
particular in the light of theories such as the Hubbert curve. In
reality, as has been proved by a researcher in Trieste, the reserves
of hydrocarbons of multinationals are growths influenced more
by the dynamics of the quotation of the barrel than by the result
of prospecting. In a similar way, the economic results of the oil
refining companies strictly depend on their possibility of
operating on the Stock Exchange, what in turn influences the
location of their plants on the globe.
All this is a consequence of the growing financialisation of
economy and therefore of its globalisation, which cannot but
determine a progressive crisis of any form of geographicalenvironmental
determinism. The existence of resources
geographically located, as all mineral resources are, and
economically accessible does not represent any longer a sufficient
prerequisite for their exploitation, nor can it be any longer
considered an hindrance to the setting up of new productions
which require them. Let us consider the export of oil from the
United States to Russia and the beginning of the steel industry in
the north of Italy, both taking place in the second half of the
nineteenth century, at the time of what Fumian calls “the first
globalization”.
It is then clear how complex are the reasons underlying any
choice concerning energy sources, technologies related,
localisation of plants and supply of the different markets. Not
knowing the past and deprived of the essential information, the
man on the street - who is yesterday’s student - is left with
practically no critical weapon to face the media bombing which
risks confusing him even more.
An isolated exam of the middle- and long term markets, of
environmental issues, the role of different technologies, the
actions of oilmen, farmers, and producers of alternative energy
plants, as is often carried out by many “experts”, even from the
academic world, can only trouble waters. Hence the need for the
scientists working in the field of Geosciences to dialogue with
each other in order to decode reality and prepare on this basis a
new generation of teachers. This way the now exceptionally high
risk might be avoided of having teachers who, without realising it
themselves, just act as propagandists spreading the interpretations
of reality which have been adopted by the strategic plans of the
industries of the sector.
It is a hard task which requires first and foremost a specific
in-depth analysis, such as the one which has been carried out by
the Working Group set up within the Association of Italian
Geographers (A.Ge.I.) since 1990 with the cooperation of
professors and researchers working in different universities in
Italy as well as of scholars not belonging to the academic world.
There is no doubt, however, that the solution of the issue will have to
be found through a closer cooperation among all the disciplines now
operating within the strategic sector of Geosciences.
700

Key words: Karst, lectures, powerpoint, speleology, teaching.
INTRODUCTION
Karst studies and speleology are increasingly important in the
scientific community finding applications in fields such as
hydrogeology (GOLDSCHEIDER & DREW, 2007), natural and
anthropogenic hazards (PARISE et alii, 2008, 2009),
geomorphology (DE WAELE et alii, 2009), mineralogy (HILL &
FORTI, 1997), biology (CULVER &PIPAN, 2009), microbiology
(BARTON, 2006), palaeoclimatology (GENTY, 2008) and many
others topics. However, these scientific resources are often not
easily accessible to non-scientists and cannot be directly used for
education purposes. Also the many textbooks on speleogenesis,
karst geomorphology and hydrology or the two major
encyclopaedia on the subject are not suitable for teaching
speleology and karst to non-scientists. Only the recent book by
Art Palmer is definitely a step forward towards science education
suitable to a wider public (PALMER, 2007).
Education is an extremely important issue in karst protection.
Early efforts in finding a way of teaching karst to non-scientists
go back to the late 70’s and 80’s (PALMER, 1984). Especially
karst-related hazards are suitable topics that can be profitably
used to teach the peculiarity of the karst environment to local
communities. There are many examples of booklets that explain
the fragile karst environment to the students, citizens and agency
personnel (VENI et alii, 2001; ZOKAITES, 1997).
Teaching karst science to cavers is important because of the
extraordinary work they carry out as an essential part of scientific
studies carried out in caves and karst areas. An example is given
by tracer tests, in which dyes are injected in cave streams deep
inside the mountains and later detected, often in an automatic
way, at the karst springs (GOLDSCHEIDER et alii., 2008).
To allow cavers to become an active part in the scientific
researches carried out in karst areas and caves they have to train
_________________________
Teaching resources in speleology and karst: a set of useful online
powerpoint lectures created by the Italian Speleological Society
(*) Istituto Italiano di Speleologia, jo.dewaele@unibo.it
Lavoro eseguito nell’ambito del progetto “Powerpoint” della Società
Speleologica Italiana.
JO DE WAELE (*)
701
themselves and become familiar with science.
In this way they will not only perform simple tasks such as
drilling speleothems or catching cave beetles, but can become
responsible of choosing the right sites, collecting samples in the
correct way, or record all types of chemical and physical data
from sometimes complex monitoring devices.
In order to bring some of this science closer to the
speleological community, a three year project has been launched
at the end of 2006 by the Italian Speleological Society (SSI) (DE
WAELE, 2010) and carried out under the umbrella of the Union
International de Spéléologie (UIS) and is here described.
METHODS
Lectures on over 50 topics have been prepared as computer
presentations. Each lecture is composed of a number of slides,
ranging between 19 and 147, starting with a title slide and ending
with two slides containing bibliographical references and credits
respectively.
All cited references are available in the SSI library at Bologna
and normally are review articles or important text books. Lectures
are composed by experts in their fields, who often have involved
several collaborators among colleague scientists, photographers
and designers. More than 100 cavers have in some way
contributed to the scientific contents of the slides, while
photographs have been provided by more than 300 persons.
Because most of the experts and collaborators are Italian, also
many examples are related to this country. Nevertheless general
contents are valid globally, and if the user wants to change
examples and pictures in the lecture this can be easily achieved,
rendering the lectures more country specific.
Slides have a black background and a footnote reporting the
lecture and the symbol of the SSI. Font is Verdana, 20 for main
text, 32 for titles and 10 for photo and figure captions. Font
colour is always white or yellow. The font type and colour and
the background have been decided to allow a comfortable view
also to people with sight problems (e.g. people with daltonism).
All slides and lectures have been peer reviewed and typeset by a
pool of correctors-designers before final submission. Final Italian
versions have then been translated by mother tongues in English,
French and Spanish.
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SESSIONE 22
RESULTS
After almost three years of intense work a total of 58 lectures
have been prepared. The entire package, called “Teaching
resources in Speleology and Karst 2009”, has been presented in
an incomplete version on a DVD during the 19 th International
Congress of Speleology at Kerrville in July 2009 thanks to the
financial support of the National Cave and Karst Research
Institute of Carlsbad, USA. Since the end of the Congress a
remaining part of lectures was finalised and most were translated
into English, French and Spanish and have been posted on a
website of the Italian Speleological Society
(http://document.speleo.it/). After registration, the lecture files
can be downloaded for free.
The files are meant to be used for educational purposes at all
levels, from primary schools to universities, as long as the
original source is mentioned. The files may be enriched with new
slides (e.g. examples of the region in which the lecture will be
given) or the slides may be extracted from different presentations
to compose an entirely new lecture. It is of course the
responsibility of the lecturer to leave the content of the single
slides unaltered. If the scientific contents of slides are changed,
these modifications should be clearly reported.
All lectures can be improved adding new slides, considering
new topics, changing photographs and figures and so on. It is
desirable that such improvements are reported to the editor of the
entire package in order to continuously update the lectures and
the website. Also suggestions and constructive criticism will
surely help us improving the quality of the product. Finally, the
presentations may be translated into other languages such as
Portuguese, German and many others. These further versions
could also find a natural place in the SSI website.
ACKNOWLEDGEMENTS
This abstract resumes the work carried out by over 300 cavers
and scientists that have, in some way or another, contributed to its
finalisation. Special thanks to Paolo Forti, who came up with the
idea, Francesco Maurano who has given an hand in the
technological (computer) sense, the layout and correction team
composed of Mauro Kraus, Franco Gherlizza and Marilena Rodi
and the coordinators of the English, French and Spanish versions,
respectively David J. Lowe, Philippe Audra and José Maria
Calaforra together with their many translators. Also the National
Cave and Karst Research Institute and the Union International de
Spéléologie are thanked for their efforts in getting the DVD out
702
in time for the 19 th ICS at Kerrville. Finally the help of the Italian
Speleological Society has been greatly appreciated.
REFERENCES
BARTON H. (2006) - Introduction to cave microbiology: an
review for the non-specialist. J. Cave Karst Stud., 68, 43-54.
CULVER D.C. & PIPAN T. (2009) - The Biology of Caves and
Other Subterranean Habitats. Oxford Univ. Press, 256 pp.
DE WAELE J. (2009) – Teaching resources in Speleology and
Karst. Intern. J. Speleol., 39(1), 29-33.
DE WAELE J., PLAN L. & AUDRA P. (2009) - Recent
developments in surface and subsurface karst
geomorphology. Geomorphology, 106, 1-8.
GENTY D. (2008) - Palaeoclimate special issue: an introduction.
Intern. J. Speleol., 37, I-IV.
GOLDSCHEIDER N. & DREW D. (2007) - Methods in Karst
Hydrogeology. Taylor & Francis, London, 264 pp.
GOLDSCHEIDER N., MEIMAN J., PRONK M. & SMART C. (2008) -
Tracer tests in karst hydrogeology and speleology. Intern. J.
Speleol., 37(1), 27-40.
HILL C.A. & FORTI P. (1997) - Cave minerals of the World.
Nation. Speleol. Soc., Huntsville, Alabama, USA, 463 pp.
PALMER A.N. (1984) - Recent trends in karst geomorphology. J.
Geosci. Edu., 32, 247–253.
PALMER A.N. (2007) - Cave Geology. Cave Books, Dayton,
Ohio, USA, 454 pp.
PARISE M., DE WAELE J. & GUTIERREZ F. (2008) - Engineering
and environmental problems in karst. Eng. Geol., 99, 91-94.
PARISE M., DE WAELE J. & GUTIERREZ F. (2009) - Current
perspectives on the environmental impacts and hazards in
karst areas. Environ. Geol., 58, 235-237.
VENI G., DUCHENE H., CRAWFORD N.C., GROVES C.G., HUPPERT
G.H., KASTNING E.H., OLSON R. & WHEELER B.J. (2001) -
Living with karst: a fragile foundation. Am. Geol. Inst., 64
pp.
ZOKAITES C. (1997) - Living on Karst: a reference guide for
landowners in limestone regions. Cave Conservancy of the
Virginias, Richmond, 26 pp.

Key words: Analysis and curriculum design, didactics of
geosciences, didactic research, first grade secondary school,
initial and recurrent education of secondary school teachers,
second grade secondary school.
Disciplinary didactics might be defined as a science aimed at
optimizing the teaching and learning processes of any single
discipline within a well determined educational frame. One can
immediately realize how complex this is in the case of the
didactics of geosciences, it being a sort of multidisciplinary
didactics or, more precisely, a rather varied cluster of disciplinary
didactics not necessarily homogeneous nor convergent from an
epistemological point of view.
In essence, the unifying point in such an apparently disparate
set is to be found in the sharing of the scientific method, not used
in a general way, but modulated according to the manifold
epistemology required by the way chosen every time to explore
the fascinating secrets preserved by our planet from different but
complementary perspectives.
Since they are to be articulated aggregates of didactic
knowledge, each one independent from the others, the first issue
to tackle is how to make them dialogue and mutually interact with
satisfying results.
To this purpose we would have to harmonize the teaching
processes of the corresponding disciplines in the domain of
geosciences, integrating their peculiar knowledge and
competences to effectively share an interesting heritage of
common goals.
Such a cooperation would first and foremost make it
necessary a careful assessment of the reciprocal propaedeutics,
which would still have to be respected, together with an attitude
of constructive dialogue among the disciplines. At an
epistemological level, this is correctly called for from many sides
but it is of course quite difficult to put into practice in the actual
everyday didactics. The command of basic knowledge in the field
of geosciences is proving in many geological contexts a decisive
_________________________
The didactics of geosciences at secondary schools:
state of the art and future perspectives
(*) Dipartimento di Scienze della Formazione e dei Processi Culturali,
Università di Trieste, michele.stoppa@dsgs.units.it.
Paper prepared within the research activity furthered by the P.I.D.D.AM. at the
Dept. of Scienze della Formazione e dei Processi Culturali under the aegis of
CIRD, University of Trieste.
GIOVANNI GIURCO (*) & MICHELE STOPPA (*)
703
factor for the survival of settlements, at the same time promoting
a more reasonable and substantial management of the territorial
system concerned. It represents therefore a valuable, highly
significant heritage capable of giving rise to an adequate culture
of citizenship.
This citizenship we all seem to agree upon, however, is not
always followed by coherent facts and efficient educational
processes, in particular in the world of the school, and above all
of the secondary school. It appears increasingly important to fight
with all our strength so that at least the basic knowledge of
geosciences and in particular that related to the themes of
environmental danger and sustainable management of georesources
is taught well enough in the schools.
As for the first grade secondary schools, to understand the
state of the art it is essential to study the present “Indications for
the Curricula for Nursery School and Primary School”, though
they are probably going to be revised shortly.
The situation of the second grade secondary schools appears
to be more complex and dynamic according to the drafts of the
“National Indications of the Specific Learning Aims for the
Licei” and the Guidelines containing the “Worksheets for the
Disciplines of the first two years of the Technical School”
recently released by the Italian Ministry of Education.
From these documents it can be easily inferred that at
secondary level geosciences do not merge into a new,
independent discipline taught by a specialized teacher, nor will
they in the future. The contents of geosciences are divided in fact
between two disciplines: “integral” Geography and “integral”
Sciences, although under different names in different types of
school, as a consequence of the many reforms which the national
system of education has been through over the last decade. These
disciplines are warmly invited to cooperate in a deep, fruitful
interdisciplinary approach, undoubtedly a valuable chance for
geo-sciences.
This paper aims at presenting a proposal for a vertical
interdisciplinary curriculum of geosciences able to give students
not only an adequate command of the main competences in the
sector but also the opportunity to discover in practice if they
would like and have the prerequisites to continue in this study at
university level.
It is an ambitious goal, considering the unrelenting, often
frankly unfair insensibility towards the geosciences, in particular
Geography. Beyond the encouraging statements pronounced in
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SESSIONE 22
official occasions when catastrophes take place, to pursue this
goal would make it necessary on part of the scholars who
recognize themselves as members of this wide family of
disciplines to ponder the meaningfulness and the intensity with
which the contents of geosciences are to be conveyed to
university students who are preparing to enter the career of
teachers.
It is also necessary to make a more motivated choice both of
the key contents to be transmitted, although always respecting
their traditional propaedeutics, and above all of new teaching
methods, in particular in the light of the didactics performed in
workshops and on the field, so as to weave a supporting tissue of
sound environmental awareness on which to found and to
promote sustainable lifestyles in a framework, as much as
possible, of a more generalized environmental safety.
704

Geoscience for the challenge of the technical and scientific
knowledge at the University “G. d’Annunzio” of Chieti-Pescara
ENRICO MICCADEI (*), SEBASTIANO MISCIA (*), LEANDRO D’ALESSANDRO (*), MILENA IMPICCIATORE (*),
TOMMASO PIACENTINI (*), MAURIZIO PREZIUSO (**) & GIANLUCA ESPOSITO (°)
Key words: Geoscience education, Upper School students,
Abruzzo region.
INTRODUCTION
The University “G. d’Annunzio” of Chieti-Pescara is working,
since 2007, on the educational project “Challenge of the
Technical and Scientific knowledge” (http://ots.udanet.it/), within
the Project RECOTESSC of the Abruzzo Region (PO FSE 2007-
2013, Piano Operativo 2007-2008), whose main purpose is to
arise the sensibility of Upper School students to different
branches of technical and scientific knowledge (Geology,
Mathematics, Chemistry, Physics and Biology).
Within the Geology field, the project is aimed at with lections
and lab work, web based activities and games, and particularly
with field excursions held according to the guidelines of Italian
Association for Geology and Tourism. The project has involved
at least 1000 students pertaining to the geology field.
LECTURES AND LAB WORK
Lectures and lab work are focused on two main points: 1)
provide to the students a contribution to a new knowledge and
sensibility of their living territory Geology; 2) illustrate and
discuss the basic tools for the study of Geoscience and landscape.
With this aim the lectures are based on the discussion of the
geology and geomorphology of the students’ living province
within the Abruzzo region. By means of a voyage through the
geological history and through the “spiral” of the geological time,
the main branches of the Geoscience are outlined with their
specific role and field of application within a well known and
daily living environment.
_________________________
(*) DIGAT Università degli Studi "G. D'Annunzio" di Chieti-Pescara,
tpiacentini@gmail.com
(**) Ud'Anet s.r.l.
(°) Via Marche, 10 (Cepagatti, PE)
Work within and with the financial support of the project "La scommessa
del sapere tecnico scientifico", funded by FSE within the multi-axis project
RECOTESSC (PO FSE 2007-2013, Piano Operativo 2007-2008) of the
Abruzzo Region.
705
The living territory is shown to lectures attendants through
new eyes and described as the result of a the 200 millions years
long geological and geomorphological history of Central Italy.
The resulting landscape is presented as a highly dynamic
equilibrium surface, between processes developed below the
earth surface (endogenous) and those developed above the earth
surface (exogenous). From this view of the landscape we tried to
promote the comprehension of the geological risks and resources
as natural result of a dynamic environment, that is to be well
known in order to safely live in it.
The main themes of the Year of the Planet Earth
(http://www.yearofplanetearth.org/) provide a guideline for the
main discussions with the students, concerning the new frontiers
and applications of Geoscience and new challenges that it will
face for accompanying the near future of our society.
The lab work are focused mainly on the analysis and
comprehension of maps as basic tool for Geoscience and
environmental studies. New technologies of digital mapping by
means of Geographic Information Systems are also presented.
Exercises of basic analysis and interpretation of topographic
maps and geological maps are carried on, using maps of the
students’ living territory. These exercises stimulate always wide
discussions over the use and application of geological maps in
land use and management at different scales, from local to
regional and on different themes of the Geoscience both in
application and scientific environment.
WEB BASED ACTIVITIES AND GAMES
Lectures and lab work have been supported by different types
of web games e web based activities, such as crosswords,
conceptual maps, quizzes and particularly a scientific grandprix
with prizes at the end. These activities are aimed at stimulating
the comprehension of the topics discussed in the classroom.
EXCURSIONS
For a better comprehension of the daily living landscape from
the geologists’ viewpoint and of the peculiarity of the geoscience
within the other scientific disciplines, the students involved in the
project have been “taken out of the classrooms” organizing
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SESSIONE 22
Fig. 1 – Geological field excursion. a) Field excursion in the Sulmona Basin; students analysing the triangular facets along the Monte Morrone fault slope. b)
Field excursion at the Tremiti Islands; students observing active cliffs along the islands coast.
specific field trips and geological excursions (Fig. 1). In these
field trips the students are “Geologist for one day”, working on
their landscape with the field tools of geology and landscape
analysis, such as maps, hammer, compass, lens and “eyes”.
To date, several excursions have been planned in the Abruzzo
Region. In the mountain areas field excursion have been held: in
the Marsica area, illustrating the remnants of ancient landscapes
and Mesozoic paleogeographies and the recent evolution of
ridges and valleys; in the Sulmona basin, illustrating the evolution
of a landscape due to tectonics and Quaternary climate
fluctuations. In the hilly piedmont area excursions have been
held: in the Pescara hinterland (Penne) and in the Chieti town,
illustrating the Pleistocene geomorphological history since the
emersion of the area from marine environment and the recent
dynamics of rivers and landslides with related risks. In the coastal
and islands area excursions have been planned: in the southern
Abruzzo rocky coast, illustrating the geological evolution related
to Pleistocene uplift and marine processes, and the recent
dynamics of beaches and active and inactive cliffs due to aeolian
processes, marine processes and landslides; in the Tremiti Islands
(offshore the southern Abruzzo coast but actually in the Puglia
Region), illustrating the complex interaction among marine, karst,
fluvial and weathering processes in the geomorphological
evolution of an area that since the Pleistocene was alternatively
connected and not connected to the Italy coast owing to sea level
fluctuations.
CONCLUSION
The final purpose of the project, particularly concerning the
Geology, is multiple: 1) specifically concerning Geoscience, give
rise the student attending the project’s activities to learn a way of
looking at and knowing their territory with new eyes and a new
awareness to natural geological and human induced dynamics that
define landscape changes and geological risk and resources; 2) in
a more general view, increase the young people sensitivity to
different branches of technical and scientific knowledge; 3) in
more wide sphere with reference to main themes of the Year of
706
the Planet Earth, provide a contribution for the comprehension of
the role of Geoscience for the Society.

Key words: Environment, landscape, integrated approach and
creative activity.
Knowledge of environment and landscape requires
methodologies, techniques and tools appropriate, which allow to
acquire and process spatial data represented as expressive codes
easily recognizable.
The environment is, primarily, a "space" or territory, which
enables and influences the life and activities of people; it is a
complex assemblage of components; some of those are natural
(geomorphology, bio-climatic, weather, climate, water, etc..),
others are determined by man (agricultural settlements,
residential, manufacturing, infrastructure, etc..), and there is a
dynamic process of relationships between them.
The characteristics of landscape, as perceived by people, is a
consequence of natural and/or human actions and their
interrelationships. The landscape study must necessarily be
performed by means of an integrated approach, whether pursuing
analysis of perceptual quality of the scenery, whether pursuing
scientific investigations considering all the factors (physical,
chemical, biological and socio-cultural) as open sets with
continuous dynamic relationships.
Therefore, the main objective of the course was to give to the
pupils an overall and comprehensive approach to the techniques,
tools and methodologies for reading, interpretation and
representation of the landscape and the environment.
In order to facilitate learning of the designed objectives,
simple simulations and/or examples were initially used. In
particular, the methodology was to relate, first, the history of the
Earth (4.5 billion years) to a cycle of one year, showing for each
month the main stages of the evolution of Planet Earth and living
organisms. The main purpose was to convey the basic concepts
related to the solar system, the geological phenomena, the birth
and evolution of the Earth, to the structural characteristics and
evolution of the Earth and endogenous processes.
Earth is alive, and our planet, in fact, is changing: as living
beings the rocks born, move, change and die. Outset were also
inputs data regarding the preservation of our planet and the
environment following perspectives and points of view.
_________________________
An enchanted garden called "Planet Earth"
(*) Autorità di Bacino Regionale, Regione Calabria,
an.pellegrino@regcal.it
ANNAMARIA PELLEGRINO (*)
707
Later, issues concerning the exogenous processes, natural
environment, weathering, erosion and selective formation of
soils, slope and landscape morphology were addressed.
Fig.1:a)header PON Project F1 ;b)calendar of the Earth.
A third part of the program was made to reach the definition of
environment and ecosystem, related to the anthropomorphic
activity: a brief introduction to the characteristics of an
ecosystem, the concept of habitat and illustration of examples of
environmental changes due to the activities of men. These topics
were followed by a guided tour of the Wildlife Recovery Centre
(CRAS) and the Mediterranean Biodiversity Park of Catanzaro.
The Park represents a centre of excellence and synthesis among
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SESSIONE 22
mineral, vegetable and animal worlds by anthropogenic activity;
it is the expression of a positive impact on land and environment
through the recovery of severely degraded areas. The main
purpose was to understand that the Earth is the cradle of life, that
every natural environment is a small world, with typical animals
and plants which are impossible to find elsewhere.
Finally, in order to promote environmental awareness
guidelines for the acquisition of habits of protecting, promoting
and respecting the 'environment, the reflection on the relationship
between man and environment and attractiveness of natural
balances have been launched. Themes about the identification of
human behavior on pollution, types of waste, recycling and
awareness-raising, the water cycle and its use in ecological
dimension, recycling and renewable energy cleaned were well
developed. Within this framework comic books and drawings on
the themes planned have been used.
Fig.2: Synthesis model of the issues addressed during the course.
Furthermore, a creative activity was conducted by means the
projection of video and photo report consulting websites for
dissemination purpose/planning, the implementation of Posters,
calendar of the Earth (Evolution of Planet in twelve months;
Fig.1) and of a “synthesis model” (Fig.2). The model, also,
contains: components and four "powers" of nature; tracks of
Earth fruits from mineral, vegetable and animal world. “Powers"
of nature represent energy sources such as fire, water, air and
earth, giving rise to endogenous- exogenous processes and life on
earth; these renewing sources make the world evolving.
708
Tracks of earth fruits were represented in the form of layers
which recall the geological evolution of the earth and then in its
every aspect and its living beings. Mineral (stones and sand),
plant (flowers and leaves) and animal (shells and fossils)
Kingdom is represented as a balanced relationship, as living and
nonliving beings, which constitute the ecosystem that must be
safeguarded.
It should be emphasized that the creative activity was,
primarily, aimed at communication of the message: be able to
interact with conscious and positive environment in which we
live.
REFERENCES
PELLEGRINO A. (2009)- “Il giardino incantato”. Scuola Aldisio-Rodari di
Catanzaro 1° CIRCOLO, Programma Operativo Nazionale 2007/2013 IT 05
I PO 007 “Competenze per lo sviluppo” finanziato con il Fondo Sociale
Europeo.

Key words: Didactics of geosciences, didactic research, didactic
workshop, education to environmental sustainability,
P.I.D.D.AM., standing education, supplementary education,
teachers’ training, territorial didactics, university didactics.
The standing workshop to promote and innovate the didactics
of geographical, environmental and territory disciplines (Italian
acronym: P.I.D.D.AM.) was born within the former Dept. of
Geographical and Historical Sciences (now Dept. of Sciences of
Education and Cultural Processes).
It soon began to operate under the aegis of CIRD, the
Interdepartmental Centre for Didactic Research, University of
Trieste. Among its purposes there were also the rationalization
and improvement of the conspicuous heritage of activities
traditionally offered to support the university courses in the fields
of geography and environment. Particular attention was given to
the courses of disciplinary didactics given by the Faculty of
Education (Science della Formazione), degrees in land-use
planning (Politica del Territorio), located in Gorizia, Education
Sciences and Primary Teachers’ Education (Scienze della
Formazione Primaria) as well as the linguistic and literary area of
the School for Secondary Teachers’ Education (S.I.S.S.).
Since its beginning in 2003, the PIDDAM workshop has been
pursuing the following ends:
- encouraging university professors to meet and interact with
school teachers at all levels, environmental educators, experts and
professionals engaged in the same fields of interest. The goal is to
create opportunities to cooperate, so as to implement the quality
of environmental research and didactics, stimulate best practices,
enhance off environmental goods and use them in sustainable
ways;
- developing scientific and didactic research towards an
interdisciplinary perspective of integration, synergy and holism.
The main issue is to lead them to experience innovation in the
scientific disciplines and their didactics in the universities, at
schools and in private education agencies;
_________________________
The didactics of geosciences at the university:
the experience of the P.I.D.D.AM. standing workshop
(*) Dipartimento di Scienze della Formazione e dei Processi Culturali,
Università di Trieste, michele.stoppa@dsgs.units.it
Paper prepared within the research activity furthered by the P.I.D.D.AM. at the
Dept. of Scienze della Formazione e dei Processi Culturali under the aegis of
CIRD, University of Trieste.
MICHELE STOPPA (*)
709
- promoting the updating and standing education of teachers
and professionals engaged in the management of territorial
systems;
- spreading a well established geographical and environmental
culture through the awakening of public opinion as to the need of
collective behaviours coherent to a sustainable management of
territorial complexes.
To reach such ambitious goals the standing workshop is
operating at the same time in the fields of research and that of
didactics, following a sinergically combination of “general” and
didactical research, steering them both towards a subsequent
didactic testing of the innovations. Some outcomes of the
research carried out, directly referred to Geosciences, are listed
below in the bibliography.
As for the didactics, the workshop is active on three strategic
directions: supplementary education, standing education and
teachers’ training. For a comprehensive, detailed outline of the
activity performed, go to the official site:
http://scfor2s.units.it/scfor/docwww/dsgs/PIDDAM/.
SESSIONE 22

SESSIONE 22
710

SESSIONE 23
Stratigrafia e analisi di bacino: eventi globali ed effetti
della tettonica regionale
CONVENERS
Renzo Valloni (Università di Parma)
711
SESSIONE 23

SESSIONE 23
The Salerno Valley (Campania continental margin, Italy):
stratigraphic and structural styles and morpho-bathymetry of a
Pleistocene half-graben
Key words: Continental margin, half-graben, Multibeam
bathymetry, reflection seismics, Salerno Valley.
INTRODUCTION
Some new results on the seismic stratigraphy and morphobathymetry
of the Pleistocene sedimentary basin of the Salerno
Valley, framed in the regional seismic stratigraphy of the passive
continental margin off southern Campania (Southern Tyrrhenian
sea, Italy) are here presented. The original data include a
Multibeam bathymetric survey of the Salerno Valley and
multichannel and single channel seismic profiles, recently
acquired onboard of the R/V Urania of the National Research
Council of Italy (SISTERII oceanographic cruise). These data
have been interpreted in order to investigate the tectonosedimentary
evolution of the basin during the Pleistocene. This
area represents a good example for a better understanding of the
geologic evolution of the extensional sedimentary basin offshore
the southern Italy.
MORPHO-BATHYMETRY
The morpho-bathymetry of the sedimentary basins represents
a research line of increasing interest, mainly for its implications
for the monitoring of the deep and coastal environment and in
terms of the definition of the geologic and environmental hazards.
The Multibeam bathymetric data recorded during the
SISTERII oceanographic cruise have shown high gradients of the
continental slope and the occurrence of erosional processes,
mainly at the toe of the slope, where a dense network of tributary
channels has been recognised. The analysis of seismic profiles
has evidenced the tectonic activity along the fault escarpment as
one of the most important triggering causes of the gravity
_________________________
GEMMA AIELLO (*), ENNIO MARSELLA (*), VINCENZO DI FIORE (*) & CLAUDIO D’ISANTO (**)
(*) IAMC – CNR (Istituto per l’Ambiente Marino Costiero) Napoli,
gemma.aiello@iamc.cnr.it
(**) Impresub s.p.a., Trento
712
submarine instability processes active during the Late Pleistocene
and the Holocene. This interpretation is also confirmed by slump
deposits, characterised by a chaotic seismic facies, interstratified
at several stratigraphic levels in the basin filling. On the contrary,
in the distal zones of the valley, where the deposition prevails, the
shallower sectors appear to be in erosion (Salerno Valley) and
show recent tectonic deformations, as antiforms and normal
faults, which are interpreted, in the regional setting of the area, as
hints of a strong synsedimentary tectonics, lasting up to recent
times (AIELLO et alii, 1997a; 1997b).
The Multibeam bathymetric data have allowed for the
reconstruction of a three-dimensional DTM, covering an area of
1600 kmq between the southern coast of the Capri island to the
north-west and the Sele river mouth to the south-east.
The continental shelf of the Salerno Gulf shows a marked
asymmetry proceeding from north to south, reflecting the
different structural domains of this sector of the Apennines chain.
The variability of the extension, of the depth of the shelf break
and of the average width of the slopes is controlled by the
geologic and structural setting of the marginal areas (BARTOLE et
alii, 1983), more than to the glacio-eustatic variations during the
Pleistocene. The continental slope surrounding the Salerno Gulf
is characterised by structural depocenters having a NW-SE
(Apenninic) trending, originated by the extensional tectonic
phases related to the Tyrrhenian basin, alternating with morphostructural
highs, adjacent to intra-slope basins. In particular, two
complex morpho-structural highs, having a NE-SO trending have
been identified.
TECTONO-STRATIGRAPHIC SETTING
The Salerno Valley is a Pleistocene half-graben, whose
identification and tectonic setting have been controlled by a
normal fault, characterised by a probable strike-slip component.
This fault has controlled the origin of the Salerno canyon,
showing erosional processes which are still active and
synsedimentary tectonics. The acoustic basement is composed of
Mesozoic carbonate platform units (drilled by the deep
lithostratigraphic wells “Mina 1”, “Margherita Mare 1” and
“Milena 1”) and by the overlying Miocene siliciclastic units
genetically related to the “Liguride Units” and to the Miocene

foredeep deposits (“Flysch del Cilento”), widely cropping out
onshore in the Cilento Promontory.
Fig. 1: Geological interpretation of the multichannel seismic profile L6. Key. 1:
Meso-Cenozoic platform carbonates. 2: Relic shelf prograding wedges (Early
Pleistocene). 3: First seismic sequence onlapping the B unconformity 4:
Second seismic sequence with inclined reflectors on the slope and parallel
reflectors in the basin. 5: Third seismic sequence with inclined reflectors on
the slope and parallel in the basin. 6: Fourth seismic sequence with inclined
reflectors on the slope and parallel reflectors in the basin. 7: Fifth seismic
sequence, with a wedge-shaped external geometry and onlapping the F
unconformity 8: Sixth seismic sequence with inclined reflectors on the slope
and parallel reflectors in the basin. 9: Seventh seismic sequence with inclined
reflectors on the slope and parallel in the basin. 10: Eighth seismic sequence
with inclined reflectors on the slope and parallel in the basin.
The L6 seismic profile show a E-W to NNW-SSE trending
and crosses the Salerno Valley at depths comprised between
– 500 m and – 900 m (Fig. 1). The geologic interpretation, based
on the criteria of seismic stratigraphy, has allowed for the
identification of several seismic horizons, corresponding to
regional unconformities. In particular, an important
unconformity, localised between 1.7 and 1.8 sec of depth, has
been correlated with the top of the Meso-Cenozoic carbonatic
sequences, widely cropping out onshore in the structural high of
the Sorrento Peninsula. This unconformity is strongly
downthrown by normal faults and bounds also the base of the
Pleistocene sedimentary filling of the Salerno Valley. The
corresponding seismic horizon overlies with lateral continuity and
passes towards a thick sedimentary filling along the slope.
In particular, the Pleistocenic sedimentary filling of the
Salerno Valley is organised in eight seismic sequences (3-10 in
Fig. 1), separated by regional unconformities (B-I in Fig. 1), for a
total thickness of about 500 meters. The first seismic sequences
represent the initial stages of filling of the half-graben and are
characterized by wedging geometries, indicating a
synsedimentary tectonic activity in correspondence to the normal
fault which identified the half-graben, probably since the middle
Pleistocene. A normal trending of subsidence and filling of the
sedimentary basin is shown by the upper seismic sequences,
suggesting that the tectonic activity lasted up to the Late
713
Pleistocene in the offshore adjacent to the sedimentary basin,
probably in correspondence to NNW-SSE trending normal faults.
This evidence is perhaps confirmed by the tectonic setting of the
morpho-structural highs and of the related intra-slope basins in
the south-western offshore of the area.
REFERENCES
AIELLO G., BUDILLON F., DE ALTERIIS G., DI RAZZA O., DE
LAURO M., MARSELLA E., PELOSI N., PEPE F., SACCHI M. &
TONIELLI R. (1997a) – Seismic exploration of the
perityrrhenian basins in the Latium-Campania offshore.
Proceedings of the 8 th Annual workshop of the ILP Task
Force "Origin of Sedimentary Basins", Torre Normanna,
Palermo, June 1997.
AIELLO G., BUDILLON F., DE ALTERIIS G., FERRANTI L.,
MARSELLA E., PAPPONE G. & SACCHI M. (1997b) – Late
Neogene tectonics and basin evolution of Southern Italy
Tyrrhenian margin. Proceedings of the 8 th Annual workshop
of the ILP Task Force "Origin of Sedimentary Basins", Torre
Normanna, Palermo, June 1997.
BARTOLE R., SAVELLI D., TRAMONTANA M. & WEZEL F.C.
(1983) - Structural and sedimentary features in the
Tyrrhenian margin off Campania, Southern Italy. Mar. Geol.,
55, 163-180.
SESSIONE 23

SESSIONE 23
Key words: Carbonatic turbidites, central Italy, early
Pleistocene, periadriatic basin.
The evolution of the periadriatic area throughout Neogene
and Quaternary is correlated to the late phases of eastward
migration of the system Apennine chain - foredeep basin -
foreland.
The Pliocene - Pleistocene marine succession has been
deposited into a physiographical articulated satellite basin and is
characterized, from base to top, by neritic to littoral sand and
gravel deposits, by pelitic deposits with intermingled gravely
sand and sandy clay horizons (Mutignano Formation auct.), and
finally by neritic to littoral sand and gravel deposits and/or
continental deposits (CANTALAMESSA et alii, 1986; CENTAMORE
et alii, 1991, 2009; CENTAMORE & MICARELLI, 1997;
CENTAMORE &NISIO, 2003).
The underground Camerano town (Ancona, Central Italy)
allows to describe a composite sedimentological and
stratigraphical section into Early Pleistocene marine deposits
(LUCCIONI, 2007). Biostratigraphic analyses allow to refer these
deposits to Early Pleistocene (MNN 19c Nannofossil Zone: RIO
et alii, 1990), and to attribute them to the Qm-A3 phase
(CENTAMORE et alii, 1991; CENTAMORE &MICARELLI, 1997).
The superposition of three main cave levels (RECANATINI,
1997), with their pattern of tunnels, also provide a tridimensional
view of depositional geometries. Beds show alternatively a subhorizontal
attitude and an average 15° eastward inclination, both
recognizable as primary depositional features.
Deposits are mainly characterized by yellow-brown sand and
grey-green clay couplets, with a variable sand/clay ratio; in the
uppermost Grotta Ricotti and in the middle cave system (Grotta
Corraducci), at least two matrix-supported gravel horizons also
occur.
Sand-clay couplets show an erosion basal surface and a
normal gradation, from plane-parallel laminated sand to massive
clay. Sand is exclusively constituted of bioclasts (foraminifers
_________________________
Resedimentation evidences in the Early Pleistocene Camerano
section (Ancona, Marches, Central Italy)
ANGELA BALDANZA (*), ROBERTO BIZZARRI (**) & IRENE LUCCIONI (°)
(*) Dipartimento di Scienze della Terra, Università di Perugia, abaldanz@unipg.it
(**) Via A. Capitini, 8 – Marsciano (PG), roberto.bizzarri@libero.it
(°) Via C. Colombo, 18 – Camerano (AN), bvzm2002@yahoo.it
714
and shell fragments), with no rock fragments occurrence.
Plane-parallel lamination are marked by repeated grain size
variations, and deposits resemble to facies F7 (MUTTI, 1992) or
S1 (LOWE, 1982), and can be referred to “traction carpets”. Some
sand levels also show parallel cross-lamination and/or ripples in
the uppermost part, but each one gradually pass to massive clay.
They are described as carbonatic turbidites.
A statistic method, applied to the total foraminifers in the sand
and clay portions, allowed to discriminate the re-suspended
supply from the main water column productivity.
On the other hand, the matrix-supported gravels are
represented by heterometric clay fragments, with the same
characters of the aforementioned clay horizons, dispersed into a
bioclastic sandy matrix, similar to these of the sand-clay couplets.
A paleoenvironmental reconstruction can be proposed: the
clay component presumably represents the basin deposition of
distal river supply, coming from the western area and mixed to
the water column productivity. In this basin, storm- to seismicinduced
carbonatic turbidites periodically transported proximal
bioclastic material, out-coming from the shallow water area in the
rear of the M.te Conero "island".
The large clay fragments, matrix-supported gravels probably
derive from seismic remobilization of partially lithified deposits
along the basin’s flank, although their provenance is not clearly
recognizable. Nevertheless, the Camerano deposits suggest the
sedimentation in a tectonically active Early Pleistocene Basin.
REFERENCES
CANTALAMESSA G., CENTAMORE E., CHIOCCHINI U., COLALONGO
M.L., MICARELLI A., NANNI T., PASINI G., POTETTI M. &
RICCI LUCCHI F. (1986) - Il Plio-Pleistocene delle Marche. In:
E. Centamore & G. Deiana (Eds.), La Geologia delle Marche.
Studi Geol. Cam., Vol. Spec. 91, 61-68.
CENTAMORE E., CANTALAMESSA G., MICARELLI A., POTETTI M.,
BERTI D., BIGI S., MORELLI C. & RIDOLFI M. (1991) -
Stratigrafia ed analisi di facies dei depositi del Miocene e del
Pliocene inferiore dell'Avanfossa Marchigiano-Abruzzese e
delle zone limitrofe. Studi Geol. Cam., Vol. Spec. CROP11,
1991/2, 125-131.

CENTAMORE E., FARABOLLINI P. & ANGELINI S. (2009) - Guida
all’escursione:”Geologia e geomorfologia del settore
fermano nel bacino periadriatico marchigiano-abruzzese”.
Rend. online Soc. Geol. It., 8, 162-168.
CENTAMORE E. & MICARELLI A. (1997) – Stratigrafia. In:
L'ambiente fisico delle Marche, Geologia, Geomorfologia,
Idrogeologia. SELCA, Firenze, 1-66.
CENTAMORE E. & NISIO S. (2003) - Significative events in the
Periadriatic foredeeps evolution (Abruzzo-Italy). Studi Geol.
Cam. Vol. Spec. 2003, 39-48.
LOWE D.R. (1982) - Sediment gravity flows II. Depositional
models with special reference to the deposits of high-density
turbidity currents. J. Sediment.Petrol.,52(1), 279-297.
LUCCIONI I. (2007) - Geologia ipogea di Camerano – Storia
della città sotto la città. Collana: Quaderni di Storia
cameranese, Castelfidardo, 115 pp.
MUTTI E. (1992) - Turbidite sandstones. Agip, Milano, 275 pp.
RECANATINI A. (1997) – Le Grotte del Conero - Ricerche di
speleologia archeologica nel Parco del Conero. Collana: I
Voli del Conero, 4, UTJ, Jesi, 254 pp.
RIO D., RAFFI I. & VILLA G. (1990) - Pliocene-Pleistocene
calcareous nannofossil distribution patterns in the Western
Mediterranean. In: K. Kastens & J. Mascle (Eds.) - Proc.
ODP Sci. Results, 107, 513-533.
715
SESSIONE 23

SESSIONE 23
The Early Aptian Oceanic Anoxic Event 1a: excess volcanogenic
CO2 triggering ocean acidification, biocalcification crisis,
fertilization, accelerated weathering
CINZIA BOTTINI (*), ANTHONY COHEN (**), ELISABETTA ERBA (*) & HUGH JENKYNS (°)
Key words: Biocalcification, Early Aptian, Oceanic Anoxic Event
1a, ocean acidification, ocean fertilization, pCO2,
weathering.
The Early Aptian (∼?120 million years ago) Oceanic Anoxic
Event (OAE) 1a is best represented by the Selli Level, a
lithostratigrahic marker defined in the Umbria Marche basin.
Selli Level equivalents have been identified in several pelagichemipelagic
successions of the Tethyan, Atlantic and Pacific
Oceans. The main characteristic of the Selli Level is the
occurrence of organic C-rich black shales and radiolarian layers
interrupting carbonate-rich lithologies.
Multi- and inter-disciplinary studies of the OAE1a have
pointed out C, O, Os, Sr isotopic anomalies, a biocalcification
crisis in pelagic and neritic settings, enhanced fertility and
primary productivity, anoxia. Although global anoxia and
enhanced organic matter burial are the most striking and
intriguing paleoceanograhic phenomena, OAE1a can be studied
to decipher the sequence of CO2 pulses and weathering changes,
regardless of the C source. The cutoff of carbonates during
OAE1a can be considered the effect of volcanogenic CO2-related
ocean acidification. Available cyclochronology allows highresolution
dating of biotic and environmental fluctuations,
providing the precision necessary for understanding the role of
pCO2 and ocean acidification on nannoplankton biocalcification
as well as adaptations, evolutionary innovation and/or
extinctions.
There is a general consensus on the causes of this casehistory,
namely excess CO2 derived from the construction of the
Ontong Java Plateau (OJP). The integrated paleontologicalgeochemical
approach has pointed out a sequence of CO2 pulses,
and perhaps some clathrate melting triggering a climate change to
_________________________
(*) Dipartimento di Scienze della Terra, Università degli Studi di Milano,
cinzia.bottini@unimi.it; elisabetta.erba@unimi.it
(**) Department of Earth & Environmental Sciences, The Open University,
UK, a.s.cohen@open.ac.uk
(°) Department of Earth Sciences, Oxford University, UK,
hugh.jenkyns@earth.ox.ac.uk
Lavoro eseguito nell’ambito del progetto PRIN2007W9B2WE 001
716
supergreenhouse conditions and ocean acidification. Changes in
nannofossil assemblages allow the discrimination of surfacewater
acidification from bottom-water acidity, that clearly
postdates the early effects recorded by calcareous nannoplankton.
The first evidence of bottom-water acidification at 120.22 Ma,
consists of severe dissolution at the sediment/water interface,
presumably induced by the shallowing of the calcite lysocline and
the calcite compensation depth. The reconstructed CO2 pulses
suggest a stepwise accumulation of CO2 in the ocean inducing
progressive acidification.
A major acceleration in weathering has been identified based
on 187 Os/ 188 Os ratio in the lowermost part of OAE1a. Perhaps,
this weathering drawdown of CO2 corresponds to the relative
cooling interval and possibly alkalinity recovery within OAE1a.
After dissolution climax, matching maximum ocean acidification,
nannoplankton and carbonate recovery developed over ~160 kyr,
under persisting global dysoxia-anoxia. This recovery presumably
implies a stasis of the OJP activity and gradual buffering of ocean
acidification or a decrease in volcanogenic CO2 emissions and
consistently higher CO2 drawdown through Corg burial and/or
weathering.
Rising pCO2 and surface-ocean acidification during OAE1a
triggered false extinctions among calcareous nannoplankton,
because the nannoconid crisis is a global case of Lazarus effect
without extinctions. Conversely, a major origination episode
starts approximately 1 My before global anoxia and persists
through OAE1a and associated acidification. Increasing pCO2
solicited coccolith production of r-strategist taxa, which,
however, secreted dwarf and malformed coccoliths.
The response of calcareous nannoplankton to increasing
ocean acidification is complex and species-specific and we
provide data and timing for integrated surface- and deep-ocean
modeling. For the first time, the OAE1a case supplies evidence
for surface-water acidification followed by deep-sea dissolution
and CCD rise, as predicted by models for future acidification
crisis.

Key words: Depositional sequences, geomorphological analysis,
Quaternary, southern Apennines, tectono-sedimentary
evolution.
INTRODUCTION
The Plio-Pleistocene succession cropping out along the
Apennines foothills forms the filling of the Apenninic foredeep.
A synthetic stratigraphic framework for this succession is
available especially from the Emilia-Romagna and Marche
Apennines. RICCI LUCCHI et alii (1982) carried out the first
comprehensive stratigraphic study of this succession and
established the subdivision into two major depositional cycles,
referred to as “Cycle Qm” and “Cycle Qc” (Quaternary marine
and Quaternary continental deposits, respectively). Subsequently,
more detailed studies have been carried out by AMOROSI et alii
(1998) and CANTALAMESSA &DI CELMA (2004). At relatively
southern locations the Plio-Pleistocene succession has been
poorly investigated with the only exception of southern Abruzzi
and Fortore River area (CAPUANO et alii, 1996; AUCELLI et alii,
1997; CHIOCCHINI et alii, 2006). Recently, AMOROSI et alii
(2009) carried out a detailed facies characterization of the Plio-
Pleistocene succession and defined an overall stratigraphic
framework in the coastal area between Trigno and Fortore rivers.
The importance of the stratigraphic study of the Plio-
Pleistocene succession is that these deposits record eustatic sealevel
oscillations and neotectonic uplift/subsidence rates. The
uplift and the deformation of these successions led to alternating
erosional and sedimentary processes within the foreland basin.
Since the Pliocene evolution of this sector is well documented
in literature (CASNEDI et alii, 1981; CELLO et alii, 1989;
PATACCA et alii, 1992), a geological and stratigraphical study
integrated with geomorphologic analysis was carried out in the
coastal sector between Trigno and Fortore rivers to investigate
_________________________
Stratigraphy and tectono-sedimentary evolution of the periadriatic
basin between Trigno and Fortore rivers (Southern Apennines)
VITO BRACONE (*), PIETRO P.C. AUCELLI (**), CARMEN M. ROSSKOPF (*) & ALESSANDRO AMOROSI (°)
(*) Dipartimento S.T.A.T., Università degli studi del Molise,
vito.bracone@unimol.it, rosskopf@unimol.it
(**) Dipartimento D.I.S.A.M., Università degli stu di “Parthenope” di
Napoli, pietro.aucelli@uniparthenope.it
(°) Dipartimento di Scienze della Terra e Geologico-Ambientali, Università
di Bologna, alessandro.amorosi@unibo.it
717
the Quaternary tectono-sedimentary evolution of the southern
Apennines foreland basin.
RESULTS AND CONCLUSION
Following the stratigraphic framework defined by AMOROSI et
alii (2009) the litostratigraphic units, represented by Montesecco
Clays, Serracapriola Sands and Campomarino Conglomerates,
have been interpreted as depositional sequences (sensu MITCHUM
et alii, 1977) in a sequence stratigraphy context. The sequencestratigraphic
analysis allowed to identify five depositional
sequences: Qm, Qm1, Qc1, Qc2 and Qc3.
Qm is represented by a homogenous succession of either
laminated or bioturbated grey clay with intercalation of silts,
interpreted as offshore deposits (Montesecco Clays). The
microfaunal assemblages within Qm deposits suggest that
deposition took place between upper Piacenzian and Santernian
(AMOROSI et alii, 2009).
The stratigraphic boundary between sequences Qm and Qm1
is characterized by a regional angular unconformity of Emilian
age, which suggests that a stratigraphic hiatus separates the two
sequences (Fig. 1).
The Qm1 sequence (Sicilian age) is established by two units:
a lower one represented by sands and silts (offshore transition
deposits); an upper one represented by a wide spectrum of littoral
Fig. 1 – Angular unconformity between Qm and Qm1 sequences
SESSIONE 23

SESSIONE 23
deposits, forming a peculiar progradational beach sequence.
The “continental” sequences Qc1 and Qc2 (early Pleistocenemiddle
Pleistocene) and Qc3 (middle Pleistocene-Holocene) are
made up of alluvial deposits. Particularly, sequences Qc1 and
Qc2 display a fining-upward tendency.
The stratigraphic boundary between these “continental”
sequences and the underlying sequences is marked by a gentle
angular unconformity. On top of Qc2 a reddish paleosol, 2 m
thick, can be observed.
The stratigraphic framework displays strong similarities with
the one reported from the northern and the central sectors of the
Apennine (periadriatic) foredeep.
Through the integration of stratigraphic data with
geomorphological analysis, additional constraints have been
identified. Particularly, two order of hanging paleosurfaces were
identified and assigned I and II order, respectively. These
paleosurfaces took place at sequence boundary of depositional
sequences.
Four tectonic phases were identified. The first one (Late
Pliocene) controlled the deposition of sequence Qm. The second
one (Emilian age) produced an important uplift and tilting of
sequence Qm. The third one (late Lower Pleistocene-Middle
Pleistocene) was preceded by a phase of relative tectonic stability
during which deposition of sequences Qm1 and Qc1 occurred.
This tectonic phase caused a further tilting and uplift of this
sector and the formation of the oldest erosion paleosurfaces
preserved in the study area (I order, 370-250 m). After this phase,
deposition of sequence Qc2 with II order paleosurfaces occurred.
Finally, the fourth (and last) tectonic phase produced the final
uplift of the area, the formation of asymmetric valleys with
sedimentation of sequence Qc3.
The estimated uplifting rates, valid at least for the Middle
Pleistocene, are comprised between 0.1-0.25 mm/yr.
This study allowed to give new constraints for the Quaternary
evolution of this sector.
REFERENCES
AMOROSI, A.,BARBIERI, M.,CASTORINA, F.,COLALONGO, M.L.,
PASINI, G. & VAIANI, S. (1998) - Sedimentology,
micropaleontology, and Strontium-isotope dating of a Lower-
Middle Pleistocene marine succession (“Argille Azzurre”) in
the Romagna Apennines, Northern Italy. Boll. Soc. Geol. It.,
117, 789-806.
AMOROSI, A.,BRACONE, V.,DI DONATO, V.,ROSSKOPF, C.M. &
AUCELLI, P.P.C. (2009) - The Plio-Pleistocene succession
between Trigno and Fortore rivers (Molise and Apulia
Apennines): stratigraphy and facies characteristics. GeoActa,
8, 1-12.
AUCELLI, P.P.C., CINQUE, A. & ROBUSTELLI, G. (1997) -
Evoluzione quaternaria del tratto di Avanfossa Appenninica
718
compresa tra Larino (Campobasso) e Apricena (Foggia).
Dati preliminari. Il Quaternario, 10, 453-460.
CANTALAMESSA, G.&DI CELMA, C. (2004) - Sequence response
to syndepositional regional uplift: insights from highresolution
sequence stratigraphy of late Early Pleistocene
strata, Periadriatic Basin, central Italy. Sed. Geol., 164, 283-
309.
CAPUANO, N., PAPPAFICO, G. & AUGELLI, G. (1996) -
Ricostruzione dei sistemi deposizionali plio-pleistocenici al
margine settentrionale dell’Avanfossa pugliese. Mem. Soc.
Geol. It., 51, 273-292.
CASNEDI, R., CRESCENTI, U., D’AMATO, C., MOSTARDINI, F. &
ROSSI U. (1981) - Il Plio-Pleistocene nel sottosuolo molisano.
Geol. Rom., 20, 1-42.
CELLO, G., MARTINI, N., PALTRINIERI, W. & TORTORICI, L.
(1989) - Structural styles in the frontal zones of the southern
Apennines, Italy: an example from the Molise district.
Tectonics, 8, 753-768.
CHIOCCHINI, U., BARBIERI, M., MADONNA, S., DI STEFANO, A. &
POTETTI, M. (2006) - I depositi del Pleistocene tra Ortona e
la stazione ferroviaria di Casalbordino (provincia di Chieti).
Rend. Soc. Geol. It., 2, 3-14.
MITCHUM, R.M., VAIL, P.R. & THOMPSON, S. (1977) - The
depositional sequence as a basic unit for stratigraphic
analysis. In: C.E. Payton (Eds.) - Seismic Stratigraphy
Application to Hydrocarbon Exploration. AAPG Mem., 26,
53-62.
PATACCA, E., SCANDONE, P., BELLATALLA, L., PERILLI, N. &
SANTINI, U. (1992) - La zona di giunzione tra l’arco
appenninico settentrionale e l’arco appenninico meridionale
nell’Abruzzo e nel Molise. Stud. Geol. Cam., 1991/2, 417-
441.
RICCI LUCCHI, F.,COLALONGO, M.L., CREMONINI, G.,GASPERI,
G., IACCARINO, S.,PAPANI, G.,RAFFI, I.&RIO, D. (1982) -
Evoluzione sedimentaria e paleogeografica del margine
appenninico. In: G. Cremonini and F. Ricci Lucchi (Eds.) -
Guida alla geologia del margine appenninico-padano. Guide
Geologiche Regionali Soc. Geol. It., 17-46.

Low-enthalpy geothermal reservoirs in the buried thrust front of the
Apennines: exploration in the alluvial plain south of Parma
Key words: Geothermal reservoir, Miocene turbidites, Parma
alluvial plain, thrust tectonics.
INTRODUCTION
The growing green economy stimulates scientific research in
the field of renewable energy resources; among these is
geothermal energy, which is becoming more and more
competitive even at low-temperatures (> 40°C). On the mountain
slopes and in the southern alluvial plain of the Po River basin
there is no high-enthalpy geothermal source known at
economically convenient depths. Yet, thermal springs and wells
are numerous in the Emilia-Romagna Apennines and alluvial
plain. For instance, a geothermal reservoir at Ferrara, represented
by fractured Mesozoic limestones situated at 1,100-1,900 m
depth, delivers 120 l/s of water at 95-100°C temperature; at
Bagno di Romagna (Forlì-Cesena) thermal springs at 42-43°C
temperature have historically been used for balneotheraphy and
lately for heating too.
The screening of the Emilia-Romagna territory for potential
geothermal resources completed by the Regional Geological
Survey led to the recognition of several areas with positive
thermic anomalies. In general their geographic distribution
coincides with the location of the main tectonic structures. In the
subsoil of the Po River alluvial plain these structures are
represented by a system of faulted folds named Emilian Folds by
PIERI &GROPPI (1981). The Emilian Folds actually represent
thrust fronts whose crest may be encountered at a few tens of
meters depth below ground surface, as in the case of the alluvial
plain south of Parma which is the target of this pilot study.
STRATIGRAPHY AND THRUST TECTONICS
The southern margin of the Po River plain represents the
perisutural zone of the Apennines orogenic belt in which
_________________________
(*) Dipartimento di Scienze della Terra, Università di Parma,
nicola.calda@unipr.it
(**) Servizio Geologico Sismico e dei Suoli, Regione Emilia-Romagna,
FMolinari@Regione.Emilia-Romagna.it .
NICOLA CALDA (*) & FABIO MOLINARI (**)
719
Neogene and Quaternary sedimentation has been controlled by
thrust tectonics. The study area, in particular, is characterized by
a buried thrust front deforming Miocene-Pleistocene beds
(CALDA et alii, 2007). The Pliocene-Quaternary sedimentation,
modulated by eustatic sea-level fluctuations, has been interpreted
on the basis of regional unconformity surfaces (RER &ENI-AGIP,
1998) in alluvial sedimentary synthems (Qc2 and Qc1 of Late-
Middle Pleistocene age) and marine sedimentary synthems
(Costamezzana and Stirone of Early Pleistocene - Late Pliocene
age and Lugagnano and Vernasca of Middle - Lower Pliocene
age).
The geometry of the top of the marine deposits
(Costamezzana synthem), dated at about 800 ky BP, is presented
in the form of the Digital Surface Model of Fig. 1. The several
hundreds of depth values of this surface have been transformed
into elevations referred to sea level which have been spatially
correlated according to the kriging square-net method by means
of the ESRI software Spatial Analyst.
The prominent feature of the kriged map is the positive
structure, extending south and west of Parma on the alignment of
the towns of Monticelli Terme, Vigatto, Lemignano Madregolo,
Fontevivo and Fontanellato, representing a thrust generated
antiform with a modest synform on its southern limb and a steep
monocline dipping northeast. At Monticelli Terme the alluvial
deposits are directly superposed on the eroded Miocene substrate
and are only 10 m thick. Westwards the thickness of the alluvium,
modulated by the culminations and depressions of the positive
structure (Fig. 1), gradually increases and its erosive base overlies
the marine Costamezzana synthem.
GEOTHERMAL RESERVOIRS
The Emilian Folds have been extensively investigated as
potential oil and gas reservoirs with the production of a rich
wealth of data, in particular, seismic profiles, stratigraphic wells,
and numerous well-log data. Additional information, with precise
depth-temperature profiles, is provided by the so-called UNMIG
collection and the ENEL-CNR studies on geothermal resources.
The implementation of these data with the databases of the
University of Parma and the Regional Geological Survey allowed
the construction of key geologic cross-sections and their dressing
with the temperature changes at depth. The positive thermic
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SESSIONE 23
Fig.1 - Digital Surface Model of the top of the marine deposits in the subsurface of the Parma area. The ground surface is simulated by the river network in
blue. The vertically exaggerated graphics highlights the positive structure created by the buried thrust front running from Monticelli Terme to Fontanellato and
by the direction of the marine deposits dipping north-east.
anomalies detected in the buried thrust front south of Parma
encouraged this research, aimed at finding potential geothermal
reservoirs.
In the study area the reservoir has been recognized in the
turbidite Miocene deposits covered by the Pliocene-Quaternary
marine and alluvial deposits described above. These turbidites,
here considered the local substrate, are coarse-grained sandstones
saturated by saline waters. The heat flow from the Miocene
substrate to the overlying fresh-water saturated sediments varies
primarily as a function of the reservoir depth: from ten meters
(Monticelli Terme) to a few hundred (es. Lemignano) and several
hundred (es. Madregolo) meters below ground surface. In the
culminations of the positive structure the temperatures detected in
the Miocene reservoir vary from 40 to 50°C.
The temperatures measured in the overlying fresh-water
aquifer are highly variable. For instance, at Monticelli Terme the
alluvial Late Pleistocene aquifer has a temperature around 20°C,
whereas at Vigatto the aquifer hosted in the Early Pleistocene
marine sands (Costamezzana) has a temperature around 16°C.
REFERENCES
CALDA N., VALLONI R. & BEDULLI F. (2007) - Three-dimensional
representation of permeability barriers and aquifers recharge
in the Pleistocene deposits of the Parma alluvial plain. In R.
720
VALLONI (Ed.): Proceedings Italian National Workshop
"Developments in Aquifer Sedimentology and Ground Water
Flow Studies in Italy", Parma June 2004, S.EL.CA. Firenze,
Memorie Descrittive Carta Geologica d'Italia, Roma, 76, 97-
108.
PIERI M. & GROPPI G. (1981) - Subsurface geological structure of
the Po Plain, Italy. Pubblicazione C.N.R. n° 414, Progetto
Finalizzato Geodinamica, 13 pp.
RER & ENI-AGIP (1998) - Riserve idriche sotterranee della
Regione Emilia-Romagna. A cura di G. Di Dio. S.EL.CA.,
Firenze, 120 pp.

1
Jurassic paleogeography and Neogene faulting at Corno di Catria
(Marche, northern Apennines)
Key words: Jurassic, Neogene transpression, northern
Apennines, pelagic carbonate platforms, submarine
escarpments.
INTRODUCTION AND METHODS
The Mt. Catria – Gola del Corno area in Northern Apennines
is part of a prominent anticline, where a Jurassic pelagic system
of intrabasinal highs and basins is exposed (CHILOVI et alii.,
2002). While the late Hettangian-early Sinemurian fragmentation
of the Calcare Massiccio (CM) carbonate platform is
unanimously ascribed to rift tectonics, genuine Early Jurassic
faults have never been actually observed in the field across the
Umbria-Marche and Sabina regions. Paleoescarpments are on the
other hand common, based on onlaps and the occurrence of
silicified CM. They document the submarine erosion of fault
surfaces/zones, which became inactive in the post-rift (late
Sinemurian; SANTANTONIO &CARMINATI, 2010). Based on the
ages of onlapping basinal formations, we subdivided escarpments
into a lower (Corniola), middle (Rosso Ammonitico to Calcari
Diasprigni), and upper (Calcari a Saccocoma ed aptici and
Maiolica) tracts. The condensed pelagic deposits resting
conformably on the footwall-block CM, indicating the top of a
pelagic carbonate platform (PCP) or a downstepped part of it,
were separated from those forming scattered patches
unconformable on its flanks (“epi-escarpment deposits”). All
were dated through ammonite biostratigraphy wherever possible,
with epi-escarpment deposits providing a minimum age for any
given escarpment tract due to their paleotopography-sealing
significance. The next step was a kynematic interpretation of the
Neogene faults, to see in which fashion(s), and to which extent,
they modified the inferred original Jurassic submarine
topography.
_________________________
(*) Università di Roma “La Sapienza”, domenico.cannata@uniroma1.it;
massimo.santantonio@uniroma1.it
DOMENICO CANNATA (*) & MASSIMO SANTANTONIO (*)
721
JURASSIC PALEOGEOGRAPHY
PCP-top - The top of the “Corno di Catria PCP” is only
exposed at low topographic elevations (~700 m a.s.l.) in the two
small outcrops of Gola del Corno and Serra Piana (2.5 km to the
SSE). At Gola del Corno, a condensed early Pliensbachian to
early Tithonian pelagic succession, ~9 m thick, represents the
western edge of the PCP, bordered by a W-facing upper
escarpment, with the Maiolica sealing the base (drowning
unconformity) of the condensed succession.
Paleoescarpment - The paleoescarpment environment is
extensively represented in the area, occupying a N-S trending belt
from Corno di Catria to Pian dell’Ortica, Balza dell’Aquila and
Bosco Rotondo/Pluviometro. One major W-dipping (towards the
Mt. Catria Basin) escarpment is exposed, dissected by high-angle
faults (see below). Onlaps indicate a lower escarpment at Bosco
Rotondo/Pluviometro/Balza dell’Aquila, with the Corniola
onlapping the CM up to 1380 m a.s.l. This northern area also
documents a corner in the escarpment, so that a basin must have
existed not only to the W, but also to the N of the high.
Elsewhere, middle- and upper-escarpment settings dominate
(onlaps of Calcari e marne a Posidonia to Maiolica). In the
opposite direction, possible evidence for an upper escarpment
tract facing S exists in the Valdorbia area. Both the W- and the
N-facing escarpments bear scattered condensed epi-escarpment
deposits of Pliensbachian age.
“Marginal step” - An incomplete condensed succession,
unconformable to conformable on the CM and up to 8 m thick, is
found in the Balze degli Spicchi/Rifugio Boccatoio sector. It is
unconformably overlain by cherty basinal deposits (upper Calcari
a Posidonia to Calcari a Saccocoma ed aptici), locally through an
interposed breccia with clasts of CM and of condensed pelagites.
A few hundred metres to the east, the same basinal units onlap the
CM directly. These relationships suggest the existence of a
narrow (

SESSIONE 23
escarpment forming two corners, we must also conclude – based
on onlaps and polarities of section thickening - that one laterally
continuous basin must have existed, with the Catria Basin
merging southwards with the Valdorbia Basin. About 4 km to the
NW, the Catria Basin strata terminated against the Mt Acuto
carbonate cusp (SANTANTONIO &CARMINATI, 2010), while ~4
km SSE of Valdorbia, the basinal strata abutted the N-facing
escarpment of the Mt. Cucco PCP (D’EMIDIO,
2006).
Fig. 1: Geological map of the Mt. Catria – Gola del Corno area.
NEOGENE FAULTING
With Neogene faulting, paleoescarpments are generally not
re-utilized as footwall ramps. Frontal ramps generally cut through
the highs, being lower-angle surfaces than the escarpments.
Lateral/oblique ramps, when striking subparallel to escarpments,
cut them at a higher angle, or cut across PCP tops. The PCP-basin
break in frontal areas commonly displays steeply dipping to
overturned basinal strata, due to thrust propagation in the CM.
Our area is dominated by high-angle transpressive dextral faults
striking 25° (Corno di Catria Fault), to ~N-S (Fonte dell’Insollio-
722
Pluviometro Fault and Balza dell’Aquila Fault), to 345° (Balza
degli Spicchi Fault= segment of the Bocca della Porta-Valle delle
Prigioni Fault in CHILOVI et alii, 2002), E to W. A frontal-zone is
seen at Rocca Baiarda-Balze della Porta, where a thrust strikes
310°. The Corno di Catria Fault cuts the PCP subparallel to its
western edge, so the upper escarpment overrides the PCP-top.
The Fonte dell’Insollio-Pluviometro Fault and the Balza
dell’Aquila Fault cause uplift and multiple offsets of the same
lower escarpment and basin-margin succession, thus mimicking –
misleadingly - a very small-scale topography of highs and basins.
The lateral component of these faults displaces the N-facing
escarpment tract seen in the corner-zone mentioned above, with a
cumulative dextral offset of ~1.7 km, so that the CM constituting
the W-facing escarpment is locally thrust on the pinch-out zone
pertaining to the N-facing escarpment (e.g. Le Scalette). The
Balza degli Spicchi fault has the middle-upper escarpment at the
hangingwall, which here includes the Bajocian “marginal step”.
In our interpretation, the CM across the Serra Piana/Gola del
Corno to Balza dell’Aquila and Pluviometro belonged to one
Jurassic footwall block. The Corno di Catria Fault does not
correspond to any Jurassic escarpment facing E; rather, it is an
uplifted tract of an escarpment dipping W. The basin at the
footwall (Maiolica to Scaglia; Jurassic is seen S of the
Castellaccio area) was conceivably the one which separated the
Corno di Catria PCP from the Mt. Roma-Val Canale high. Based
on new paleotopographic constraints, and on correlation between
footwall and hangingwall (Neogene faults) paleoenvironments,
vertical offsets produced by dextral transpression can be
estimated to amount to 700-900 m, while cumulative lateral
displacement produced by the Corno di Catria and Balza degli
Spicchi Faults, partly also accommodated by the locally
interposed N-S trending faults, amounts to ~5 km.
REFERENCES (STILE: REFERENCES)
CHILOVI C., DE FEYTER A. J., MINELLI G&BARCHI M. R. (2002)
- Neogene strike - slip reactivation of Jurassic normal faults
in the M. Nerone - M. Catria Anticline (Umbro - Marchean
Apennines, Italy) Boll. Soc. Geol. It. Vol. spec. 1,199–207.
D’EMIDIO M. (2006) - Assetto Geologico e paleogeografia del
settore compreso tra M. Cucco e Corno di Catria. Tesi di
Laurea Università di Roma “La Sapienza”, 81 pp.
SANTANTONIO M. & CARMINATI E. (2010) – Jurassic rifting
evolution of the Apennines and Southern Alps (Italy):
Parallels and differences. GSA Bulletin doi:
10.1130/B30104.1

Key words: Basin Evolution, clay mineral assemblages, fluid
inclusions,vitrinite reflectance, western Pyrenees.
INTRODUCTION
Late-Variscan (Late Carboniferous-Early Triassic) evolution
in the Axial Zone of the Pyrenees is characterised by continental
basin formation. These basins are presently preserved in the
hanging wall of the main thrusts responsible for the uplift of the
Axial Zone. Sedimentary sequences filling the Late Variscan
basins developed under a post-collisional, strike-slip regime and
evolved towards an extensional setting during the Permian with
fluvial and lacustrine facies accompanied by extensive pyroclastic
deposition. The continental successions are preserved in basins
organised along the E-W direction, parallel to the present-day
outcrop of the Axial Zone of the Pyrenees, with limited extension
and lengthening in the same direction. Although these units are
traditionally considered as purely sedimentary, metamorphic
parageneses (greenschist facies) have been locally recognized in
the Aragón-Bearn basin. This metamorphism has been interpreted
as related to later intrusion of andesitic bodies, although its
causes are still matter of debate. In order to constrain the origin
and features of this metamorphism, we applied an integrated
study of fluid inclusion micro-thermometry on veins and cements,
X-ray diffraction, and organic matter optical analyses of the
Aragón-Bearn basin sediments.
ARAGÓN-BÉARN BASIN
The Aragón-Béarn Basin, about 1200-1600 m thick, is
characterized by Paleozoic alluvial and lacustrine sediments
overlain by Triassic continental deposits.
_________________________
Late Paleozoic basin evolution of the Aragón-Béarn Basin
(Western Pyrenees): insight from thermal indicators
(*) Dipartimento di Scienze della Terra, Università di Camerino,
valentina.cantarelli@unicam.it, chiara.invernizzi@unicam.it
(**) Dipartimento di Scienze Geologiche, Università Roma TRE,
aldega@uniroma3.it, corrado@uniroma3.it
(°) Departamento de Ciencias de la Tierra, Universidad de Zaragoza,
acasas@unizar.es
VALENTINA CANTARELLI (*), LUCA ALDEGA (**), SVEVA CORRADO (**),
CHIARA INVERNIZZI (*) & ANTONIO CASAS-SAINZ (°)
723
Between the Variscan basement (mainly consisting of
Devonian limestones and Carboniferous turbiditic Culm facies)
and the Alpine sedimentary cover (Early Triassic continental
deposits), the Stephanian-Autunian record is a fining-upward
lacustrine, 1000-1500 m thick sedimentary succession constituted
by dolomitic limestones, conglomerates, sandstones and
siltstones.
It is organized in four depositional units: Grey Unit
(Stephanian B), Intermediate Unit (Stephanian B-Autunian),
Lower Red Unit (Autunian) and Upper Red Unit (late Permian).
The entire succession is limited by first order unconformities.
RESULTS
A suite of 20 samples has been collected from the
Intermediate Unit, Lower Red Unit and Upper Red Unit. Fluid
inclusion micro-thermometry was performed on post-sedimentary
veins filled by calcite and occasionally by quartz and on syndiagenetic
cements in order to define the evolution of fluid
composition and P-T condition during deformation.
We have sampled various generation of veins: (i) veins
parallel to bedding; (ii) veins parallel to Alpine foliation; (iii)
veins cutting through bedding or foliation.
First results show that fluid inclusions are mainly
geometrically related to calcite crystal growth within the veins
and that calcite crystals are generally twinned. Homogenization
temperatures (Th) are in the range of 115-130°C both in (i) and
(ii) veins. Histograms relative to Th distribution reveal that some
re-equilibration occurred in few samples which are particularly
deformed (thick and patchy twins and/or curved twins).
Nevertheless, Th data from syn-diagenetic cement show higher
values (150-180°C).
Organic matter thermal maturity dataset consists of vitrinite
reflectance and Rock-Eval pyrolisis values published by VALERO
GARCÉS (1993) and new vitrinite reflectance data. Analyses were
performed on the basal member of the Intermediate Unit close to
the andesitic bodies with Ro% values comprised between 4.72
and 4.16% and Tmax values from pyrolisis exceeding 500°C. Both
sets of data indicate the overmature stage of hydrocarbon
generation corresponding to meta-anthracite coal rank.
The only Ro% value available above the paraconformity in the
Upper Red Unit (2.9%) indicates a sensibly lower thermal
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SESSIONE 23
maturity (corresponding to the anthracite coal rank) in the
overmature stage of hydrocarbon generation.
Our data, deriving from the Intermediate Unit and sampled far
from the andesitic dykes, show histograms with a gaussian
distribution which identify an indigenous population of vitrinitehuminite
macerals with Ro% of 2.49.
XRD analyses of the < 2 μm grain-size fraction from the
Intermediate Unit show an illite-rich composition with
subordinate amounts of chlorite and minor amounts of
paragonite.
In a few samples, a pyrophyllite + rectorite paragenesis have
been observed. Kübler index data are in the range of 0.32-0.46
°Δ2θ indicating diagenetic/anchizone conditions in agreement
with clay minerals assemblages.
Oriented mounts from the Lower Red Unit mostly contain
illite, chlorite, R3 mixed layer I-S with an illite content of 95%
and small amounts of paragonite. Kübler index data reveal a full
width at half maximum height ranging from 0.32 to 0.52 °Δ2θ
indicating deep diagenetic/anchizone conditions.
Traces of smectite have been recognized in a few samples by
the broad and low intensity reflection at 5.2 °Δ2θ (17 Å) in the
ethylene-glycol solvated patterns suggesting retrograde alteration.
The Upper Red Unit is characterized by paragonite (wt. 4-
30%), chlorite (12-18%), illite (40-67%) and mixed layer R3 I-S
(5-44%). I-S displays low expandable structures with an illite
content ranging from 85 to 92%. Kübler index data range from
0.57 to 0.94 °Δ2θ suggesting diagenetic conditions.
CONCLUSION
The integration of organic and inorganic thermal parameters
shed new light into the thermal evolution of the Late Paleozoic
basins in the Western Pyrenees.
A prograde trend of increasing thermal maturity as function of
depth has been identified by Kübler index data and clay mineral
assemblages. Calculated maximum temperature for the bottom of
the Aragón-Bearn basin succession is about 240 °C.
Vitrinite reflectance confirms the temperature derived from
clay mineral thermal parameters and allows defining basin sectors
that have been affected by dykes intrusions.
Data from fluid inclusion micro-thermometry reveal
comparable results either for different vein types (i and ii) or
various sampled units. This suggests that fluid inclusion
developed in the late stage of thermal evolution of the basin
(Alpine orogeny?) and they have been partially re-equilibrated
during the late stage of deformation.
Homogenization temperatures from syn-sedimentary cement
reveal higher temperature than those derived from veins and
probably they reflect the burial condition within the basin.
724
REFERENCES
VALERO GARCÉS B.L. (1993) - Lacustrine deposition and related
volcanism in a transtensional tectonic setting: Upper
Stephanian–Lower Autunian in the Aragón–Béarn Basin,
western Pyrenees (Spain–France), Sediment. Geol., 83, 133-
160.

Provenance, depositional and palaeogeographic insights from the
coarse-disorganised deposits of the Macigno turbidite systems (late
Oligocene-early Miocene, Northern Apennines)
Key words: Debris flows, Late Oligocene, Macigno, turbidite
systems.
INTRODUCTION
Coarse-disorganised and chaotic deposits (clasts > 5 cm) are
generally produced by mass-flows like debris flows. If included
in deep-sea turbidite systems, they reveal a great importance, as
they represent particular flow events. They usually occur inside
very proximal turbidite systems, whereas are unusual for distal
and high-efficiency ones. The significance and importance of
coarse-disorganised and chaotic deposits within turbidite systems
have been for long undervalued, also due to their sporadic
occurrence. Their sedimentological, stratigraphical and
compositional features can provide a lot of remarkable
information about: triggering mechanisms (or events), transport
and depositional processes, flow-transformation processes,
palaeogeography, provenance, and composition of the
sourcing/feeding systems. They reveal as well features about: the
shallower portions of the basin, the slope and deep-sea basinal
physiography, and the efficiency of the turbidite system. The
Northern Apennine range with its late Oligocene-early Miocene
diachronous foredeep turbidite systems represents good study
area to observe such deposits and to investigate their
peculiarities. Moreover, the role played by these deposits in the
palaeogeographic/geodynamic reconstruction of the Northern
Apennines is relevant. Two turbidite systems have been
considered in this research: the so-called “Macigno costiero” and
“Macigno del Chianti” (both outcropping in Southern Tuscany
area), thick respectively 600 and 1500-2000 metres and
concerning respectively to a low-efficiency and to a medium- to
high-efficiency system. They are represented by several facies
associations, and by the occurrence of rare coarse-disorganised
levels. These turbidite successions include in fact thick
_________________________
(*) Dipartimento di Scienze della Terra, Università di Siena,
cornamusini@unisi.it
(**) Centro di Geotecnologie, Università di Siena
GIANLUCA CORNAMUSINI (*) (**) & ALESSANDRO IELPI (*)
725
olistostromes (submarine slides coming from the orogenic units
stack) and coarse-disorganised deposits, these latter subject of
this work. The restricted areas where such deposits crop out are
(from the west): Baratti-Piombino, Calafuria and Punta Ala
along the Tyrrhenian coast (for the “Macigno costiero”), Chianni,
Rocca d’Orcia and Chianti Mts in the tuscan inland (for the
“Macigno del Chianti”); besides, similar deposits have been also
signalled in the easternmost Liguria, to the north of the study
area. Some of these have been studied by sedimentological or
compositional point of views by a few researchers (i.e. PATACCA,
1973; FERRINI &PANDELI, 1983; CORNAMUSINI et alii, 2002).
DATA AND DISCUSSION
All these coarse disorganised-chaotic deposits show similar
textures, with minor differences in terms of thickness and lateral
extent, clast/matrix ratio, mud amount of the matrix, clast shape,
grain-size and sedimentary structures. The texture is commonly
disorganised/chaotic, poorly sorted, with intrabasinal or
extrabasinal clasts (pebbles and cobbles) dispersed inside a
muddy matrix, with scarce to absent organisation (just raw clast
orientation). Clasts are well-rounded with spherical or bladed
shapes. Mass flow deposits in the Macigno l.s. turbidite systems
can be classified in three types, based on their sedimentological
and compositional features, hereby described. Type 1: mainly
intrabasinal coarse disorganised-chaotic deposits, subdivided into
three portions (from the bottom): basal lenticular graded pebbly
sandstones with extrabasinal clasts (facies C); pebbly mudstone
with muddy-silty matrix containing dispersed intrabasinal
carbonate clasts, fossils and floating muddy-silty slides (facies
B'); deposits similar to facies B', but characterized by muddy-silty
slide/slump floating blocks (facies A'). Type 2: mainly
extrabasinal coarse disorganised-chaotic deposits. They are
characterised by a muddy-sandy matrix with dispersed wellrounded
extrabasinal clasts (facies B'''). Sometimes, vertical
facies changes can occur, with a matrix-poor conglomerate
(pebbles) (facies B'') at the bottom and sub-angular sandstone
cobbles/boulders (intrabasinal) and floating slumped silty-muddy
blocks (facies A) at the top. Type 3: chaotic huge bodies of
allochthonous slides (olistostromes and olistoliths), much
diffused in the Macigno systems, not considered here. The facies
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Fig. 1 – Depositional-geodynamic model for the Northern Apennines thrust-foredeep system during Late Oligocene.
of both Type 1-2 coarse-disorganised deposits correspond to very
immature deposits, laid down in proximal sites, not far from the
flow source. Long transport pathways can be excluded for them.
They can be interpreted as the product of submarine cohesive
debris flows interacting with deep-sea turbidite fans. The
composition of the clasts is relative to a crystalline basement and
subordinately to volcanic and sedimentary rocks. Such deposits
show the same composition of the adjacent turbidite sandstones,
and they reveal then a similar provenance. We can suppose that
these debris flows are likely a reworked product of proximal
sedimentary systems (e.g. fan-deltas or beach), fed by
extrabasinal clastic drainages. Besides, joining sedimentological
and compositional features of both coarse-disorganised deposits
and interlayered sandstones allow to reconstruct the source vs.
basin infilling history as well as to better understand the regionalgeodynamic
framework. As a result, the mass flows source area is
inferred in the inner hinterland of the foredeep, and more in detail
in the Corsica-Sardinia Massif, part of the European basement
(Fig. 1). In such a scenario, the debris flow feeding mechanism
was transversal to the inner foredeep and therefore, flows likely
originated from narrow shallower thrust-top basins (close to the
palaeoeuropean margin). Moreover, such deposits should also
have recorded the main thrust propagation events. These remarks
726
may in the end allow to reconsider the whole late Oligocene –
early Miocene foredeep sourcing system of the Northern
Apennines. In fact, while few Authors already reviewed the
innermost and oldest “Macigno Costiero” system, some unclear
points of the outer “Macigno del Chianti” system are still to be
discussed.
REFERENCES
CORNAMUSINI G., ELTER F.M. & SANDRELLI F. (2002) - The
Corsica-Sardinia Massif as source area for the early
northern Apennines foredeep system: evidence from debris
flows in the “Macigno costiero” (Late Oligocene, Italy). Int.
J. Earth Sci., 91, 280-290.
FERRINI G. & PANDELI E. (1983) - Le associazioni di facies
torbiditiche nel Macigno dei Monti del Chianti. Boll. Soc.
Geol. It., 102, 223-240.
PATACCA E. (1973) – Microfacies dei conglomerati della
“Scaglia” e del “Macigno” di alcune serie toscane. Mem.
Soc. Geol. It., 12(2), 187-225.

Basin analysis and tectonostratigraphy: an integrated approach to
decipher the Ligurian Alps geodynamics
Key words: Briançonnais, Geodynamics, Ligurian Alps,
Prepiedmont, rifting.
INTRODUCTION
The Ligurian Alps are a particularly complex sector of the
Alpine chain, in which the emplacement of thrust folds driven by
orogenesis completely masks the original scenario in which the
respective volcanic and sedimentary successions were deposited.
Moreover, the effects of Variscan and Alpine orogenesis overlaps
where some fault-systems have been re-activated several times in
different tectonic contexts, exasperating the geological
framework and its interpretation in terms of geodynamic
response. For these reasons, since the Sixties, the approach has
been to collect and rationalize field data in a tectonostratigraphic
frame. Thus the fundamental features of the main stratigraphicstructural
units were at first defined, and then they were attributed
to three major palaeogeographic domains (e.g. VANOSSI, 1980,
1986 cum ref.): the External Ligurian Briançonnais, Internal
Ligurian Briançonnais and Prepiedmont (Fig. 1). Thanks to the
attendance of our research-group to field surveying-oriented
projects (CARG and EU fund INTERREG IV), in the last years a
major detail has been achieved in the Ligurian Alps successions
(BONINI et alii, 2009; DALLAGIOVANNA et alii, 2009; DECARLIS
&LUALDI, 2009; SENO et alii, 2005). A basin analysis at the
Alpine Tethys-scale allowed us to correlate some Ligurian
lithostratigraphic units (e.g. DECARLIS &LUALDI, 2008) with the
coeval ones in different Alpine domains (i.e. Western Alps and
Southern Alps), contributing to define their role as “geodynamic
marker” and thus leading to a better comprehension of the
Ligurian geodynamic itself.
_________________________
ALESSANDRO DECARLIS (*), GIORGIO DALLAGIOVANNA (*), ALBERTO LUALDI (*),
MATTEO MAINO (*) & SILVIO SENO (*)
(*) Dipartimento di Scienze della Terra, Università di Pavia,
decarlis@dst.unipv.it
The research was supported by PRIN 2008 grants (Coord. Calamita-Seno-
Tavarnelli).
727
THE GEODYNAMIC-ORIENTED PROJECT
The aim of this project is to rationalize the field data through
harmonizing stratigraphy with the synsedimentary tectonics that
predates the orogen formation. The final goal is to provide a
dynamic reconstruction through the different phases that finally
lead to the ocean spreading in the Ligurian area. From Early
Permian to Upper Jurassic, a complete stratigraphic frame is
provided by different sectors of the Ligurian Alps. The
relationships among sedimentation rate, stratigraphic gaps,
tectonics and the palaeogeographic position of selected
successions, give us the opportunity to study an almost complete
section across the continental margin. Correlation with the
adjacent sectors of the Alps may be crucial to fill data lacks and
to bypass uncertainty induced by tectonic omissions. On the relics
of Variscan orogenesis and during the whole deposition of its
molasse (Late Permian-Early Triassic) a generalized tensional
tectonics gradually increased, first providing the required
accommodation for the thick carbonate platforms of Middle and
Upper Triassic. Subsequently, this still undeciphered geodynamic
phase that preceded the Jurassic collapse of the margin, initially
acted as a sharp deepening of the depositional environment (from
peritidal deposits to open-shelf cherty limestones) and then as a
fault-controlled slope, with large amount of tectonic breccias
Fig. 1 – Location of the study area and tectonic sketch of the Ligurian Alps.
SESSIONE 23

SESSIONE 23
Fig. 2 – Base of the Monte Galero Breccia Formation (more than 400 m.thick),
generated by the tectonic evolution of the European margin during the
paroxistic phase of rifting (Late Lias-Early Dogger).
(DALLAGIOVANNA & LUALDI, 1986; Fig. 2). Details regarding the
anatomy of the Jurassic rifting and its relationships with the
previous geodynamic trend have been analyzed. First data drive
us to take into a great account inheredited Variscan structures,
which later acted as crustal weakness during Tethyan rifting s.s
and which are probably responsible for the location of the final
break away of the Ligurian Tethys.
REFERENCES
BONINI L., DALLAGIOVANNA G. & SENO S. (2009) - The role of
pre-existing faults in the structural evolution of thrust
systems: Insights from the Ligurian Alps (Italy).
Tectonophys., 480 (1), 73-87.
DALLAGIOVANNA G. & LUALDI A (1986) - Le Brecce di Monte
Galero: nuovi dati e interpretazioni. Mem. Soc. Geol. It., 28,
409-418.
DALLAGIOVANNA G., GAGGERO L., MAINO M., SENO S. &
TIEPOLO M. (2009) - U-Pb zircon ages for post-Variscan
728
volcanism in the Ligurian Alps(Northern Italy). Journ. Geol.
Soc. London, 166, 101-114.
DECARLIS A. & LUALDI L. (2008) - Late Triassic-Early Jurassic
paleokarst from the Ligurian Alps and its geological
significance (Siderolitico Auct., Ligurian Briançonnais
domain). Swiss J. Geosc., 101, 579-593.
DECARLIS A. & LUALDI L. (2009) - A sequence stratigraphic
approach to a Middle Triassic shelf-slope complex of the
Ligurian Alps (Ligurian Briançonnais, Monte Carmo-Rialto
unit, Italy). Facies, 55, 267-290.
SENO S., DALLAGIOVANNA G. & VANOSSI M. (2005) - Pre-
Piedmont and Piedmont-Ligurian nappes in the central sector
of the Ligurian Alps: a possible pathway for their
superposition on to the inner Briançonnais units. Boll. Soc.
Geol. It., 124, 455-464.
VANOSSI M. (1980) - Les unités géologiques des Alpes Maritimes
entre l’Ellero et la Mer Ligure: un aperçu schématique.
Mem. Sc. Geol. Univ. Padova, 34, 101-142.
VANOSSI M. (a cura di) (1986) - Geologia delle Alpi Liguri. Mem.
Soc. Geol. It., 28, 598 pp.

A megaclastic basin-fill Jurassic succession at Montagna dei Fiori
(Abruzzo, Italy)
Key words: Apennines, Jurassic, olistoliths
INTRODUCTION
The Montagna dei Fiori structure is a fault-related anticline in
the south-eastern part of Northern Apennines. It displays an
eastern overturned forelimb, cut by the antiformal-shaped
Salinello thrust (DI FRANCESCO et alii, 2010), and a western
backlimb cut by a Miocene Normal fault. This structure resulted
from the interaction between a complex Jurassic submarine
topography, Miocene extension, and thrusting and folding due to
building of the Apenninic chain in the Neogene (MATTEI, 1987;
CALAMITA et alii, 1998; DI FRANCESCO et alii, 2010, and
references therein).
The stratigraphic succession at Montagna dei Fiori is the
classic Umbria-Marche succession, but it also comprises two
local formations: the “Dolomie di Castel Manfrino Fm.” and the
Fig. 1 - Simplified geological map of the Montagna dei Fiori.
_______________________
(*) Dipartimento di Scienze della Terra, Università “La Sapienza”, Roma
simone.fabbi@uniroma1.it; massimo.santantonio@uniroma1.it
SIMONE FABBI (*) & MASSIMO SANTANTONIO (*)
729
“Salinello Fm.” (GIANNINI et alii, 1970 and references therein).
The former unit is essentially a dolomitized Calcare Massiccio
(henceforth CM), Hettangian-Sinemurian p.p. in age. The
Corniola, Rosso Ammonitico and Calcari a Posidonia Fms. bear
abundant interbedded gravity flow deposits, sourced by a
carbonate platform. Next comes the Salinello Fm. (Bathonian
p.p.-Oxfordian; GIANNINI et alii. 1970), an arenite/rudite unit that
is lateral equivalent of the Calcari diasprigni Fm. The succession
continues with the Calcari a Saccocoma and aptici and the
Maiolica Fms., followed by the Cretaceous to Miocene Marne a
Fucoidi, Scaglia, and Marne con Cerrogna Fms. In previous
studies, the area had been interpreted as a small-scale system of
Jurassic pelagic basins with fault-bounded highs made of CM,
capped by a condensed succession (MATTEI 1987; CALAMITA et
alii, 1998). For this study, we placed emphasis on the four main
outcrops of CM, described below, and on their bedding attitude
and boundaries with the surrounding basinal units (Fig. 1).
DATA AND DISCUSSION
Corano quarry. This is a small (~ 0.35 km 2 ) outcrop of CM,
which is unconformably capped by the much younger Salinello
Fm., without any interposed condensed succession. Despite its
previous interpretation as a fault-bounded structural high
(MATTEI, 1987), this is in our interpretation an olistolith, for the
following reasons: (i) The CM dips 45° toward the W and is
surrounded by E-dipping basinal units (Corniola to Salinello),
markedly clastic (also with thick lensoid breccias; MATTEI,
1987); should one elect to restore the original attitude of the CM
to the horizontal, a cumbersome geometry with downlapping
basinal units would be produced; (ii) it is possible to walk all
around the outcrop, where the onlap line of the top Corniola
encircles an object that is at least one order of magnitude smaller
than even the smallest structural high in the region (e.g. Mt.
Acuto, Marche) at that paleotopographic level (in the lower
escarpment hypothesis); (iii) the exposed surface of CM, cut by
neptunian dykes, is silicified. Silicification of exhumed surfaces
of CM is known to be a marker of the unconformity with
onlapping chert-rich basinal units (GALLUZZO &SANTANTONIO,
2002), so this is an evidence for a stratigraphic contact. Only
scattered unconformable condensed pelagites (condensed
Corniola) are seen, and any genuine condensed succession at the
top of the CM is missing. These pelagites can be interpreted as
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SESSIONE 23
former epi-escarpment deposits (GALLUZZO & SANTANTONIO,
2002); (iv) nowhere across the region is an intrabasinal high, with
an inferred flat top, devoid of an even thin condensed succession,
being instead buried by rudites through a hiatus; also the
clastic/megaclastic nature of the surrounding basin is itself an
element supporting the interpretation of Corano as an olistolith.
Fosso Grande. This small (< 0.3 km 2 ) outcrop of CM was
previously interpreted as a structural-high as well. It is impossible
to detect bedding in the CM here, but the condensed Corniola has
an irregular distribution, locally draping the underside of an
overhang of CM. This can either be explained as the result of
exhumation of a neptunian dyke through removal of one of its
walls, or as due to rotation of the CM. The same considerations
put forward for Corano hold true here, regarding size, lack of a
condensed succession, onlap geometries, and clastic nature of the
encasing succession. In our view this is also an olistolith.
Valle del Salinello. In the Salinello Valley, the CM is at the
hangingwall of a thrust with the Scaglia Fm. This CM has been
interpreted as the footwall of a Liassic extensional fault (MATTEI
1987; CALAMITA et alii, 1998). However, we note the following:
(i) Silicification of exhumed surfaces of CM is widespread in the
area. This evidences that contacts with the (Jurassic) basinal units
are everywhere stratigraphic, and not Jurassic shear zones; (ii)
The subhorizontal topographic top of the CM, where a condensed
succession had been inferred by previous authors, is not its
stratigraphic top: the CM in fact dips 42°-50° toward NE, so this
is a spectacular angular unconformity. The stratigraphic top of the
CM lies at the eastern boundary of the outcrop, where the CM,
passing to the Calcare Massiccio B (drowning succession;
MARINO &SANTANTONIO, 2010), is conformably capped by a
very thin condensed succession, ending in the lower
Pliensbachian, and unconformably overlain by the Salinello Fm.;
(iii) The resulting picture is that of a rotated CM block, onlapped
to the W and S by laterally continuous Corniola (with olistoliths
of CM) to Salinello succession, with the latter unit draping its
topographic top, much like at Corano; in doing so, the ~80 m
thick Salinello Fm. seals a ~0.5 km thick section of CM; (iv) The
geometric tops of the Salinello and Corano CM lie not only at the
same topographic elevation, but also at the same stratigraphic
level, being both capped by the Salinello Fm. Based on the
above, interpreting this CM as indicating an olistolith is the more
conservative working hypothesis, documenting collapse of the
edge and margin of a pelagic carbonate platform in the early
Pliensbachian, soon after inception of the condensed sequence. In
support, we offer these additional considerations:
a) Should we restore the CM to the horizontal, and treat the
main subhorizontal unconformity as a paleoescarpment contact,
how could we justify an ~80 m unit (Salinello) sealing alone 0.5
km of CM stratigraphy? If we alternatively treated this as a
strongly rotated Liassic fault block, representing the natural
source of the other olistoliths described above, how can a fallen
block (e.g. Corano) lie at the same paleotopographic level as the
730
parent platform?
Castelmanfrino. This is the smallest CM outcrop, thoroughly
dolomitized. This has previously been interpreted as hangingwallblock
CM, conformably overlain by the Corniola. However, the
CM is seen as being not only overlain, but also surrounded by
dolomitized Corniola, without any evidence of faults, so this
appears as a block encased in the lower part of the basinal
succession. The actual relationships between the CM and the
Corniola Fm. were probably oversighted because both the
dolomitized Corniola and the dolomitized CM had been included
in one formation, the Dolomie di Castelmanfrino Fm.
In conclusion, we interpret the four main outcrops of CM as
olistoliths produced by pulses of retreat of a pelagic carbonate
platform margin, and rooted in the lower to middle Corniola.
Collapse of the Salinello block had to occur following platform
drowning and initial deposition of a condensed succession. This
interpretation implies that all the Jurassic rocks seen in the area
belong to a basin fill succession. The basin received abundant
input from a neighbouring productive platform, so the submarine
block-dominated topography was levelled around the Oxfordian.
REFERENCES
CALAMITA F., PIZZI A., RIDOLFI M., RUSCIADELLI G. & SCISCIANI
V. (1998) – Il buttressing delle faglie sinsedimentarie prethrusting
sulla strutturazione neogenica della catena
appenninica: L’esempio della Montagna dei Fiori
(Appennino centrale esterno). Boll. Soc. Geol. It., 117, 725-
745.
DI FRANCESCO L., FABBI S., SANTANTONIO M., BIGI S. & POBLET
J. (2010) – Contribution of different kinematic models and a
complex Jurassic stratigraphy in the construction of a
forward model for the Montagna dei Fiori fault-related fold
(Central Apennines, Italy). Geol. J., DOI: 10.1002/gj.1191.
GALLUZZO F. & SANTANTONIO M. (2002) – The Sabina Plateau:
a new element in the Mesozoic palaeogeography of Central
Apennines. Boll Soc. Geol. It., Vol. Spec. n. 1, 561-588.
GIANNINI E., LAZZAROTTO A. & ZAMPI M. (1970) – Studio
stratigrafico e micropaleontologico del Giurassico della
Montagna dei Fiori (Ascoli Piceno – Teramo). Mem. Soc.
Geol. It., 9, 29-53.
MARINO M. & SANTANTONIO M. (2010) – Understanding the
geological record of carbonate platform drowning across
rifted Tethyan margins: Examples from the Lower Jurassic of
the Apennines and Sicily (Italy). Sediment. Geol., 225, 116-
137.
MATTEI M. (1987) – Analisi geologico-strutturale della
Montagna dei Fiori (Ascoli Piceno, Italia centrale). Geol.
Romana, 26, 327-347.

“Inner” and “outer” wedge-top sequences in the Late Miocene
Sicilian Foreland Basin System; inferences from the Upper Tortonian
– Lower Messinian Terravecchia Fm. of NW Sicily
Key words: Late Miocene, sedimentology, Terravecchia
Formation, wedge-top depozone.
INTRODUCTION
Sicily is a sector of the SE-verging alpine orogenic belt in the
Central Mediterranean area and has been interpreted as a result of
both post-collisional convergence between Africa and Europe and
rollback of the subduction hinge of the Ionian lithosphere
(CATALANO et alii, 2000 and references therein).
The migration of the thrust belt toward the external areas
begun since the latest Oligocene-early Miocene and has been
accompanied by the formation of a complex “peripheral”
foreland basin (DICKINSON, 1974) developed lying in the front
and partially above the growing orogenic building. This area of
major subsidence accommodates a thick sedimentary succession
made up of silico- and carbonate-clastics, evaporites and
carbonates filling the different depozones (CATALANO et alii,
1989; 2000; NIGRO &RENDA, 2000; GUGLIOTTA, 2010).
Between the Late Tortonian and Early Messinian time the
innermost sectors of this complex tettono-depositional area were
characterized by a wide wedge-top depozone (sensu DE CELLES
&GILES, 1996). The latter was characterized by several kinds of
synkinematics basins filled by the coarse clastic successions
pertaining to the Upper Tortonian – Lower Messinian
Terravecchia Formation (SCHMIDT DI FRIEDBERG, 1962). This
formation is characterized by a great variability of rock-types,
and sedimentary facies and shows quite different patterns of sindepositional
and post-depositional deformation comparing the
different basins of Sicily. Sedimentologic, stratigraphic and facies
analyses integrated with structural analyses have been performed
on Terravecchia Fm. cropping out in three main basins, located in
NW Sicily (Scillato, Ciminna and Camporeale basins, Fig. 1).
These analyses allowed to recognize two “end-member”
stratigraphic sequences characterized by quite diffferent
depositional and deformative patterns and which could have
_________________________
(*) Dipartimento di Geologia e Geodesia, Università degli Studi di Palermo,
c.gugliotta@unipa.it
CALOGERO GUGLIOTTA (*)
731
Fig. 1 – Shaded relief showing the location of the study areas
recorded deposition in different sectors of the wedge-top
depozone.
INNER WEDGE-TOP SEQUENCE
This sequence (up to 1300 meters thick) is mainly composed
of alluvial to transitional facies associations arranged with a
fining- to coarsening upward trend. It is made up by, from the
bottom:
- stacked amalgamated to unamalgamated and crudely bedded
conglomerates (with crystalline basement-derived clasts) passing
into cross-stratified sandstones and clays interpreted as an
entrenced (incised) stream valley fill evolving into low energy
alluvial plain with ephemeral ponds;
- interbedded silti-clays, cross-stratified sandstones and
conglomerates arranged in 60 up to 120 metres-thick, coarsening
upward, mouth bar parasequences, arranged with a backstepping
stacking pattern. These parasequences have been related to a
retrograding river-dominated delta front;
- silti-clays and clays with brackish fauna, locally interbedded
with centimetre-thick sandy layers (flood-generated hyperpycnal
flows deposits) passing upward into marine marls with planktonic
microfauna. This portion of the sequence has been related to a
distal delta front passing into brackish prodelta and marine
environment;
- yellowish silti-clays interbedded with tabular- to lent-shaped
conglomerate bodies (up to 8m thick) and sandstones deposited
in a prograding distal fan delta front with slump scars;
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SESSIONE 23
- interbedded conglomerates, sandstones and sandy-clays
arranged in 60 up to 120 metres-thick, coarsening upward, mouth
bar parasequences, arranged with a thickening upward stacking
pattern. These parasequences have been related to a prograding
river-dominated delta front;
- conglomerates and cross-stratified sandstones arranged in
fining upward sequences (meter in scale) stacked along planarshaped
to concave-up erosional surfaces. This deposits have been
related to a gravelly delta-top environment.
Evidences of a severe “local scale” syn-depositional (e.g.
syntectonic intraformational angular unconformities of RIBA,
1976, sudden change of palaeoflow direction and growth
geometries) and post-depositional tectonics have been widely
observed throughout the sequence. The inner wedge-top
sequence develops above an angular unconformity with strong
“incised” features. The latter cut the uppermost units of the
tectonic edifice (Sicilide and decolléd Numidian Flysch units)
and/or an already deformed thrust-top succession pertaining to
the Upper Serravallian - Lower Tortonian Castellana Sicula Fm.
OUTER WEDGE-TOP SEQUENCE
This sequence (up to 700 meters thick) is mainly composed of
transitional to open marine facies associations arranged with an
overall fining upward trend which locally (at the base) become
coarsening- to fining- upward. It is made up by, from the bottom:
- conglomerates and cross-stratified sandstones arranged in
fining upward sequences (up to 5 meters thick) stacked along
planar-shaped to slightly concave-up erosional surfaces. This
deposits have been related to an unconfined external gravelly
braidplain environment;
- interbedded silti- to sandy-clays, cross-stratified sandstones
and conglomerates arranged in 60 up to 120 metres-thick,
coarsening upward, shoreface “parasequences”, arranged with a
backstepping stacking pattern. These parasequences have been
related to a retrograding wave and storm-dominated delta front
setting;
- sandy to silti-clays and marls with planctonic foraminifers
and calcareous nannofossils locally interbedded with thin layers
of sandstones and matrix-supported conglomerates. These
deposits have been related to an offshore-transition to offshore
environment with sporadic storm-induced gravity flows.
No evidences of a “local scale” syndepositional tectonics have
been observed along this sequence while, a severe postdepositional
deformation is clearly identifiable. The outer wedgetop
sequence develops above an angular unconformity with no
“incised” features. The latter cut both an already deformed thrusttop
succession pertaining to the Upper Serravallian - Lower
Tortonian Castellana Sicula Fm. and/or the Numidian Flysch
tectonic units which are tectonically superimposed to the deeper
carbonate platform units.
732
CONCLUSIVE REMARKS
During the Late Tortonian to Early Messinian time the
Sicilian fold and thrust belt was associated to a peripheral
foreland basin in which a wide continental to shallow-water
wedge-top depozone developed above the growing thrust sheets.
In this depozone the Teravecchia Fm. was deposited filling wide
to quite narrow sedimentary basins located at different structural
position. In the inner wedge-top depozone the Terravecchia Fm.
was deposited as coarse continental to transitional sequences
filling narrow, often oversupplied basins, recording a strong
syntectonics deformation since the Late Tortonian time.
Contemporaneously, coarse- to fine-grained sequences were
deposited in the outer wedge-top depozone filling wider and
mainly shallow-marine basins. These latter have been strongly
deformed since the Early Messinian time.
REFERENCES
CATALANO R., D’ARGENIO B. & TORELLI L. (1989) – From
Sardinia channel to Sicily straits. A geologic section based on
seismic and field data. In: A. Boriani, M. Bonafede, G.B.
Piccardo and G.B. Vai (Eds.) - The lithosphere in Italy.
Advances in Earth science research. Atti dei Convegni Lincei,
Roma, 109-127.
CATALANO R., FRANCHINO A., MERLINI S., & SULLI A. (2000) -
Central western Sicily structural setting interpreted from
seismic reflection profiles. Mem. Soc. Geol. It., 55, 5-16.
DE CELLES P. G. & GILES K. A. (1996) - Foreland Basin Systems.
Basin Res., 8, 105-123.
DICKINSON W. R. (1974) – Plate tectonics and sedimentation. In:
W.R. Dickinson (Ed.) – Tectonics and Sedimentation. Spec.
Pub. Soc. Econ. Paleont. Mineral.,Tulsa, 22, 1-27.
GUGLIOTTA C. (2010) – L’evoluzione tortoniano-messiniana
dell’avanfossa siciliana; interazione tra sedimentazione e
tettonica. Tesi di Dottorato. Università di Palermo.
NIGRO F. & RENDA P. (2000) - Un modello di evoluzione tettonosedimentaria
dell’avanfossa neogenica siciliana. Boll. Soc.
Geol. It., 119, 667-686.
RIBA O. (1976) – Syntectonic unconformities of the Alto
Cardener, spanish Pyrenees: a genetic interpretation.
Sediment. Geol., 15, 213-233.
SCHMIDT DI FRIEDBERG P. (1962) - Introduction a la géologié
pétrolière de la Sicilie. Revue. Inst. Franc. Du Petr., 17(5),
635-669.

Tectonically-enhanced deposition in the Late Tortonian Scillato
Basin (N Sicily): a sequence stratigraphic view
Key words: Depositional pattern, northern Sicily, Scillato basin,
sedimentology, sequence stratigraphy, Terravecchia Fm.
INTRODUCTION
During the Late Miocene time the Sicilian fold and thrust belt
was associated to a peripheral foreland basin in which a wide
continental to shallow-water wedge-top depozone developed
above the growing thrust sheets. In this depozone the Upper
Tortonian – Lower Messinian Teravecchia Fm. (SCHMIDT DI
FRIEDBERG, 1962) was deposited filling wide to quite narrow
sedimentary basins whose present day remnants outcrop in
northern and north-western Sicily (GUGLIOTTA, 2010). Among
these, the Scillato Basin is a small N-S-trending depression that
has been considered as a remnant of a small basin developed
since the Late Tortonian (CATALANO & D’ARGENIO, 1990;
BUTLER & GRASSO, 1993; GIUNTA et alii, 2000). In
correspondence of this basin an up to 1300 m thick Upper
Tortonian stratigraphic succession pertaining to the Terravecchia
Fm. is exposed (CATALANO &D’ARGENIO, 1990) lacking of the
Lower Messinian rocks (GUGLIOTTA, 2010). The sedimentary
succession rests unconformably on the already deformed tectonic
units (Sicilide and/or Numidian Flysch) or overlies (southern
edge of the basin) an Upper Serravallian - Lower Tortonian
succession (Castellana Sicula Fm.) through a regional angular
unconformity with strong erosional character.
Detailed sedimentologic, stratigraphic and facies analyses
performed on Terravecchia Fm. cropping out in the Scillato Basin
allowed to recognize the main facies associations and to point out
their arrangement in the frame of sequence stratigraphy.
FACIES ASSOCIATIONS
Along the studied stratigraphic succession seven main facies
associations (f.a.) have been recognized:
- Incised stream valley fill (A)
_________________________
(*) Dipartimento di Geologia e Geodesia, Università degli Studi di Palermo,
c.gugliotta@unipa.it; agate@unipa.it
CALOGERO GUGLIOTTA (*) & MAURO AGATE (*)
733
Amalgamated, crudely bedded cobble- and boulder
conglomerates (with crystalline basement-derived clasts) passing
into boulder- and pebble conglomerates and cross-stratified
sandstones arranged in unamalgamated, fining upward, braided
channel units (metre in scale).
- Low energy alluvial plain with ephemeral ponds (B)
Massive dark grey to yellowish silti-clays and clays with
interbedded lent-shaped bodies (metre in scale) made up of
pebble conglomerates and sandstones interpreted as isolated
channel units. This facies association appears arranged with an
overall fining upward trend.
- Retrograding river-dominated delta front (C)
Interbedded silti-clays, cross-stratified sandstones and
conglomerates arranged in 60m up to 120m-thick, coarsening
upward, mouth bar parasequences. These parasequences appear
arranged with a backstepping (thinning upward) stacking pattern-
- Distal delta front and prodelta (D)
Silti-clays and clays with brackish fauna, locally interbedded
with centimetre-thick sandy layers interpreted as flood-generated
hyperpycnal flows deposits. This facies association appears
arranged with a fining to coarsening upward trend given by the
progressive increase in thickness and frequence of sandy layers
toward the top.
- Prograding distal fan delta front with slump scars (E)
Yellowish silti-clays interbedded with tabular- to lent-shaped
boulder to pebble conglomerate bodies (up to 8m thick)
associated with planar- to cross-stratified sandstones.
- Prograding river-dominated delta front (F)
Interbedded conglomerates, cross-stratified sandstones and
sandy-clays arranged in 60 up to 120 metres-thick, coarsening
upward, mouth bar parasequences, arranged with a thickening
upward stacking pattern.
- Delta-plain (G)
Conglomerates and cross-stratified sandstones arranged in
fining upward braid channel units (meter in scale) stacked along
planar-shaped to concave-up erosional surfaces.
Evidences of an active syn-depositional tectonics have been
observed and fully described throughout the entire succession
(GUGLIOTTA, 2010). Several syntectonic intraformational angular
unconformities (RIBA, 1976) have been found (i) at the base of
facies association C; (ii) at the base of facies association F and
(iii) at the base of facies association G. These unconformities are
also associated with sudden change in the mean palaeoflow
SESSIONE 23

SESSIONE 23
direction, with evidence of “cannibalistic” erosion of the basin
margins and with development of growth stratal patterns.
DEPOSITIONAL MODEL AND SEQUENCE
STRATIGRAPHY
The above mentioned facies associations are arranged to
constitute a complex sedimentary sequence which shows a finingto
coarsening- and shallowing upward trend. Along this, three
main depositional stages have been recognized and interpreted
from a sequence stratigraphy point of view basing also on what
described in neighbour similar basins (see LO CICERO et alii.,
1997).
-Confined braidplain stage
This depositional stage is characterised by the couple A-B
facies associations. It overlays at the base an erosional
unconformity interpreted as a subaerial unconformity. The
stacked channel units (f.a. A) are interpreted as representing an
LST deposit. Toward the top, the decrease of channels
amalgamation, of bedload size and the occurrence of low energy
braidplain clays with isolated channels (f.a. B) is interpreted as
the transition to the early TST;
- Retrograding river-dominated fan delta system stage
This depositional stage is imaged by the superimposed C-D
facies associations. The “backstepping” delta front parasequences
(f.a. C) interfinger toward the top with the prodelta deposits (f.a
D) imaging a well developed TST. The ravinement surface
associated to the TST is not well recognizable probably because
it reworks the underlying subaerial unconformity becoming part
of the sequence boundary. Toward the top, the evolution from a
fining- to a coarsening upward trend is interpreted as the sign of
the maximum flooding surface and the transition to the HST.
- Prograding river-dominated fan delta system stage
This depositional stage involves the facies association E-F;
particularly the facies association E could record the early stage
of progradation of the delta front systems accompanied by a
sudden steepening of the delta slope. The rapid progradation of
delta front and delta plain deposits (f.a. F) seams to be driven by
the forced regression of the shoreline and by the local
“cannibalization” of the basin margins (induced by the tectonic
enhancement of the source areas). This feature contribute to
preliminalrly interpret this depositional stage as the record of a
falling stage systems tract (FSST) bounded at it’s base by a
complex surface roughly correspondent to the basal surface of
forced regression. The latter not also overlays the chain units
(Sicilide and Numidian Flysch) but cut and reworks the already
deformed Terravecchia Fm. strata (A, B, C f.a. as well as the
bounding surfaces) marking a precise evidence of the interplay
between tectonics and sedimentation in this basin (see
GUGLIOTTA &GASPARO MORTICELLI, this volume, for details).
734
CONCLUSIONS
The Terravecchia Fm. that crops out in the Scillato Basin is
arranged as an up to 1300 m thick stratigraphic succession
deposited during the Late Tortonian. The facies assemblage and
the depositional arrangement of this formation allowed to
recognize three main depositional stages: (i) Confined braidplain,
(ii) retrograding river-dominated fan delta system, (iii)
prograding river-dominated fan delta system superimposed
following the relative variations of sea level and the
decreasing/increasing rate of sedimentary supply.
A complete depositional sequence (see depositional sequence
IV of CATUNEANU, 2002 and references therein) has been
recognized in the basin, characterized by a basal LST, an
intemediate TST and HST capped by an upper FFST. A complex
set of “embricated” angular and syntectonic intraformational
angular unconformities recognized at the base and along of the
sedimentary sequence allowed to point out the intimate interplay
between tectonics and sedimentation in this basin. As a
consequence the development of the recognized systems tracts
are here considered tectonically-enhanced and so they assume a
strong local character.
REFERENCES
BUTLER R. & GRASSO M. (1993) - Tectonic controls on base-level
variations and depositional sequences within thrust-top and
foredeep basins: Examples from the Neogene thrust belt of
Central Sicily. Basin Res., 5, 137-151.
CATALANO R. & D’ARGENIO B. (1990) - Hammering a seismic
section. Guide book of the field trip in western Sicily.
International Conference “Geology Of The Oceans”, Terrasini
(Pa), May 17-19.
CATUNEANU O. (2002) – Sequence stratigraphy of clastic systems:
Concepts, merits and pitfalls. J. Afr. Earth Sci., 35, 1–43.
GIUNTA G., NIGRO F. & RENDA P. (2000) - Extensional tectonics
during Maghrebides chain building since Late Miocene:
Expamples from northern Sicily. Ann. Soc. Geol. Pol., 70, 81-98.
GUGLIOTTA C. (2010) – L’evoluzione tortoniano-messiniana
dell’avanfossa siciliana; interazione tra sedimentazione e
tettonica. Tesi di Dottorato, Università degli Studi di Palermo,
236 pp.
RIBA O. (1976) – Syntectonic unconformities of the Alto Cardener,
spanish Pyrenees: a genetic interpretation. Sediment. Geol., 15,
213-233.
SCHMIDT DI FRIEDBERG P. (1962) - Introduction a la géologié
pétrolière de la Sicilie. Revue. Inst. Franc. du Petr., 17(5), 635-
669.

Key words: Northern Sicily, Scillato basin, syntectonic
sedimentation, Terravecchia Fm.
INTRODUCTION
In central-northern and NW Sicily the building of the sicilian
fold and thrust belt (SFTB) occurred since the Early-Middle
Miocene developing toward two successive tectonic events
(CATALANO et alii, 2000).
Between the Langhian to Serravallian time interval
Cretaceous – Paleocene hemipelagites pertaining to Sicilide Units
(SU) ovethrusted the Oligo – Miocene and partially decollèd
Numidian Flysch Units (NFU). Subsequently (since Early
Tortonian), basin - to - slope carbonates (Imerese Units, IMU)
have been deformed in several tectonic units and stacked above a
carbonate platform rock body through low-angle, SW-vergent
thrusts, associated with NW-SE-trending folds (event 1). During
the Latest Miocene – Early Pliocene (event 2) the deformation
reached the deepest carbonate platform units. The already
emplaced tectonic units have been passively re-deformed and
strongly dissected by mean of S-verging, deep-seated thrusts
associated with backthrusts and E-W-, NE-SW-trending folds
(AVELLONE et alii, 2010).
During the Late Miocene time the SFTB was associated to
development of wide to quite narrow syntectonics basins partly
located above the growing thrust sheets (wedge-top depozone),
filled by the Upper Tortonian - Lower Messinian Terravecchia
Fm. (SCHMIDT DI FRIEDBERG, 1962). Among these “thrust-top”
basins (ORI &FRIEND, 1984) the Scillato Basin (SB) is a narrow
depression developed since the Late Tortonian.
_________________________
Evidences of a polyphasic tectonics in a sedimentary basin
developed above an orogenic belt; the Scillato Basin study case
(N Sicily)
STRATIGRAPHIC FEATURES
(*) Dipartimento di Geologia e Geodesia, Università degli Studi di Palermo,
c.gugliotta@unipa.it, mgasparo@unipa.it
CALOGERO GUGLIOTTA (*) & MAURIZIO GASPARO MORTICELLI (*)
735
The SB is filled by an up to 1300 m thick Upper Tortonian
stratigraphic succession pertaining to the Terravecchia Fm.,
lacking of the Early Messinian rocks (GUGLIOTTA, 2010).
The Terravecchia Fm. develops above a regional angular
unconformity (S1) with strong erosional features whose cut the
already deformed substrate made up by SU and (southern edge of
the basin) the Upper Serravallian-Lower Tortonian Castellana
Sicula Fm.. The Terravecchia Fm. is characterized by a complex
facies assemblage in which a confined braidplain, retrograding
river-dominated fan delta system and prograding river-dominated
fan delta system environments have been distiguished
(GUGLIOTTA, 2010). The facies assemblage is arranged with a
fining to coarsening upward trend along which an earlier
“trasgressive stage” (TS) and a later “regressive stage” (RS)
have been recognized. Growth geometries and several (three at
least) syntectonic intraformational angular unconformities (RIBA,
1976) have been found along the succession. Among these, the S3
surface is the most important. It develops with erosional features
from the eastern and north-eastern margins of the basin, where it
cuts the older S1 and the SU substrate, progressively disappearing
toward the basin depocentre. Along this surface a discordance is
also observable between the less deformed RS (above) and the
well deformed TS (below) (Fig. 1). Through the S3 surface a
Fig. 1 – Inferred tectono-depositional sketch for the Scillato Basin evolution;
see text for acronyms.
SESSIONE 23

SESSIONE 23
sudden change in the mean palaeocurrent direction has been
documented (from prevalently SE in the TS to WNW in the RS)
also associated with a clear evidence of variation in source areas
position and “cannibalistic” erosion of the basin margins.
DEFORMATIVE PATTERN
The SB appear as a roughly N-S-trending major asymmetric
syncline. A detailed bedding analyses performed on Terravecchia
Fm. strata allowed to recognize that TS and RS show a different
deformative pattern. In particular, the TS is deformed as an
asymmetric syncline with a well deformed southeastern forelimb
(up to 70° of strata inclination). On the other hand the RS strata
appear as a less deformed NW-dipping monocline. The
interference between this two deformative patterns produced the
N-S trend of the major syncline.
The SB is bordered eastward and southward by structural
highs, respectively Cervi and Rocca di Sciara ridges. Field data
allowed to interpret these ridges as partially outcropping NW-SEtrending
ramp anticlines, the innermost Cervi Anticline CA, and
the outermost Rocca di Sciara Anticline, RA, respectively. These
anticlines are related to SW-verging thrusts involving the IMU
tectonic units (event 1). The “exhumed” thrust related to the CA
nucleation outcrops along the southwestern slope of the Cervi
ridge. Data collected along the CA forelimb (minor folds and
pressure solution cleavage-extensional veins systems) highlight
the presence of two main plicative systems respectively NW-SEtrending
(N330°) (H1) and ENE-WSW-trending (N60°) (H2).
Cross-cutting relationships between these two systems allowed to
recognize that H2 (earlier) is superimposed to the H1 (older).
The CA is characterized by a well observable SE-dipping
axis; moving north-westward the latter results cut and displayed
by a NE-SW-trending (N350°) major transpressive, left-lateral,
fault (Cervi Fault), developed in a stress field compatible with H2
folds system (event 2). Analogues structures have been
recognized on field along the RA limbs.
The structures above mentioned are compatible with a
maximum stress oriented respectively NE-SW (H1) and NNW-
SSE (H2 and Cervi Fault).
DISCUSSION AND CONCLUSIONS
The depositional pattern recognized in the older TS has been
interpreted as the sedimentary fill of a narrow morphostructural
depression with an about NW-SE-oriented axis. This data is also
supported by the average SE-oriented palaeoflow directions. The
beginning of the earlier RS recorded an increase in coarse-clastics
supply due both to an inferred tectonic enhancement of relief in
the source areas and to a cannibalistic erosion of the eastern basin
margin. This data are supported by the strong variation of
palaeoflow direction (WNW-directed) that confirm an occurred
736
major shifting of source area toward the Est during RS
deposition. The strong tectonic control on basin development is
also sustained by the recognizing within Terravecchia Fm. of
typical syntectonic stratal patterns such as syntectonic
intraformational angular unconformities and growth geometries
due to the progressive tilting of the steeper southern and eastern
margins of the basin.
The strong deformation and erosion of the eastern margin of
the SB has been related to the activity of the Cervi Fault occurred
at least during the deposition of the RS (Late Tortonian).
The different orientation of maximum stress recognized in
association to the main tectonic structures is in agreement with
the clockwise rotations of the tectonic units occurred during the
development of tectonics events 1 and 2 (OLDOW et alii, 1990).
In conclusion the SB developed as a NW-SE-trending thrusttop
basin, enclosed between two major thrust-related IMU
anticlines (CA and RA inherited from event 1), filled by the TS.
During a successive stage the intervening deformation and
uplifing of the CA by mean of the Cervi Faults induced the
deformation and partially erosion of the TS along the eastern
margin of the SB and the contemporaneous deposition (with
discordance) of the RS. Following as abovementioned the
Scillato Basin fills records an active polyphasic tectonics.
Moreover, the data here presented allowed to agedate the
onset of deep-seated tectonic event (event 2), in these areas, back
at least to the Late Tortonian.
REFERENCES
AVELLONE G., BARCHI M., CATALANO R., GASPARO MORTICELLI
M. & SULLI A. (2010) - Interference between shallow and
deep-seated structures in the Sicilian fold and thrust belt. J.
Geol. Soc. London, 167, 109–126.
CATALANO R., FRANCHINO A., MERLINI S. & SULLI A. (2000) -
Central western Sicily structural setting interpreted from
seismic reflection profiles. Mem. Soc. Geol. It., 55, 5-16.
GUGLIOTTA C. (2010) – L’evoluzione tortoniano-messiniana
dell’avanfossa siciliana; interazione tra sedimentazione e
tettonica. Tesi di Dottorato. Università di Palermo.
OLDOW J. S., CHANNEL J. E. T., CATALANO R. & D’ARGENIO,B.
(1990) - Contemporaneous thrusting and large-scale
rotations in the western Sicilian fold and thrust belt.
Tectonics, 9, 661-681.
ORI G.C. & FRIEND P.F. (1984) - Sedimentary Basins Formed
And Carried Piggyback On Active Thrust Sheet. Geology, 12,
475-478.
SCHMIDT DI FRIEDBERG P. (1962) - Introduction a la géologié
pétrolière de la Sicilie. Revue. Inst. Franc. Du Petr., 17(5),
635-669.

Constraining the onset and development of “deep-seated” tectonics
in the Sicilian thrust belt; field data from northern Sicily
CALOGERO GUGLIOTTA (*), GIUSEPPE AVELLONE (*), MAURIZIO GASPARO MORTICELLI (*) & MAURO AGATE (*)
Key words: Deep-seated tectonics, syntectonic deposition, Sicily.
INTRODUCTION
The Sicilian-Maghrebian fold and thrust belt developed since
the latest Oligocene/earliest Miocene as a consequence of the
collision between the Sardinian block and a segment of the
African continental margin (CATALANO et alii, 2000 and
references therein). The building up of the chain follows two
subsequent main compressional events, “shallow-seated” and
"deep-seated" respectively, whose structures are detached at
different structural level (AVELLONE et alii, 2010). During the
"shallow-seated" tectonic event, basin - to - slope carbonates
(Imerese-Sicanian domains) have been deformed in several
tectonic units and stacked above a carbonate platform rock body
(Panormide-Trapanese domains), through low-angle SO-verging
thrusts associated with NW-SE-trending folds. The “deep-seated”
tectonic event produced large double verging pop-up structures
affecting the whole tectonic stack, frequently resulting into large
folds, with vertical to recumbent limbs, accomplished by highangle
transpressive thrusts and backthrusts. The latter, passively
refolded the older thrusts inherited from “shallow-seated” event
(AVELLONE et alii, 2010). The age of the “shallow-seated” event
has been well constrained both from field and geophysical data to
the early-middle Miocene (CATALANO et alii, 2000 and reference
therein). On the other hand the onset of deep-seated structures in
northern Sicily is still matter of debate. In north-western Sicily,
CATALANO et alii, (2000) agedated the onset of the “deep-seated”
deformation to the Late Miocene - Early Pliocene time span. The
Messinian angular unconformities observed in the evaporitic
sequences outcropping in the Ciminna Basin (LO CICERO et alii,
1997) and subsurface data collected in the northern Madonie
offshore area (DEL BEN &GUARNIERI, 2000) indicate tectonic
activity during Messinian time. The difference in elevation of
lower Pliocene Trubi Fm. between the northern Madonie
Mountains area (100 m a.s.l.) and the central Madonie area
_________________________
(*) Dipartimento di Geologia e Geodesia, Università degli Studi di Palermo,
c.gugliotta@unipa.it, giuavellone@unipa.it, mgasparo@unipa.it,
agate@unipa.it
737
(1600m a.s.l.) suggests that, in this sector of the fold and thrust
belt, “deep-seated” deformation continued after Trubi deposition.
Some field evidences were here documented, from two well
exposed outcrop areas (Scillato and Lascari basins), with the
main aim to contribute to a better constraining of the onset and
timing of the deep-seated “transpressive” deformation in northern
Sicily.
Fig. 1 – Tectonic sketch showing the location of study areas.
THE SCILLATO BASIN STUDY CASE
The Scillato Basin (northern Sicily, Fig. 1) is a N-S-trending
depression bordered eastward and southward by structural highs,
respectively Cervi and Rocca di Sciara ridges (Imerese Units).
This depression has been considered as the remnant of a small
basin developed during the Late Tortonian. In correspondence of
the Scillato Basin an up to 1300m thick Upper Tortonian
stratigraphic succession pertaining to the Terravecchia Fm.
(TRV) (SCHMIDT DI FRIEDBERG, 1962). The TRV unconformably
rests on an already deformed substrate made up by Sicilide
tectonics units which in turn overthrusted the Numidian Flysch
units (between the Langhian and the Late Serravallian time).
Locally, the TRV covers the Upper Serravallian - Lower
Tortonian silti clays pertaining to the Castellana Sicula Fm..
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SESSIONE 23
The TRV is characterized by a complex facies assemblage in
which a lower “trasgressive stage” (TS) and a upper “regressive
stage” (RS) have been recognized (GUGLIOTTA, 2010).
Evidences of an active syn-depositional tectonics have been
observed and fully described throughout the entire succession
(for details see GUGLIOTTA, 2010). Several “embricated”
syntectonic intraformational angular unconformities (RIBA, 1976)
have been found (associated with sudden change in palaeoflow
direction, evidence of “cannibalistic” erosion and growth stratal
patterns) in the Upper Tortonian deposits. Detailed field
structural data collected both in the Scillato Basin sedimentary
fill and in the carbonate rocks (pertaining to the Imerese units)
outcropping in the neighbour Monte dei Cervi and Rocca di
Sciara allowed to consider that a severe transpressive tectonics
was active during the Late Tortonian time. As documented by the
AA high angle NW-verging transpressive faults affected these
areas after the emplacement of the “shallow-seated” structures
and have driven the contemporaneous deposition of the
“regressive stage” of the Terravecchia Fm.
THE LASCARI BASIN STUDY CASE
The Lascari Basin (Madonie Mountains, northern Sicily, Fig.
1) is a roughly E-W-trending depression filled by an up to 100m
thick succession of limestones, marls and calcarenites pertaining
to the Lower Pliocene Trubi Fm.. The latter, unconformably
overlays, through an angular unconformity with strong erosional
features, an already deformed tectonic stack made up of
Oligocene-Early Miocene marly-arenaceous deposits pertaining
to the Tufiti di Tusa Fm. (Sicilide Units) which in turn
overthrusted the Numidian Flysch units between the Langhian
and the Late Serravallian time span. Detailed stratigraphic,
sedimentologic and structural data coming from field study
(AVELLONE et alii, 2008) poited out the existence of
syntectonics-related growth geometries (associated with slumps
and earthquake-related structures) that involve the Zanclean
deposits. These geometries result from the progressive tilting of
the depositional surface occurred during Early Pliocene and
related to the nucleation of roughly E-W trending, N-ward
verging folds. The transpressive deformative field is associated
with the development of two conjugate sets of deep-seated
transpressive/transcurrent faults, NE-SW (left-lateral) and NW-
SE (right-lateral) oriented.
These transpression-related structure affected the Sicilide unit
floor thrust which previously formed “shallow-seated”
compressional structures. All the above mentioned data allowed
to consider that in these areas the “deep-seated” transpressive
tectonics was active at least during the earliest Pliocene
(Zanclean).
738
CONCLUSIVE REMARKS
New and mainly field-derived stratigraphic, sedimentologic and
structural data, pertaining the interplay between tectonics and
contemporaneous sedimentation allowed to point out some
remarks on the onset and development of the deep-seated
traspressive tectonics in the northern Sicily thrust belt. Data
coming from the Late Tortonian Scillato Basin pointed out that in
these areas the deep-seated transpressive tectonics have driven
the syntectonics deposition of the the “regressive stage”
recognized within the Terravecchia Fm.. This data allowed to
date the onset of this deformative event in the study areas back at
least to the latest Tortonian time. Moreover, as demonstrated by
syntectonics deposition of the Trubi Fm. in the Lascari Basin the
transpressive tectonics continued during the Zanclean age.
REFERENCES
AVELLONE G., BARCHI M., CATALANO R., GASPARO MORTICELLI M. &
SULLI A. (2010) - Interference between shallow and deep-seated
structures in the Sicilian fold and thrust belt. J. Geol. Soc. London,
167, 109–126.
AVELLONE G., GENNARO C., GASPARO MORTICELLI M. GUGLIOTTA C.
&AGATE M. (2008) - Syn-sedimentary tectonics during Early
Pliocene time in the northern Madonie Mountains (Sicily). Rend.
Online Soc. Geol. It., 3 (2008).
CATALANO R., FRANCHINO A., MERLINI S. & SULLI A. (2000) -Central
western Sicily structural setting interpreted from seismic reflection
profiles. Mem. Soc. Geol. It., 55, 5-16.
DEL BEN A. & GUARNIERI P. (2000) - Neogene transpression in the
Cefalù Basin (Southern Tyrrhenian): Comparison between land
and marine data. Mem. Soc. Geol. It., 55: 27-33.
GUGLIOTTA C. (2010) – L’evoluzione tortoniano-messiniana
dell’avanfossa siciliana; interazione tra sedimentazione e tettonica.
Tesi di Dottorato in Geologia XXI Ciclo. Dipartimento di Geologia
e Geodesia, Università degli Studi di Palermo, 236 pp.
LO CICERO G., DI STEFANO E., CATALANO R., SPROVIERI R., AGATE M.,
CONTINO A., GRECO G. & MAURO G. (1997). The Ciminna
evaporitic basin cyclical sedimentation and eustatic control in a
traspressive tectonic setting. In: R. Catalano (Ed.) - Time scales and
basin dynamics. Sicily, the adjacent Mediterranean and other natural
laboratories, 8 th Workshop Of The Ilp Task Force “Origin Of
Sedimenatry Basins”, Palermo (Sicily), June 7-13, 1997.
RIBA O. (1976) – Syntectonic unconformities of the Alto Cardener,
spanish Pyrenees: a genetic interpretation. Sedim. Geol., 15, 213-
233.
SCHMIDT DI FRIEDBERG P. (1962) - Introduction a la géologié
pétrolière de la Sicilie. Revue. Inst. Franc. Du Petr., 17(5), . 635-
669.

Key words: Corals, East Alborz Lower Carboniferous, north
Damghan.
A Balast stratigraphical section was studied at the north
Damghan. These sections have been composed by limestone
alternate with shale of Tournaisian and Visean in age. Up to 20
species of corals belong to 11 genera have been distinguished.
The following species are: Sychnoelasma sp., Caninia
cornocopiae, Caninia ? lonsdaleiforme, Caninia ? sp.,
Pseudozaphrentoides ? sp., Siphonophyllia iranica,
Siphonophyllia cf, dorlodoti, Siphonophyllia cylindrica
cylindrical, Siphonophyllia cf. samsonensis, Heterocaninia sp.,
Dibunophyllum bipartitum, Arachnolasma sp. A,
Kueichouphyllum alborzense minor, Kueichouphyllum
crassiseptum, Kueichouphyllum lalunense, Tehranophyllum sp.
A, Tehranophyllum sp. B, Tehranophyllum sp. C, Michelinia
megastoma, Syringopora sp.
Stratigraphical section of north Damghan show regressive
sequence from Tournaisian to Lower Visean. Three main
environments containing rugosa and tabulate corals were
identified: open shelf to oolitic shoals. According to corals
morphology, three ecological assemblages were distinguished.
First is compost of solitary, undissepimented rugosa corals. It
consist of Cyathaxonia fauna that corresponding to Lower
Tournaisian. Second assemblage is composed of solitary
dissepimented rugosa corals of median to large sizes.
This assemblage occurs at shallow areas of the open shelf.
The age of this assemblage is Upper Tournaisian. Third
assemblage is composed of solitary dissepimented rugosa corals
of big size and occurs at massive oolitic limestones of upper part
of section and corresponding to shoal areas of Lower Visean in
age. Lower Carboniferous corals of Balast stratigraphical section
have been compared with Lower Carboniferous corals of another
part of Iran.
Iranian Lower Carboniferous corals belong to shallow areas
of open shelf of unique oceans.
_________________________
Lower Carboniferous biostratigraphy, paleoecology and
biogeography of Balast section, north of Damghan, Iran
(*) High Education Center of Jahad Keshavarzi, Hemat Av. Karaj, Iran.
kavehkhaksar@gmail.com
(**) Payam-e-nur University, Damghan, Iran.
KAVEH KHAKSAR (*) & MOHAMMED REZA KEBRIAEE-ZADEH (**)
739
SESSIONE 23

SESSIONE 23
Corals association in the Mobarak formation, section of
South Vali-Abade, in Marzan-Abad (North Iran)
KAVEH KHAKSAR (*), FATEMEH REZVAN NIA (**), MOHAMAD R. KEBRIAEE ZADE (**) & KEYVAN KHAKSAR (°)
Key words: Central Alborz, corals, Lower Carboniferous,
Mobarak formation, Vali-Abad section.
The Mobarak formation in the Vali-Abad section, southern
Marzan-Abad, in Central Alborz, is composed of alternating
limestone and schists. It is 200 m thick and is divided in three
lithologic units.
On the basis of microfacies studies, corals associations,
lithological compositions and field data, we deduced that it was
formed in a shallow carbonatic shelf. On the basis of the present
corals characteristic the Mobarak formation was deposited during
the lower carboniferous between the Upper Tournaisian and the
Visean-Namurian.
Two species of tabulate corals belonging to two different
genera have been individuated and assigned to two local zone
associations. The former belongs to the lithozone B, and was
deposited in a shallow shelf built up by oolitic shoals,
Tournaisian to Middle Visean in age. All the corals belonging to
this association are solitary and of large sizes. The latter
association belongs to lithozone C, and was deposited between
the Upper Visean and the Namurian.
_________________________
(*) Department of Soil and Water Science, Institute of Scientific Applied
High Education of Jihad-e-Agriculture, IRAN, kavehkhaksar@gmail.com
(**) Geology group of Faculty of Science of Tehran Payam Noor
University, Iran
(°) Islamic Azad University, Qom branch, Iran.
740

Key words: Facies analysis, sequence stratigraphy, Siena Basin.
Continental-to-inner shelf deposits typically provide a
sensitive record of relative sea-level fluctuations as even lowamplitude
relative sea-level changes are manifested by significant
facies shifts with associated development of erosional surfaces
(e.g. subaerial unconformities, ravinement surfaces, etc.).
Specifically, outcrop studies of these deposits provide analogues
for prediction of small-scale reservoirs geometries and
heterogeneities at sub-seismic scale.
The present study focuses on the Pliocene deposits exposed in
a key-area in the northern Siena Basin (Monteaperti-Castelnuovo
Berardenga area) whose stratigraphic architecture has been
refined through new fieldwork based on facies analysis and
sequence stratigraphic concepts.
The Siena Basin is one of the widest Neogene-Quaternary
basins of Tuscany and its Pliocene fill in the investigated area
consist of a relatively monotonous alternation of sand and mud
packages with minor conglomerates. These deposits have been
traditionally divided according to lithostratigraphic criteria and
interpreted as the record of a unique transgressive-regressive
cycle spanning from Early Pliocene to Middle Pliocene
(COSTANTINI et alii, 1982). Contrary, we recognized 4
depositional sequences (labeled S1 to S4 in upward stratigraphic
order) thus establishing a new stratigraphic framework. They are
representative of alluvial-to-inner shelf settings and point to a
more complex depositional history than previously described for
this sector of the basin.
Except for sequence S4, characterized by a well developed
FSST of deltaic deposits, each sequence consists of a poorly
developed FSST/LST, typically made of fluvial-to-deltaic
deposits, covered by nearshore-to-offshore sediments of TST.
Furthermore, units S2 to S4 also consist of offshore-to-nearshore
sediments pertaining to the HST. TST deposits show a great
variability from one sequence to another, ranging from very thin
_________________________
Sequence stratigraphic architecture of the Pliocene strata of the
northern Siena Basin (Tuscany, Italy)
(*) Dipartimento di Scienze della Terra, Università di Siena,
martini.ivan@unisi.it
(**) Weatherford Petroleum Consultants AS, Bergen, Norway.
Lavoro eseguito con il contributo finanziario dell’Università di Siena (PAR
Sandrelli).
IVAN MARTINI (*), MAURO ALDINUCCI (**) & FABIO SANDRELLI (*)
741
(< 1 m) shoreface sand to decameter-thick shoreface-to-deltaic
packages organized into retrogradational parasequences. Finally,
inferences on eustatic vs tectonic control on sequences
development have been made based on stratigraphic and regional
constraints, and sequences architecture.
REFERENCES
COSTANTINI A., LAZZAROTTO A. & SANDRELLI F. (1982) –
Conoscenze geologico-strutturali. In: AA.VV. – Il Graben di
Siena. CNR, Progetto Finalizzato Energetica, Sottoprogetto
Energia Geotermica. Final Report, Pisa, 11-34.
SESSIONE 23

SESSIONE 23
Stratigraphic architecture of basin-margin deposits in the Bradanic
Trough: changes in geodynamics vs. sea-level changes
Key-words: Bradanic trough, foreland basin fill, geodynamics
vs. sea-level changes, southern Italy.
The outcropping part of the in-fill succession of the
Bradanic Trough (the Southern Appennines foredeep) is
represented by a Pleistocene regressive succession made up of
silty clay deposits (argille subappennine Formation) followed
by sandstones and/or conglomerates belonging to paralic,
deltaic and/or alluvial environments (TROPEANO et alii, 2002).
In each sector of the basin, these coarse-grained deposits,
named “Regressive coastal deposits” by PIERI et alii (1996),
represent the top of the foredeep successions and diacronously
develop onto the argille subappennine Formation alternatively
in transitional or erosional contact. The argille subappennine
deposits become younger and younger toward the Ionian coast
and their sedimentation at present survives in the offshore
setting of the Taranto Gulf. Accordingly, the highest and oldest
“Regressive coastal deposits” are located in the middle of the
Bradanic Trough near the chain border (Banzi-Genzano area),
whilst younger deposits prograde towards the Taranto Gulf.
In the Banzi-Genzano area, the coarse-grained part of the
regressive suite is composed of several alluvial/delta bodies
with an aggradational configuration (a vertical stacking pattern)
while, southward, starting from the Irsina-Grassano area,
alluvial/delta bodies show a downward shifting configuration (a
progradational, offlapping, stacking pattern). Change in style of
stacking of alluvial/delta bodies could be interpreted as the
record of a major change in the geodynamic behaviour of the
Bradanic Trough which, during filling, recorded the passage
from a still subsiding basin to an uplifting one.
In detail, the "Regressive coastal deposits" of the Banzi-
Genzano area show a stratigrafic pattern induced by highfrequency
sea-level changes in a sector of the Bradanic Trough
where the rate of sedimentation compensated the rate of
subsidence (CILUMBRIELLO et alii, 2008a). Toward the SE of
the Banzi-Genzano area, in the adjacent Irsina-Grassano area,
the downward-shifting configuration that characterizes the
_________________________
MARCELLO TROPEANO (*), LUISA SABATO (*) ANTONIETTA CILUMBRIELLO (*) & PIERO PIERI (*)
(*) Dipartimento di Geologia e Geofisica, Università "Aldo Moro" di Bari
m.tropeano@geo.uniba.it, l.sabato@geo.uniba.it.
742
“Regressive coastal deposits” is interpreted to derive from
high-frequency sea-level changes in an uplifing context
(TROPEANO et alii, 2002; SABATO et alii, 2004). Moreover, in
the southernmost part of the Bradanic Trough, the "Regressive
coastal deposits" are represented by the well-known “marine
terraced deposits” of Metaponto (VEZZANI, 1967; BRÜCKNER,
1980), which correspond to wedges with a complex internal
stratigraphic arrangement induced by very high-frequency
relative sea-level changes (CILUMBRIELLO et aii., 2008b).
Wedges shifted during time up to the present-day coastal area
still in response to interferences between high-frequency sealevel
changes and uplift of the area but this downward-shifting
configuration differs from that observed in the Irsina-Grassano
area since each wedge is detached from the others. Changes in
style of downward-shifting configurations could have been
produced either by variation in amplitudes of high-frequency
sea-level changes or by changes in rates of uplift.
REFERENCES
BRÜCKNER H. (1980) - Marine terrasen in Süditalien. Eine
quartärmorphologische. Studie über das Kustentiefland von
Metapont. Düsseldorfer Geographische Schriften, 14, 235
pp.
CILUMBRIELLO A., SABATO L. & TROPEANO M. (2008a) -
Problemi di cartografia geologica relativa ai depositi
quaternari di chiusura del ciclo della Fossa bradanica:
l'area chiave di Banzi e Genzano di Lucania (Basilicata).
Mem. Descr. Carta Geol. It., 77, 119-146.
CILUMBRIELLO A., TROPEANO M. & SABATO L. (2008b) - The
Quaternary terraced marine-deposits of the Metaponto
area (Southern Italy) in a sequence-stratigraphic
perspective. Geoacta, Spec. Publ., 1, 27-54.
PIERI P., SABATO L. & TROPEANO M. (1996) - Significato
geodinamico dei caratteri deposizionali e strutturali della
Fossa bradanica nel Pleistocene. Mem. Soc. Geol. It., 51,
501-515.
SABATO L., TROPEANO M. & PIERI P. (2004) - Problemi di
cartografia geologica relativa ai depositi quaternari del
F°471 “Irsina”. Il Conglomerato di Irsina: mito o realtà?
Il Quaternario, 17(2/1), 391-404.

TROPEANO M., SABATO L. & PIERI P. (2002) - Filling and
cannibalization of a foredeep: Bradanic Trough, southern
Italy. Geol. Soc. Spec. Publ., 191, 55-79.
VEZZANI L. (1967) - I depositi plio-pleistocenici del litorale
ionico della Lucania. Atti Acc. Gioenia Sc. Nat., 18, 159-
180.
743
SESSIONE 23

SESSIONE 23
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SESSIONE 23

SESSIONE 23
746

SESSIONE 24
I sistemi misti terrigeno-carbonatici nel contesto
mediterraneo
CONVENERS
Gabriele Carannante (Università di Napoli)
Marcello Tropeano (Università di Bari)
747
SESSIONE 24

SESSIONE 24
Depositional model and paleodepth reconstruction of a coral-rich,
mixed siliciclastic-carbonate system: the Burdigalian of Capo Testa
(Northern Sardinia, Italy)
Key words: Burdigalian, corals, Mediterranean, facies,
paleodepth.
In the fossil record, but also at the present time, it is quite
common to find coral reefs that are physically related to
terrigenous sediments. In such environments, coral build-up
location, morphology and internal structure are controlled
primarily by the clastic sedimentary system rather than by the
independent growth of the framework builders, as in normal reef
environments.
This study presents a detailed facies analysis and paleodepth
reconstruction of a coral-rich mixed siliciclastic- carbonate
system Burdigalian in age, outcropping in the northern sector of
Sardinia (Capo Testa). Excellent exposures of 1.5 Km continuous
sea-cliff outcrops around the south-western and north-eastern
sides of the Capo Testa promontory has allowed us to: (1) trace
stratigraphic surfaces; (2) document stratal geometries; (3)
discern details of the lithofacies and, (4) reconstruct the
paleodepths of the different depositional environments.
Paleodepth reconstruction is necessary for depositional
modelling, for sea-level reconstruction, and for basin analysis
Such reconstructions have been conducted for various carbonate
and mixed carbonate systems (PERRIN et al. 1995; POMAR et al.
2002; BRANDANO et al. 2005, 2009; COFFEY &READ 2007)
based on the interpretation of paleoenvironmental facies using
paleoecological and sedimentological data. When these results
can be combined with spatial data, a reference model can be
created to interpret areas where lateral facies associations are not
available (e.g. extrapolation of drill core results, interpretation of
intensely tectonized outcrops, etc).
A total of seven sedimentary facies (F1-F7) has been
recognized and interpreted: siliciclastic conglomerate and coarse
bioclastic sandstone (F1), fine- to medium-grained hybrid
sandstone (F2), scleractinian coral domestone (F3), bioclastic
packstone to floatstone with platy Porites (F4), red algae
floatstone to rudstone (F5), larger benthic foraminifers (LBF)
_________________________
MARCO BRANDANO (*), LAURA TOMASSETTI (*), FRANCESCA BOSELLINI (**) & ANDREA MAZZUCCHI (°)
(*) Dipartimento di Scienze della Terra, Università di Roma “La Sapienza”,
marco.brandano@uniroma1.it
(**) Dipartimento di Scienze della Terra, Università di Modena e Reggio
Emilia
(°) Piazza Marianna Benti Bulgarelli 20, 00139 Roma
748
bioclastic rudstone floatstone in a packstone matrix (F6),
molluscan floatstone in a bioclastic packstone matrix (F7). The
absence of tectonic displacement and the possibility to follow
individual beds along the continuous sea-cliff outcrops, from the
highest point to the beach, has allowed us to define paleodepths
directly from the present day elevation of the recognized facies.
Moving down-dip (i.e., from southwest to northeast) the highest
facies is represented by F1, located at 50 m above present sea
level, whereas F5 and F6 outcrop at beach level. This difference
represents the paleodepth interval that is possible to observe in
the Capo Testa outcrop. The investigated system is characterized
by nearshore (0-15 m) to shoreface (15-30 m)deposits with a
conspicuous terrigenous content that grades seaward into deeper
zones where coral patch-reefs developed in association with
adjacent areas colonized by seagrass meadows (30-50 m). The
more distal facies are constituted by scattered encrusting tabular
colonies of Porites in growth position occurring in a deeper and
low-energy environment (45-50 m). The paleodepth interval that
is observed in the Capo Testa outcrop ranges from 0 to 50 m.
These results were then used to create a detailed depositional
model and paleodepth reconstruction of the entire Burdigalian
Capo Testa mixed depositional system.
REFERENCES
BRANDANO M., MATEU-VICENS G. & OBRADOR A. (2005) -
Comparative analysis of two Miocene carbonate platforms: a
distally steepened ramp (Menorca, Spain) and a low-angle
ramp (Latium Abruzzi, Italy). LESC Exploratory Workshop,
Potsdam, Germany 22-26 February, 8.
BRANDANO M., FREZZA V., TOMASSETTI L., PEDLEY M. &
MATTEUCCI R. (2009) - Facies analysis and
palaeoenvironmental interpretation of the Late Oligocene
Attard Member (Lower Coralline Limestone Formation),
Malta. Sedimentology, 56, 1138–1158.
COFFEY B.P. & READ J.F. (2007) - Subtropical to temperate
facies from a transition zone, mixed carbonate–siliciclastic
system, Palaeogene, North Carolina, USA. Sedimentology,
54, 339–365.

PERRIN C., BOSENCE D. & ROSEN B. (1995) - Quantitative
approaches to palaeozonation and palaeobathymetry of
corals and coralline algae in Cenozoic reefs. In: D.W.J.
Bosence, and P.A. Allison (Eds) - Marine
Palaeoenvironmental Analysis from Fossils. Geological
Society Spec. Publ., 83, 181-229.
POMAR L., OBRADOR A. & WESTPHAL H. (2002) - Sub-wavebase
cross-bedded grainstones on a distally steepened carbonate
ramp, upper Miocene, Menorca, Spain. Sedimentology, 49,
139-169.
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SESSIONE 24

SESSIONE 24
The bryomol carbonate factory of a mixed depositional system in the
Gelasian thrust-top setting of Acerenza (south-Apennines, Italy)
DOMENICO CHIARELLA (*), SERGIO G. LONGHITANO (*), LUIGI SPALLUTO (**) & MARCELLO TROPEANO (**)
Key words: Acerenza, Bryomol carbonate factory, Lucanian
Apennines, mixed (lithoclastic and bioclastic)
sedimentation, southern Italy.
During Gelasian times, laterally discontinuous successions
of mixed bioclastic-siliciclastic deposits characterized thrusttop
settings of the Lucanian Apennines in southern Italy. One of
the best exposed succession crops out in the vicinity of the
Acerenza village (Basilicata); sediments consist of sand-to
gravel-sized bioclastic debris mixed with quartz-rich sand and
gravel. This mixed succession shows a wide spectrum of crossstratifications
and cross-laminations suggesting the interaction
of hydrodynamic processes of different nature as currents and
waves; facies associations are vertically arranged in shallowingupward
parasequences (CHIARELLA & LONGHITANO, 2008,
2009).
The present study focuses on the carbonate factory
coexisting with terrigenous sedimentation and producing
bioclasts in the Acerenza setting. The carbonate fraction is
almost completely made up of fragments of bryozoans and
mollusks with minor contributions of benthic foraminifers,
planktonic foraminifers serpulids, echinoids, brachiopods,
barnacles and rare red algae. As a result, locally bryozoans and
mollusks are the most important sediment producing biota of
the carbonate factory (bryomol carbonates sensu NELSON et
alii, 1988).
The study of bryozoans morphotypes (i.e. zoarial forms) is
the most promising method to interpret environmental
conditions in which bryomol carbonates developed (e.g. BONE
&JAMES, 1993). In the studied succession all bryozoans belong
to the cheilostomata group and three main morphotypes have
been recognized: a) encrusting, multilamilar, either arborescent
or nodular celleporiform; b) erect, robust, lobate, bifurcate
branches adeoniform; c) erect, cylindrical branches, flexible
cellariform. The above association indicates shallow-to-mid
shelf environments characterized by high to moderate energy
_________________________
(*) Dipartimento di Scienze della Terra. Università della Basilicata.
(**) Dipartimento di Geologia e Geofisica. Università di Bari “Aldo Moro”.
l.spalluto@geo.uniba.it. m.tropeano@geo.uniba.it.
750
Fig. 1 – Encrusting, multilamilar, nodular celleporiform.
Fig. 2 – Erect, robust, lobate, bifurcate branches adeoniform.
levels, moderate to high sedimentation rates and flexible to hard
substrates.
Both stacking pattern of lithofacies with different
sedimentary structures and distribution and relative abundance
of different bryozoan morphotypes in the studied succession
reflect a shallowing-upward trend in each parasequence. In fact,
wave-dominated cross-bedded sandy bioclastic packstones and
grainstones forming the upper part of parasequences are
characterized by thicker and larger celleporiform forms in
association with flexible cellariform ones adapted to live in

Fig. 3 – Erect, cylindrical branches, flexible cellariform.
high-energy environments (BONE & JAMES, 1993). On the
contrary, smaller and thinner bryozoan colonies lived in
relatively deeper environments where currents produced crossbeds
of allochemic sandstones marking the lower and the
middle part of parasequences respectively. The carbonate
factory shut off during relative sea-level rises, since condensed
intervals and hardgrounds, indicating drowning phenomena,
mark the base of each parasequence.
REFERENCES
BONE Y. & JAMES N.P. (1993) – Bryozoans as carbonate
sediment producers on the cool-water Lapedece Shelf,
southern Australia. Sediment. Geol., 86, 247-271.
CHIARELLA D. & LONGHITANO S.G. (2008) – Sedimentary
features of the middle-upper Pliocene mixed bioclasticsiliciclastic
succession near Acerenza (Lucanian Apennines,
Southern Italy). In SABATO L. & TROPEANO M. – Plio-
Pleistocene stratigraphic and tectonic evolution of the
Souther Italy foredeep: key examples from South Apennines
front and Bradanic Trough (Basilicata Region). GeoSed
2008, Pre-congress field guide, Bari.
CHIARELLA D. & LONGHITANO S.G. (2009) – Sediment
segregation rate as tool for discriminating depositional
environments in ancient mixed (silici-bioclastic) shallowwater
marine systems (Pliocene, Southern Apennines, Italy).
Proceeding 27 th Meeting IAS 2009, Alghero.
NELSON C.S., HYDEN F.M., KEANE S.L., LEASK W.L. &
GORDON D.P. (1988) – Application of bryozoan zoarial
growth form studies in facies analysis of non-tropical
carbonate deposits in New Zealand. Sediment. Geol., 60,
301-322.
751
SESSIONE 24

SESSIONE 24
Key words: Bonifacio Strait, Maërl, mixed shelf, Posidonia
oceanica, sediment, sedimentological map.
INTRODUCTION
This paper presents the sedimentological map at 1:50,000
scale of the mixed carbonate-silicilastic inner shelf of the
Bonifacio straits.
The study has been carried out in order to evaluate the
relationships between the production and transport of biogenic
carbonate and terrigenous sediments and the morphological and
hydrodynamical characteristics of the basin.
GEOLOGICAL SETTING
The geology of North Sardinia and South Corsica, the
structure of which is due to the Hercynian orogeny, is dominated
by the Corse-Sardinia batholiths (upper Carboniferous-Permian),
outcropping for a total length of 400 km between the two islands
and made of different calco-alkaline granitic. The post Hercynian
formation crops out in Sardinia (Capo Testa) and in the southern
Corsica (from Bonifacio to Santa Amanza Bay) as Miocene
limestone. Quaternary deposits are limited to coastal areas and
alluvial plains, several submerged shorelines are also reported.
In the sector study the depth does not exceed 90 m. The
seabed morphology of the northern shelf sector is characterized
by a tabular relief at ca. 55 m depth with incisions forming
channels which converge toward the center of the basin. In the
eastern sector morphological heights of Lavezzi archipelago
delimit small basins. Bedforms, like E-W oriented comet marks
and ripple marks, have been reported in the whole area
(PLUQUET, 2006).
METHODS
New SSS data recorded lines were used to report bedforms
_________________________
Sedimentological map of Bonifacio Strait inner shelf
SANDRO DE MURO (*), TIZIANA BATZELLA (*), GIOVANNI DE FALCO (**) & MARCO PORTA (*)
(*)Dipartimento di Scienze della Terra, Università degli Studi di Cagliari,
marinegeology@unica.it
(**) Consiglio Nazionale delle Ricerche
The research work was conducted within the framework of the research
project Interreg IIIA GERER
752
(DE MURO, 2003; PUSCEDDU, 2008). New sub-bottom recorded
lines were used to find out sediment deposits (Fig. 1).
Furthermore sub-bottom recorded lines were used to determine
acoustic facies (BARTOLE &DE MURO, 2009). A total of 84 new
sediment samples were collected by Van Veen grab, from 5 to 77
m depth. Grain size distribution was determined by sieving at 1f
intervals using Udden - Wentworth scale. Carbonate percentage
was determined by gasometrical measurements.
The mineralogical composition of samples was classified by
distinguishing lithoclasts, quartz, feldspars, micas and other
minerals using a binocular microscope. The taxonomical
classification was performed on 55 samples which showed a
weight percent > 0.5 mm exceeding 70% by categorizing in the
following groups: Red Algae, Bryozoans, Mollusks, Cnidarians,
Arthropods, Echinoderms, Foraminifers, Polychaeta–Serpulida
and indeterminate grains. In order to verify the sediment
distribution, a tri-dimensional hydrodynamic model was applied to
reproduce the wind and tide, generating water currents in the area.
RESULTS
The sedimentological map was drawn using the classification
into six sedimentary facies, realized using the multivariate
statistical technique, which distinguishes sample groups on the
basis of different sediment characteristics (texture, mineralogy,
taxonomical groups) (DE FALCO et alii, 2008).
Bonifacio Mouth shelf carbonate sediments consist almost
entirely of whole and fragmented skeletal material characterized
by their coarseness, more or less irrespective of water depth, with
a mud content generally < 5%. A total of six sedimentary facies
and four subfacies were recognized:
a) Coastal biogenic gravelly sand. It was subdivided in 2
subfacies related to intermattes and the upper limit of Posidonia
oceanica (L.) meadows, recognized as a major ecosystem
producing biogenic carbonate sediments in the infralittoral.
Bioclastic sediments are formed from heterozoan skeletal
assemblages (bryozoans, calcareous red algae, bivalve mollusk)
with significant presence of undetermined grains.
b) Reworked detritic sands. This facies was subdivided in two
subfacies based on the percentage of terrigenous sediments: i)
“Mixed coarse sand” characterized by reworked skeletal
fragments often with glauconite infilled, where terrigenous
materials are quartz and grain aggregates formed of several
siliciclastic sediments cemented (encrusted) probably by
filamentous algae; ii) “Reworked medium-fine bioclastic sands”

Fig.1 – Sedimentological map of Bonifacio Strait inner shelf.
where carbonate organisms are represented by bivalves,
bryozoans, sponge spicules, echinoderm fragments and spines,
planktonic and benthic foraminifera.
c) Maërl beds. This facies represents the major ecosystem
carbonate producer in the circalitoral zone. Sediments consist
almost entirely of coralline algae (mostly Lithothamnion
corallioides) occurring primarily as branches and nodules. Other
common coarse grains are whole and fragmented mollusks,
bryozoans. In the fine sandy fraction echinoderms and benthic
foraminifera are the main components.
d) Mixed gravelly sands. The sediments contain ca. 40% of
terrigenous elements (feldspar, biotite and quarz) mostly relict
gravels. The bioclastics fraction is made up of bryozoans and
bivalves.
e) Coralligenous. Coralligène concretions were found in two
points at ca. 15 and 30 m depth. However the points registered as
rocks are probably parts of this biogenic association.
f) Mixed shoreface facies, formed by silicilastic and
carbonate sediments derived from Posidonia meadows.
REFERENCES
BARTOLE R. & DE MURO S. (2009) - Features and bedforms of
the last eustatic cycle in the La Maddalena Archipelago
(North Sardinia, Italy) from high-resolution acoustic data.
753
Medimond International Proceeding, ISBN: 978-88-7587-
554-1, 79-84.
DE FALCO G., BAROLI M., CUCCO A. & SIMEONE S. (2008) -
Intrabasinal conditions promoting the development of a
biogenic carbonate sedimentary facies associated with the
seagrass Posidonia oceanica. Continental Shelf Research 28
(6), 797-812.
DE MURO S., BARTOLE R., RAMELLA R. & DONDA F. (2003) –
Acoustic facies and morphologies of the holocene deposists
within the la Maddalena Archipelago (Bocche di Bonifacio –
NW Sardinia, Italy) - Atti del convegno Geosed 2003,
Alghero, Italia, 119- 123.
PLUQUET F. (2006) - Évolution récente et sédimentation des
plates-formes continentales de la Corse. PhD Thesis
Université de Corse, 300 pp.
PUSCEDDU N. (2009) – Caratterizzazione sedimentologica della
piattaforma interna dell’Arcipelago di La Maddalena. Studio
e modellizzazione di tre spiagge campione. PhD Thesis in
Earth Sciences. Università di Cagliari, 186 pp..
SESSIONE 24

SESSIONE 24
Key words: Coastal cartography, sedimentology, Site of
Community Importance (SCI), south-west Sardinia.
INTRODUCTION
The paper presents the results obtained from the morhologicsedimentological
study of Chia beaches located in the Site of
Community Importance (SCI) ITB 042230 “Porto Campana”.
The research work was conducted within the framework of the
research project Life+ Nature & Biodiversity – Providune
(LIFE07NAT/IT/000519) (DE MURO et alii, 2009) using survey
methodological standards with high resolution, defined and tested
during the European Project Interreg IIIA GERER “Gestion
intègrèe de l’environnement à haute risque d’èrosion” (DE
MURO &DE FALCO, 2010).
The aim was to describe coastal morphologies, define
sedimentological and hydrodynamic characteristics and processes
of the area and produce submerged and dry beach cartography in
1:5,000 scale.
AREA LOCATION
The ITB042230 “Porto Campana” SCI is located in Domus
de Maria municipality, SW Sardinia - Sulcis area (Fig. 1). The
study object is the beaches at Chia, which are included in the SCI.
Their continuity is interrupted by two low rocky headlands which
divide it into three areas from NE to SW called Sa Colonia,
Campana and Su Giudeu. The geological setting is characterized
by a Precambrian and Palaeozoic basement formed by
metamorphic rocks (ortogneiss of Monte Filau and micaceous
shales of Monte Settiballas) and granitoid lithotypes of Monti sa
Guardia Manna and Capo Spartivento.
Moreover crops of “Bithia Formation” (Precambian?-Lower
_________________________
Sedimentary processes, morphodynamics and sedimentological map
of “Porto Campana” SCI beaches (Domus De Maria - SW Sardinia)
SANDRO DE MURO (*), CLAUDIO KALB (*), ANGELO IBBA (*), FABRIZIO FERRARO (*) & CONCETTA FERRARA (*)
(*) Dipartimento di Scienze della Terra, Università di Cagliari,
demuros@unica.it, ckalb@unica.it
The research work was conducted within the framework of the research
project Life+ Nature & Biodiversity – Providune (LIFE07NAT/IT/000519).
754
Cambrian), formed by phyllites, metasandstones, marbles and
basic metavolcanic rocks are observed.
On the Palaeozoic basement, Quaternary deposits lie, which
are formed from Holocenic and recent beach sands, ancient and
recent alluvial deposits related to the main rivers and colluvial
deposits on the slope floors.
The surface beyond the backshore, called “Su Planu
Spartivento” is characterized by colluvial-alluvial deposits made
up of sandy matrix clastic sediments, while the alluvial plains of
“Rio di Chia” and“Sa Tanca ‘e sa Tuerra” are composed of
alluvial sandy-gravelly deposits. In the area two ponds are also
present (Su Stangioni de su Sali and Stagno di Chia) connected
with the alluvial plains.
Fig. 1 – Map Index.
RESEARCH METHODS
The survey was conducted by field measurements referred to
a geodetic net based on the IGM95 ETRF2000 n.239901 point,
located in Monte Filau (DE MURO et alii, 2009). The dry beach
was surveyed with a DGPS system, obtaining the points with xyz
coordinates on 1 Hz frequency. For the submerged beach, a
system of interfaced Reson Navisound 215 echosounder/
Omnistar 8300HP DGPS through Reson PDS2000 navigation
software was used, installed on the Novamarine RH580 ship of
the “Osservatorio Coste E Ambiente Naturale Sottomarino”
(OCEANS) of the Earth Science Department – Cagliari
University. The surveys were obtained together on submerged
and dry beach on a 50m side grid. In “post-processing mode”
data were processed and filtered to realize a studied area DTM.
Then a sedimentological survey, along prefixed land-sea transects
was carried out. During this survey the following samples were
collected: 67 samples from the submerged beach (using 5 liters
van veen grab), 42 samples from dry beach and shoreline and 74
samples from the dune area.

Granulometric analysis was made following the ASTM
International standard metodology, with sieves spaced on ¼ F
between 2000 μm and 63 μm (Udden-Wentworth scale, 1922).
The grainsize parameters of FOLK &WARD (1957): Meansize
(Mz), sorting (s I,), skewness (SkI) and kurtosis (KG) were
obtained for every sample. The compositional analysis was made
with Dietrich-Fruhling calcimeter to estimate the total carbonate
percentage. This method was linked to a semi-quantitative
evaluation of different component percentages (quartz, feldspars,
micas, heavy minerale, lithoclasts and bioclasts) observed under
binocular microscope using a visual comparison chart.
Collected data have allowed the realization of wave and
hydrodinamic models with Delft3D software, WAVE and FLOW
modules. The models were also based on meteomarine data
recorded in the area and calibrate with observations and
measurements in situ (KALB, 2008).
RESULTS
Meansize Mz values from Sa Colonia to Su Giudeu (from NE
to SW) allowed the identification of a general trend in size
reduction. This trend is underlined mostly on shoreline with
values from 0.92F in Sa Colonia to 1.94F in Su Giudeu.
From a compositional point of view the results show that dune
samples consist of quartz (75-80%), bioclastic-carbonate
component (7-10%) and a low percentage of femic minerals.
Dry beach samples are very similar to dune ones with tails of
coarse sediments, prevalently formed by clastics materials.
Submerged beach samples can be grouped into two types: the
first made up entirely of angular quartz clasts (90%) and small
amounts of bioclasts and femic minerals (8-10%); the second is
prevalently quartz-feldspathic sediment (75-80%) with major
amounts of bioclasts (15-20%) and femic minerals (5%). The
Fig. 2 – Hydrodynamic scheme following Scirocco wind with 10 m/s
intensity.
755
coarse tails are formed of bioclastic, quartz and lithic
metamorphic clasts.
The hydrodynamic models demonstrate that Libeccio (225°)
and Scirocco (135°) control the exchange processes and set the
bar and trough area (surfzone). These events produce longshore
SW-NE currents and several circulation cells (Fig. 2) which
shape a double system of bars and trough, with a surfzone
extension over 300 metres. (Fig. 3).
Fig. 3 – Arrangement of the surfzone following Scirocco wind with 10
m/s intensity.
The various thematic maps obtained (bathimetry, refraction,
bottom current distribution, texture, facies distribution, surfzone
dynamic) show the main mechanisms of sediment flows.
The results underline clearly the main mechanisms of control
and behavior of sedimentary fluxes between dune-drybeachshoreface.
REFERENCES
DE MURO S., KALB C., FERRARO F., IBBA A. & FERRARA C.
(2009) – Studi sedimentologici e dinamica marino-costiera -
SIC “PORTO CAMPANA” (ITB042230). Report ACTION
A.2 Progetto Life+ Nature & Biodiversity Providune
(LIFE07NAT/IT/000519), 1-53.
DE MURO S. & DE FALCO G. (2010) – Dati e manuale scientificotecnico
per lo studio e la gestione delle spiagge della
Sardegna e della Corsica. Volume atti conclusivi Progetto
Interreg. IIIA GERER “Gestione ambientale integrata in
località ad elevato rischio di erosione” – University press –
Scienze del Mare, CUEC.
KALB C. (2008) – I sedimenti superficiali della piattaforma
interna del Golfo di Cagliari. Relazioni tra moto ondoso,
correnti indotte e processi di sedimentazione su sistemi di
spiaggia campione. Tesi di Dottorato in Scienze della Terra –
Università degli Studi di Cagliari, Italy, 295 pp.
SESSIONE 24

SESSIONE 24
Sedimentological map of the seafloor between Porto Pozzo Bay and
Capo Ferro - NE Sardinia
Key words: Cartography, facies association, North-East
Sardinia, Posidonia oceanica, sedimentology.
INTRODUCTION AND GENERAL INFORMATION
The Sedimentological map of the seafloor between Porto
Pozzo Bay and Capo Ferro - NE Sardinia is presented. The
purpose of this study is to improve the knowledge of actual
sedimentary distribution in 1:25,000 scale.
The research in based on acoustic data (Edgetech DF-1000
Side Scan Sonar – 70NM 2 ), seismic data (Datasonic Chirp Sub
Bottom Profiler – 200NM) and sedimentological data (Van Veen
grab – 170 samples).
The data were collected during: PALEOCLI.GE Campaign
(1999, 2000 and 2001), Palau 2004 Campaign, Bocche di
Bonifacio 2005 Campaign and GERER 2007 Campaign
organized by “Osservatorio Coste E Ambiente Naturale
Sottomarino” (O.C.E.A.N.S.). Previous research work (DE MURO
et alii, 2000, 2003; FANZUTTI &PIANI, 2003; PUSCEDDU, 2009;
Fig. 1 – Sedimentological data and Sub Bottom Profiler data position.
_________________________
(*) Dipartimento di Scienze della Terra, Università di Cagliari,
demuros@unica.it; marinegeology@unica.it
The research work was supported by the European project INTERREG IIIA
Italy-France “Islands” - "Gestion intègrèe de l’environnement à haute risque
d’èrosion" (GERER).
SANDRO DE MURO (*), NICOLA PUSCEDDU (*) & CLAUDIO KALB (*)
756
BARTOLE &DE MURO, 2009) has been made in the studied area
(Fig. 1 and Fig. 2).
Side Scan Sonar data were also used (Ministero
dell’Ambiente e della Tutela del Territorio - Servizio difesa del
mare, 2002).
Fig. 2 – Side Scan Sonar data position: PALEOCLI.GE 2000 Campaign and
MINISTERO DELL’AMBIENTE E DELLA TUTELA DEL TERRITORIO -SERVIZIO
DIFESA DEL MARE, (2002).
As cartographic bases we used the Carte Tecniche Regionali,
in 1:10,000 scale, (CTR-Regione Autonoma della Sardegna,
1998) and the Italian nautical maps (Istituto Idrografico Militare -
I.I.M.I., 1990).
The NE Sardinia geology is primary dominated by the Corse-
Sardinia batholiths (upper Carboniferous-Permian), which are
made of different calco-alkaline granitic outcrops. Also
secondary outcrops of metamorphic basement can be preserved in
Golfo delle Saline, Caprera Island and Capo Ferro.
Quaternary deposits are limited to coastal areas and alluvial
plains; several submerged shorelines are also reported.
METHODS
The grain size analysis was performed according to the
international standard method ASTM and classified by Nota and
Folk scale.
The mineralogical composition of samples (quartz, feldspars,
micas, other minerals, lithoclasts and bioclasts) were classified by
using comparison charts for the visual estimation of mineral
percentages with a binocular microscope.
Sedimentological data and geomorphological data were used

Fig. 3 – Sedimentological map of the seafloor between Porto Pozzo Bay and Capo Ferro - NE Sardinia.
to create a database for the statistical approach to classify the sea
bottom distribution in main 11 sedimentary facies.
RESULTS
All cartographic data, acoustic data, seismic data and
sedimentary data collected, have been revised, processed, georeferred
and digitized to create a sedimentological map 1:25,000
scale (Fig. 3).
The sedimentological map shows the surface distribution of
the actual and sub actual deposits (based on 11 facies groups) and
the distribution of mainly bedforms.
REFERENCES
BARTOLE R. & DE MURO S. (2009) - Features and bedforms of
the last eustatic cycle in the La Maddalena Archipelago
(North Sardinia, Italy) from high-resolution acoustic data. In:
A. Amoroso (Ed.) - 27th IAS Meeting of Sedimentologists .
Medimond International Proceeding, 79-84.
757
DE MURO S., FANZUTTI G. P. & CAMIN M. (2000) – Carta
geomorfologica terra-mare del settore compreso tra Punta
Don Diego e la Penisola di Culuccia (Sardegna Nord-
Orientale - Italia). – Scala 1:10.000.
DE MURO S., FANZUTTI G. P., CABRAS M. & PIANI R. (2003) -
Carta tessiturale dell’area marina compresa tra P.ta
Sardegna e Capo d’Orso – Sardegna settentrionale. Atti del
Convegno “Geosed 2003”, Alghero, Italia, 97-101.
FANZUTTI G. P. & PIANI R. (2003) - Pattern distribution of
bottom sediments in the SE area of Caprera Island
(Archipelago of La Maddalena, Northern Sardinia). Atti del
Convegno “Geosed 2003” Alghero, Italia, 171-172.
MINISTERO DELL’AMBIENTE E DELLA TUTELA DEL TERRITORIO –
SERVIZIO DIFESA DEL MARE (2002) – Mappatura delle
praterie di Posidonia oceanica lungo le coste della Sardegna
e delle piccole isole circostanti.
PUSCEDDU N. (2009) - Caratterizzazione sedimentologica della
piattaforma interna dell’Arcipelago di La Maddalena: studio
e modellizzazione di tre spiagge campione. PhD Thesis in
Earth Science, Cagliari University, 186.
SESSIONE 24

SESSIONE 24
Sediments and foraminiferal assemblages in Posidonia oceanica
seagrass: two cases in the Central Tyrrhenian Sea (Latium, Italy)
Key words: Foraminifera, grain size, Posidonia oceanica,
Tyrrhenian Sea.
INTRODUCTION
Phanerogam meadows play a significant role in temperate and
tropical coastal marine systems, mostly in the structuring of
habitats through the production of organic matter and oxygen.
Posidonia oceanica, a typical Mediterranean marine plant, often
has been claimed as a significant contributor to carbonate
production since it develops at quite shallow depths and greatly
contributes to bottom stabilization (JAMES, 1997).
Two areas of Latium (Central Tyrrhenian Sea) characterised
by Posidonia seagrass and by siliciclastic-carbonate mixed
sedimentation (TORTORA, 1989; BRANDANO &CIVITELLI, 2007)
were investigated. The first area is located along the Northern
Latium coast (near Santa Marinella), whereas the second area is
near the Ponza Island (Southern Latium). In order to characterise
the carbonate sediment production of these areas the sediment
composition of shallow-water samples and, particularly, the
foraminiferal assemblages were analysed and described.
MATERIALS AND METHODS
A total of 22 samples (13 from Santa Marinella: 7.5-13.5 m
water depth; 9 from Ponza Island: 15.8-34.5 m) were obtained by
scuba diving.
The sediments were studied using grain size and
compositional, chemical and micropaleontological analyses.
Samples were cleaned by washing. After wet sieving at 63 μm
_________________________
VIRGILIO FREZZA (*), ALESSIO BALDASSARRE (*), GIOVANNI GAGLIANONE (*),
GUILLEM MATEU-VICENS (**) & MARCO BRANDANO (*) (°)
(*) Dipartimento di Scienze della Terra, Università di Roma “La Sapienza”,
virgilio.frezza@uniroma1.it
(**) Departament de Ciències de la Terra, Universitat de les Illes Balears,
Spain.
(°) IGAG-CNR
Lavoro eseguito nell’ambito del progetto “Caratteri sedimentologici del
substrato delle praterie a Posidonia” (Ricerca di Ateneo Federato 2007 –
Resp. Dr. M. Brandano
758
grain size, analysis was carried out. The finer fraction was
analysed by a high resolution laser diffraction system, while the
coarser fraction by dry sieving. At least 300 grains from each
sample were separated and determined. One gram of sediment
was used to determine the carbonate content. A thin section
microfacies analysis was performed to gain more information on
the composition of the fine grained sediments.
Finally the foraminiferal assemblages were analysed. When
possible, at least 300 benthic foraminifera from each sample (>
63 μm size fraction) were counted and classified. Hierarchical
Cluster Analysis (HCA) was carried out using SPSS software
(version 13). Only foraminiferal species more abundant than 5%
in at least one sample were considered for the statistical analyses.
The α-Fisher index and the Percentage of Dominance (PD) were
also calculated.
RESULTS AND DISCUSSION
The sediments are prevalently sandy (74.6-98.8%), with
subordinately gravel (0.3-19.1%) and silt (0.3-9.8%); the clay is
very few (0-2.6%). Along the Latium coast, carbonate biota
assemblages are dominated by typical epiphytic foraminifera,
bivalves, echinoids, bryozoans and, subordinately, by red algae.
Near Ponza Island the most abundant components reported are
foraminifera and red algae, followed by molluscs (gastropods,
bivalves and very scarce scaphopods and pteropods), bryozoans,
serpulids and negligible amounts of crustacean (balanids,
decapods and ostracods), echinoids and hydrozoans. The
carbonate content analyses show values of 6.3-18.9% in the Santa
Marinella coast, whereas in the Pontine Archipelago it ranges
between 17.0 and 43.5%, confirming the mixed carbonatesiliciclastic
sedimentation in this area, as already reported in
previous works (BRANDANO &CIVITELLI, 2007).
Concerning the micropaleontological analyses, 145 benthic
foraminifera species belonging to 72 genera were classified.
Seventeen species show a relative abundance higher than 5% in at
least one sample, whereas only the frequency of Asterigerinata
mamilla, Conorbella hexacamerata, Lobatula lobatula, Rosalina
bradyi and Rosalina floridana is greater than 10%: these taxa are
typical of infralittoral zone with vegetated bottom (LANGER,
1993; SGARRELLA &MONCHARMONT ZEI, 1993). The α-Fisher
index shows relatively high values (8.4-23.9), whereas PD ranges

etween 10.3 and 31.4%, confirming on the whole assemblages
well diversified.
The resulting dendrogram of Q-mode HCA (Ward method,
Euclidean distance) represents the grouping of samples according
to the relative abundance of benthic foraminiferal species. The
dendrogram singles out two main clusters A and B that can be
subdivided into subclusters: A1-A2 and B1-B2, respectively (Fig.
1).
Cluster A1 groups 5 samples of Santa Marinella (10-13.5 m
water depth). A. mamilla (24.2-31.4%) is the most frequent
species. R. bradyi (15.8-25.1%) and, subordinately, L. lobatula
(5.0-12.9%), Ammonia beccarii (2.5-6.3%), Astrononion
stelligerum (3.6-8.5%), and R. floridana (0-5.5%) are other
typical species of this assemblage.
Cluster A2 includes 4 samples of Santa Marinella (8-12 m). A.
mamilla (14.4-22.5%) and R. bradyi (16.6-22.1%) are the
Fig. 1 – Dendrogram of Q-mode HCA of the samples, based on the relative
abundance of species > 5%.
dominant species, in two samples each. L. lobatula (6.5-9.3%),
Quinqueloculina stelligera (1.6-8.2%), A. stelligerum (4.6-6.7%),
and A. beccarii (1.0-5.9%) are other important taxa.
Cluster B1 (9 samples of Ponza, 1 of Santa Marinella; 10-34.5
m) is dominated by L. lobatula (7.7 - 18.9%) and R. bradyi (10.3-
13.8%). R. floridana (5.6-10.7%), A. mamilla (1.3-9.3%),
Neoconorbina posidonicola (1.9 - 8.5%), Q. stelligera (2.5-
8.2%), Spirillina vivipara (0.7 - 7.7%), Nubecularia lucifuga (0.0
-7.4%), Elphidium pulvereum (0-6.1%), Discorbis sp. (0 - 5.8%),
Miliolinella subrotunda (1.9-5.8%), Tretomphalus concinnus (0-
5.7%) and Sigmoilinita costata (0.6-5.0%) are frequent.
Cluster B2 includes 3 samples collected in the shallowest
759
waters of Santa Marinella (7.5-9 m). L. lobatula (12.1-25.0%), R.
brady (17.6-24.2%) and C. hexacamerata (12.8-18.7%) are the
prevailing taxa. Also A. mamilla (6.2 - 11.2%) and Miliolinella
elongata (0-6.6%) show relevant percentages.
CONCLUSIONS
The sediments analysed are constituted principally by
foraminifera, molluscs, bryozoans and red algae. The carbonate
content shows the highest values in the Pontine Archipelago.
Foraminiferal assemblages are dominated by typical epiphytic
species. The statistical analysis allowed us to distinguish four
assemblages: three founded only near Santa Marinella (A1, A2
and B2), one comprising all samples from Ponza Island and only
one sample of Santa Marinella (B1). Clusters A are dominated by
an assemblage with A. mamilla and R. bradyi, whereas clusters B
are characterised by a L. lobatula and R. bradyi assemblage. The
difference among assemblages can be imputable to different
siliciclastic apports or to the fact that in Santa Marinella the
seagrass ends at 15 m, whereas around Ponza Island it develops
at greater depths. Future studies will also investigate to Ponza a
bathymetric range comparable to that of Santa Marinella (< 15
m).
REFERENCES
BRANDANO M. & CIVITELLI G. (2007) - Non-seagrass meadow
sedimentary facies of the Pontinian Islands, Tyrrhenian Sea:
A modern example of mixed carbonate-siliciclastic
sedimentation. Sed. Geol., 201, 286-301.
JAMES N.P. (1997) - The cool-water carbonate depositional
realm. In: N.P. James and J.A.D. Clarke (Eds.) - Cool-Water
carbonates. SEPM Spec. Publ., 56, 1-20.
LANGER M. (1993) - Epiphytic foraminifera. Mar. Micropal., 20,
235-265.
SGARRELLA F. & MONCHARMONT ZEI M. (1993) - Benthic
foraminifera of the Gulf of Naple (Italy): systematics and
autoecology. Boll. Soc. Pal. It., 32, 145-264.
TORTORA P. (1989) - La sedimentazione olocenica nella
piattaforma continentale interna tra il Monte Argentario e la
foce del Fiume Mignone (Tirreno Centrale). Giornale Geol.,
51, 93-117.
SESSIONE 24

SESSIONE 24
Tectonic control on the sedimentary architecture of Early Mesozoic
mixed siliciclastic-carbonate Pseudoverrucano successions
(southern Tuscany, Italy)
Key words: Pseudoverrucano units, Tuscan series, alluvial
deposition coastal lagoons.
The mixed siliciclastic-carbonate successions of Early
Mesozoic age exposed in the Pseudoverrucano tectonic units,
along the coast of southern Tuscany (Montebrandoli and Punta
delle Rocchette, Early Liassic) and in the Monti dell'Uccellina
(Porticciolo di Cala di Forno and Salto del Cervo, Late Triassic)
are characterized by fossil assemblages suggesting a close
relationship with the coeval, mainly carbonate successions of the
“Tuscan Series” while the depositional features are completely
different.
The composition of the mixed facies are similar, characterized
by: (i) recurring fining-upward sequences with well rounded but
poorly selected white quartz-conglomerates, (ii) coarse quartz
sand grading to lagoonal lime-muds, or (iii) thin intercalations or
isolated quartz pebbles enclosed together with shell debris, within
open marine although shallow carbonates.
The depositional environments correspond to alluvial-fan
complexes on narrow coastal plains merging with sandy beaches
and lagoonal to shallow marine settings where the carbonate
micritic deposition prevailed. This sedimentary style suggests that
unsorted quartz debris was transported from an adjacent uplifted
source area by gravity currents through very narrow coastal
plains, and flowing into coastal lagoons or directly into the open
sea, mixed coarse, land derived debris with open marine
carbonate muds.
The peculiar vertical evolution of the Pseudoverrucano facies
suggests that the episodic input of siliciclastic materials was
connected with storm events most probably triggered by tectonic
pulses since no evidences of eustatic or climatic constrain on the
sedimentation is apparent.
The depositional features and fossil content of the mixed
siliciclastic-carbonate Pseudoverrucano successions argues for a
coastal sedimentation on narrow shelves delimited by active,
fault-bounded highs, representing the landward extension of the
_________________________
(*) Dipartimento di Scienze della Terra, Università di Siena,
gandin@unisi.it.
Lavoro eseguito con il contributo finanziario dell’Università di Siena (PAR
ANNA GANDIN (*)
760
epicontinental pelagic basins that from late Triassic in a regime of
continental rifting, developed on the European shelf.

Key words: Bonifacio basin, corals, mixed carbonate-siliciclastic
deposits
Admixed rhodalgal-chlorozoan skeletal carbonates and ruditic
to sandy siliciclastic units were deposited in the Bonifacio basin
directely above the Variscan granites. The succession records the
mainly Burdigalian stratigraphic and environmental evolution of
the Bonifacio Basin during Corsica–Sardinia block rotation
(Chattian to Tortonian). The Miocene sediments of the Bonifacio
basin are divided in two formations (FERRANDINI et alii, 2002;
2003): the Cala di Labra Formation (Burdigalian) and the
Bonifacio Formation (upper Burdigalian/lower Langhian)
(BRANDANO et alii, 2009). The first marine Miocene sediments
of Bonifacio is represented by Cala di Labra Formation where a
highly diversified coral framework crops out.
These corals directly lying disconformably on the Variscan
granitic basement and mantle the granitic boulders and blocks as
well as the deeply eroded granitic substrate. Three different reef
geometries can be distinguished within the Cala di Labra
framework based on their depositional attitude in relation with
the substrate and the internal fabric of the framework: (1) a lens
shape framework with a flat-topped surface developed in the
largest cavities between blocks and on the blocks itself; (2) coral
rubbles associated with granitic cobbles and pebbles; (3) coral
carpets that laterally interfingered with bioclastic sandstone.
The dominant framebuilders are poritids (Porites sp.) and
faviids (Tarbellastrea sp., Thegioastrea burdigalensis, Favites,
Thegioastrea sp, Favia sp.) and subordinated acroporids
(Astreopora sp). The dominant growth form are massive to
hemispheric with domal and globous form, platy forms are
subordinates.
The reefal textures are mainly represented by bindstone and
framestone with a bioclastic wackestone to packstone matrix
made up by larger benthic foraminifera, red algae nodules and
debris. Other components are articulated red algae fragments,
bivalves and oysters, echinoids fragments, rotaliids, textularids,
barnacles and bryozoan fragments. Small planctonic foraminifera
_________________________
Burdigalian coral facies of Eastern Bonifacio basin
(southern Corsica)
LAURA TOMASSETTI (*), MARCO BRANDANO (*) & FRANCESCA BOSELLINI (**)
(*) Dipartimento di Scienze della Terra, Università di Roma “La Sapienza”,
marco.brandano@uniroma1.it
(**) Dipartimento di Scienze della Terra, Università di Modena e Reggio
Emilia
761
are present. Bioerosion traces and dissolution phenomena are
common especially on the red algae thalli.
The total thickness does not exceed 4 metres and southward
these coral deposits passes into hybrid calcarenites with quartz
and feldspar, red algae, oysters and echinoid fragments. Toward
NE the coral unit pinches out on the hercynian granites.
The Cala di Labra coral framework could be interpreted as a
fringing reef because of its attachment to the continent,
nevertheless this framework does not present the typical
ecological zonation of the fringing reef deposits. These coral
form a thin veneer of seaward thickening carbonate deposits over
granite substrate with no distinct ecological zonation and for this
reason it can be classified as a coral carpet or a biostrome (sensu
RIEGL & PILLER, 1999). This work focuses on the origin and the
inter-relationship between the siliciclastic and coral-rich
carbonate deposits of the Bonifacio Basin.
REFERENCES
FERRANDINI J., GATTACECCA J., FERRANDINI M., DEINO A&
JANINI M.C. (2003) - Chronostratigraphy and
paleomagnetism of Oligo-Miocene deposits of Corsica:
geodynamic implications for the liguro-Provenc_al basin
spreading. Bull. Soc. Geol. France, 174, 357-371.
FERRANDINI M., GALLONI F., BABINOT J.F. & MARGEREI J.P.
(2002) - La plate-foeme carbonatèe burdigalienne de
Bonifacio (Corse du Sud) : microfaunes et
palèoenvironnements. Rev. Micropal., 45,1,57-68.
BRANDANO M, JADOUL F, LANFRANCHI A, TOMASSETTI L, BERRA
F, FERRANDINI M&FERRANDINI J (2009) – Stratigraphic
architeture of mixed carbonate-siliciclastic system in the
Bonifacio Basin (Early-Middle Miocene, South Corsica).
Field Trip Guide (FT13), 299-313 pp., 27th IAS International
Meeting of Sedimentology, Alghero, Sardegna, Italy, 24-25
Settembre 2009.
RIEGL B. & PILLER W.E. (1999) - Frameworks revisited: Reefs
and coral carpets of the northern Red Sea. Coral Reefs, 18,
305-316.
SESSIONE 24

SESSIONE 24
Mixed litho-bioclastic carbonates in Apulia (southern Italy)
Key words: Apulia foreland, mixed litho-bioclastic carbonates,
Plio-Pleistocene, southern Italy.
During Pliocene and early Pleistocene times, Apulia was
part of the subsiding outer foreland-basin of the southern
Apennines (southern Italy). Before subsidence, the Apulian
Foreland, was already a large carbonate landmass with a
complex horst and graben structure, that became an archipelago
during relative sea-level rise induced by subsequent subsidence.
Around islands, shallow-marine carbonate sedimentation
took place. Sediment supply was two fold: carbonate lithoclasts
derived from exposed highlands and bioclasts produced in the
MARCELLO TROPEANO (*), LUISA SABATO (*) & LUIGI SPALLUTO (*)
762
newly flooded areas.
Mixing of both types of carbonate particles (lithoclasts and
bioclasts) characterizes individual lithosomes and derived from
coexistence of skeletal factories in “terrigenous” fed settings
(rather than to mechanical mixing) (Fig.1). Alternation of
mainly lithoclastic with mainly bioclastic lithosomes was also
observed and this temporal variability of facies is interpreted as
induced by high-frequency relative sea-level changes
(reciprocal sedimentation). Finally, in a regional view, the
spatial organization, internal architecture and distribution of
heterogeneities of the different lithosomes, along with their
skeletal composition, sedimentary structures and bedding
patterns, resulted from the interaction between basement
physiography, type and loci of carbonate production, bottom
currents and changes in accommodation (TROPEANO &
Fig. 1 – Distribution of depositional zones around islands characterized by mixed litho(extraclastic)-bioclastic carbonate systems (after TROPEANO et alii, 2009).
_________________________
(*) Dipartimento di Geologia e Geofisica, Università "Aldo Moro" di Bari,
Italy. m.tropeano@geo.uniba.it

SABATO, 2000; POMAR &TROPEANO, 2001; MATEU-VICENS et
alii, 2008).
REFERENCES
MATEU-VICENS G., POMAR L. & TROPEANO M. (2008) -
Architectural complexity of a carbonate transgressive
systems tract induced by basement physiography.
Sedimentology, 55, 1815-1848.
POMAR L. & TROPEANO M. (2001) - The Calcarenite di
Gravina Formation in Matera (Southern Italy): new
insights for coarse-grained, large-scale, crossbedded
bodies encased in offshore deposits. AAPG Bull., 85, 661-
689.
TROPEANO M. & SABATO L. (2000) - Response of Plio-
Pleistocene mixed bioclastic-lithoclastic temperate-water
carbonate systems to forced regressions: the Calcarenite di
Gravina Formation, Puglia SE Italy. In: D. Hunt and R.L.
Gawthorpe (Eds.) - Sedimentary Responses to Forced
Regressions. Geological Society, London, Spec. Publ., 172,
217-243.
TROPEANO M., SABATO L., MATEU-VICENS G. & POMAR L.
(2009) - Bioclastic/lithoclastic mixed carbonate successions
in Apulia (Plio-Pleistocene, southern Italy). Book of
Abstracts, 27 th meeting IAS 2009, Alghero, Italy, 705.
763
SESSIONE 24

SESSIONE 24
Key words: Apulia shelves, carbonate and mixed deposits,
present-day sedimentation, southern Italy.
Unlike the “classical” chlorozoan carbonate factories mainly
flourishing in tropical-subtropical oligotrophic settings,
temperate-type carbonate factories frequently develop in areas
with a significant siliciclastic input. They normally bear biotic
assemblages in which molluscs, bryozoans, encrusting red algae,
barnacles and benthonic foraminifers appear in different
proportion (foramol sensu lato: molechfor/rhodalgal/bryomol
assemblages). Among the biotic constituents, filter feeder
organisms and mesotrophic/tendentially eutrophic conditionadapted
assemblages can be significant. Relationships among the
foramol-type production areas and the surrounding terrigenous
domains may be largely variable. In the related depositional
settings, mixing of foramol skeletal debris and terrigenous
components results in variously characterized deposits in relation
with several geo-morphological and oceanographic parameters.
The knowledge of modern foramol-type carbonate factories
and of their compatibility with a significant siliciclastic input in
the depositional setting appears fundamental in interpreting
ancient mixed systems. The study of the present-day Apulia shelf
(southern Italy) may contribute significantly to bring light on this
topic.
Apulia is the easternmost region of Italy; it is characterized by
three large Meso-Cenozoic limestone landmasses flanked by sea.
Respectively, moving from N to S, these three areas are: the
Gargano Promontory, the Murge Plateau, and the Salento
Peninsula. The related Apulia Shelf sectors are characterised by
low-energy waves, a microtidal regime, and superficial
thermohaline currents. Going from the Gargano Promontory to
the Salento Peninsula, composition of present-day shallowmarine
sediments passes from mixed to carbonate (foramol-type
sensu lato) in origin. Latitude, climate and sea-water temperature
led to attribute the carbonate production to temperate-type
factories (TROPEANO &SPALLUTO, 2006).
_________________________
Present-day sedimentation on Apulia shelf (southern Italy):
mixed vs. carbonate environments
MARCELLO TROPEANO (*), LUIGI SPALLUTO (*), GABRIELE CARANNANTE (**), MASSIMO MORETTI (*),
LUISA SABATO (*) & LUCIA SIMONE (**)
(*) Dipartimento di Geologia e Geofisica, Università di Bari "Aldo Moro",
m.tropeano@geo.uniba.it.
(**) Dipartimento di Scienze della Terra, Università di Napoli “Federico
II”.
764
Siliciclastic input from the exposed region is low to the shelf,
since a few rivers run in Apulia and, moreover, they bring a small
amount of terrigenous material to the mouths; in spite of this, an
alongshore muddy-prism, fed by superficial currents and coming
from north, contours the Gargano Promontory and occupies
middle-shelf settings up to northern Murge. However, according
to water circulation, coasts and nearshore zones of Gargano are
mainly characterised by rocky bottoms, colonized by an
encrusting coralligenous community, and, moving toward south
(in the Manfredonia Gulf), rocky coasts pass to depositional
paralic settings, that are characterised by hybrid sands, whose
carbonate components are fed by mollusks and nearshore
rhodalgal mounds. More southward, Murge and Salento Adriatic
shelf sectors are characterised by rocky coasts that alternate with
depositional ones; these latter are characterized by
molechfor/rhodalgal sand-grained facies. Both types of coasts
pass seaward to a rhodalgal nearshore zone characterised by
Posidonia meadows. A relict rhodalgal belt is observed along the
shelf edge.
The shelf which contours the Salento Peninsula is
characterised by cliffed coasts toward the Otranto Strait and by
an alternation of promontories and beaches toward the Ionian
Sea. A rhodalgal nearshore rocky belt develops, while seaward,
where the shelf becomes flat, a rhodalgal (relict) - bryomol
(modern) belt occurs.
REFERENCES
TROPEANO M. & SPALLUTO L. (2006). Present-day temperatetype
carbonate sedimentation on Apulia shelves (southern
Italy). Geoacta, 5, 129-142.