Explanatory notes to the digital geological map of the Rax ... - KATER

KATER II (KArst waTER research program)
Geology of the Rax-Schneeberg-Region
Explanatory notes to the
digital geological map
of the Rax-Schneeberg-Region
Gerhard W. Mandl
Vienna, December 2006
Geologische Bundesanstalt Wien
im Rahmen d. Teilrechtsfähigkeit gem § 18 Abs.5 FOG, BGBl Nr. 341/1981 i.d.g.F.
Neulinggasse 38, A - 1030 Wien Tel.: 712 56 74 / 0 www.geologie.ac.at

KATER II (Karst waTER research program)
Geology of the Rax-Schneeberg-Region
Explanatory notes to the
digital geological map
of the Rax-Schneeberg-Region
Gerhard W. Mandl
Vienna, Dezember 2006
Geological Survey of Austria

KATER II Geology of the Rax-Schneeberg-region
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CONTENT
Abstract ............................................................................................................................... 3
Introduction ............................................................................................................................... 5
1 STRATIGRAPHY ............................................................................................................... 7
1.1 Noric-Tyrolic Nappe System ............................................................................................ 7
Greywacke Zone (95) – (91) .............................................................................. 7
Werfen Imbricates Zone (90) – (85) ..................................................................... 7
1.2 Meliaticum (84) ................................................................................................................. 8
1.3 Juvavic Nappe System ....................................................................................................... 8
Permian – Lower Triassic (83) – (79).................................................................... 8
Middle Triassic to Lower Carnian (78) – (61) ...................................................... 8
Upper Carnian to Rhaetian (60) – (52)................................................................. 11
1.4 Tyrolic Nappe System (Göller Nappe) ............................................................................... 14
Triassic (51) – (44) ................................................................................................ 14
Jurassic (43) – (34)................................................................................................ 14
1.5 Gosau Group .................................................................................................................... 15
Cretaceous to Paleocene (33) – (24) ................................................................................ 15
1.6 Inneralpine Molasse, Vienna Basin ................................................................................... 16
Palaeogene – Neogene (22) – (20) ...................................................................... 16
1.7 Quaternary.......................................................................................................................... 16
Pleistocene (20) - (13)........................................................................................... 16
Late Pleistocene to Holocene (12) - (1) ................................................................ 17
2 TECTONIC ......................................................................................................................... 18
2.1 Principles of NCA structural evolution ................................................................................ 18
2.2 Structural frame of the Rax/Schneeberg aquifer system ................................................... 21
Schneeberg Nappe................................................................................................ 21
Mürzalpen Nappe ................................................................................................ 23
Göller Nappe ......................................................................................................... 23
Werfen Imbricates Zone ....................................................................................... 24
Acknowledgements ......................................................................................................................... 25
References ............................................................................................................................... 25
Attachments: Geological map and cross-sections 1:25.000
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KATER II Geology of the Rax-Schneeberg-region
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Abstract
Within the karst water system the geological setting is responsible for the collection, filtering,
storage and distribution of karst water on its way down from the surface through permeable
rocks to the spring. The geological setting provides boundary conditions to apply general
models on specific aquifers as well as to interpret measurements of water parameters (e.g.
discharge curves, water chemistry, isotopes and others).
Due to the complex geological genesis of the project area the geological mapping had to be
accompanied by additional investigations in lithostratigraphy, biostratigraphy, micropalaentology,
carbonate facies (lateral transitions) and tectonics.
Mesozoic carbonates are the dominant rock type within the Northern Calcareous Alps,
whereas siliciclastic sediments are restricted to a few stratigraphic levels and act as layers of
reduced permeability. The following sedimentary succession forms the Schneeberg/Rax area
(the mentioned thicknesses may vary considerable due to tectonic cutting):
The sedimentary succession starts with Permian continental red beds (Prebichl-Fm.; 0-150
meters), transgressing discordant over Early Paleozoic rocks of the Greywacke Zone. A
marine clay-evaporite association is locally developed and may affect the water quality with
sulfates. The Early Triassic is characterized by deposition of some 100 meters of marine
shallow shelf siliciclastics (Werfen-Fm.). They represent the main layer of low permeability.
In Middle Triassic times carbonate sedimentation became prevailing with well bedded
(Gutenstein-Formation; 150 m) and massive limestones and dolomites (Steinalm-Formation;
80-100 m). During the Middle Anisian a rapid deepening of the marin environment was
associated with blockfaulting. This has generated a pronounced relief of the sea-floor, which
is the reason for the subsequent development of different sedimentary facies: shallow-water
carbonate platforms (Wetterstein-Formation and lateral slope sediments) coexist with basins
of different shape, water depth and circulation. Four types of basinal sediments occur in the
investigated area: black, thin bedded allodapic limestones (Grafensteig-Fm., 300 m), nodular
limestones with chert (Reifling-Fm.; 20-30 m), light grey to reddish, nodular, bedded or
massive limestones (Hallstatt Limestones; 40 m) and bedded to massive multicolored
allodapic limestones (up to 250 m).
In general, the Wetterstein platforms show a rapid progradation of reef and reef breccias
over the adjacent basinal sediments. The thick platform carbonates (up to 1000 m) build the
main aquifer in the Hochschwab and Schneeberg/Rax region. The primary porosity of these
bioclastic sediments has been lost due to early diagenetic cementation. During diagenesis
also parts of the Wetterstein limestone as well as parts of the adjacent basinal limestones
became transformed into dolomite. Extended bodies of dolomitic rocks within the aquifer are
responsible for lower percolation rates and a more regular discharge of some springs.
The prevailing carbonate producing organisms within the platform lagoon were calcareous
green algae (dasycladaceans). The knowledge about their distinct evolution during Triassic
Times has been proved recently by correlation with conodont zonation and can be used now
as a powerfull tool for biostratigraphic dating. Tectonic offset along fault zones within
monotonous platform carbonates could be recognized and sometimes quantified in this way.
In the early Upper Triassic (Carnian) the platforms emerged and the basins received
sandstones and shales (10-30 m). In the Late Carnian a sea-level rise has initiated the
development of the Norian carbonate platform (up to 1000m) characterized by Dachstein
limestone (reef and lagoonal facies) and Hauptdolomite (intertidal facies).
Most of the following younger rocks are of minor significance for the lithological composition
of the karst aquifer but relevant for revealing the structural history.
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The platform growth has been terminated in the latest Triassic. During Jurassic times marly
and cherty limestones covered the subsiding seafloor. Locally they are replaced by
condensed red limestones. The deposition of radiolarite indicates the stage of greatest water
depth. Due to plate tectonic movements a first tectonic event affected the southem part of the
NCA during Upper Jurassic. Sedimentation became controlled by tectonic activity, which
finally culminated in the Cretaceous nappe stacking.
After a period of subaerial erosion, Upper Cretaceous to Eocene clastics of the Gosau-Group
have been deposited on the nappe stack in a subsiding environment. Sedimentation has
started with terrestric to shallow marine clastics, later on a strong subsidence has led to
turbiditic deep slope conditions. After the collision of the Austroalpin Units with the
accretionary wedge of the Rhenodanubian Flysch Zone the NCA became a dry land.
The plateau character of several mountain areas in the NCA is the result of erosion during
Oligocene. The NCA became a lowland, covered by fluvial deposits, which were delivered
from the uplifting Central Alps in the south.
Compressional deformation at the beginning of Miocene has caused large strike slip fault
systems. These brittle tectonic structures are crucial for the development of water
permeability in the NCA sedimentary rocks and for the karstification of the uplifting carbonate
plateaus.
The youngest, Pleistozän to Holocene sediments are only of minor influence on the karstic
springs, due to the location of springs within the carbonatic bedrocks.
The knowledge of the complex interaction of sedimentation, nappe tectonics and faulting
provides a useful tool for understanding the hydrogeology of the karstic springs of the Vienna
Water Supply. It offers also a database for decision finding in a management system for a
sustainable drinking water supply.
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Introduction
The inhabitants (about 1.65 million people) of the Austrian capital city Vienna become
supplied with high quality drinking water from karstic springs. Up to 200.000 cbm per day are
flowing via each of the two pipelines 150 resp. 180 kilometers from the Northern Calcareous
Alps towards Vienna. The protected area around the springs comprises about 32.000 hectars
of karstified mountain ranges, a sensible ecosystem with complex interactions between
rocks, water, soil, vegetation, climate and human landuse.
Water supply agencies permanently have to balance between saving water quality and
quantity, economic requirements and monitoring of environmental pollution. To maintain at
least a minimum water supply in case of local pollution it is necessary to have a better
understandig of the catchment areas of individual springs and of the potential subterranean
water paths.
About 1990 the government of Vienna has initiated a multidisciplinary “Karst Research
Project”. Within this frame the Austrian Geological Survey has started a detailed geological
mapping of the catchment area of the Second Vienna Water Supply System. The final report
2002 offers a modern geological map of about 520 sq.km area of the Hochschwab mountain
range in form of a digital database.
In the meantime the Karst Research Project of the Government of Vienna has initiated a
transnational and interdisciplinary project on European level, due to its fundamental
significance for municipal water supply systems. The aim of KATER (KArst waTER research
program in the frame of EU Interreg II c) was to form the basic tools for a decision finding
system in the field of regional policy, water supply and environment protection – basics like
definition of metadata, cartographic standards and GIS (Geographic Information Systems) -
tools.
The following project KATER II (in the frame of EU Interreg III b CADSES) has the aim of
developing a GIS-based decision system to estimate or quantify the influences of land use
activities on drinking water ressources in karstified areas.
As a part of this project the geology of the catchment areas of the First Vienna Water Supply
System has to be investigated in a similar way as in the former Hochschwab project. Data
integration of available modern maps and additional geological mapping with a focus on the
Schneeberg area was done by the Austrian Geological Survey, starting in december 2003.
The final report presents the results in form of a geological map 1:25.000, four geological
cross sections and explanatory notes. The geological map is also available as a digital
database (ArcGis9/GeoDatabase).
Within the karst water system the geological setting is responsible for the collection, filtering,
storage and distribution of karst water on its way down from the surface through the
permeable rock to the spring. The petrography of rocks and the geometry of their structural
features has influence on the water paths and the position of springs and the chemistry of
rocks may also affect water quality.
The large karstified areas of the Northern Calcareous Alps are composed mainly of thick
sequences of shallow water carbonates of seemingly monotonous lithology. Only a very
general overall fiew could be obtained from older geological maps. No detailed knowledge
existed about structures like internal thrusts or fault systems and about the geometry of
internal lithological aquitards/aquicludes.
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KATER II Geology of the Rax-Schneeberg-region
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A main task of remapping such areas was therefore a detailed subdivision of the carbonate
rocks. The geological mapping had to be accompanied by additional investigations in
lithostratigraphy, biostratigraphy, micropalaeontology, carbonate facies (lateral transitions)
and tectonics.
The geological setting provides boundary conditions to apply general models on specific
aquifers as well as to interpret measurements of water parameters (e.g. discharge curves,
water chemistry, isotopes and others).
Parts of the catchment area of the First Vienna Water Supply have been mapped in such a
detailed way, they are available in printed form (scale 1:50.000) since several years:
ÖK-sheet 75/Puchberg am Schneeberg (1991), ÖK-sheet 105/Neunkirchen (1992),
ÖK-sheet 104/Mürzzuschlag (2001).
The area of Kuhschneeeberg and its surrounding (ÖK-sheet 74/Hohenberg) has to be
mapped additionally to obtain a modern view on the overall catchment area.
All data have been integrated and partly actualized and refined to a digital data base,
comparable with a printed map at a scale of 1:25.000.
Fig.1
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KATER II Geology of the Rax-Schneeberg-region
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1 STRATIGRAPHY
The Northern Calcareous Alps (NCA) – as a prominent part of the Eastern Alps – extend for
about 500 kilometers from the Rhine valley in the west to Vienna in the east, forming a 20 to
50 kilometer wide mountain belt. In the western and middle part the highest peaks reach
altitudes of up to 3.000 meters and are locally glaciated, in the eastern part elevations are up
to 2.000 meters (Rax, Schneeberg). At their eastern end the NCA are bounded by the
Vienna Basin, which subsided during Neogene times. In the basement of the Vienna Basin,
however, the NCA continue into equivalent units of the Western Carpathians even if the
details are still in discussion.
The Grauwacken Zone, consisting mainly of Ordovician to Carboniferous Metasediments, is
the basement of the NCA. The transgressive sedimentary sequence of the NCA begins in the
Permian and extends locally into the Paleogene (Gosau Group). The Triassic carbonates are
the most prevailing rocks. They are forming extended karstified landscapes, the catchment
areas of several drinking water supply systems – the most importend one is the Vienna water
supply.
Due to the intense nappe tectonic during the Alpine orogenesis the originally succession of
sedimentary rocks has been dissected into several nappes with different stratigraphic
content. Therefore the legend of the map as well as the explanatory notes are grouping the
formations according to the main tectonic units and then according to their sedimentary age,
beginning with the oldest one.
Overviews as well as detailed data and further literature to this topic are given by BÖHM
1992, FAUPL & WAGREICH 1996, FLÜGEL 1981, LEIN 1987, LOBITZER, MANDL,
MAZZULLO & MELLO 1990, MANDL 2000, MANDL & ONDREJICKOVA 1993, NEUBAUER
et al. 1994, SCHLAGINTWEIT & EBLI 1999, TOLLMANN 1976, 1985, 1986, WAGREICH &
FAUPL 1994, ZANKL 1971.
A schematic representation of the Triassic sedimentary sequences is shown in Figs. 2 and 3.
1.1 Noric-Tyrolic Nappe System
Greywacke Zone (95) – (91)
The palaeozoic metasediments of the Greywacke Zone are separated into three nappes, two
of them can be found in the project area:
# the Silbersberg Nappe contains remnants of a crystalline basement („Vöstenhof-
Crystalline”) and transgreding siliciclastics of the Silbersberg-Group (95).
# the Noric Nappe is built by phyllits and greenschists (94), Ordovician volcanic rocks of
the “Blasseneck Porphyroid” (93), Silurian sandy grey shale “Radschiefer” (92) with
lydites and Devonian carbonate rocks (91).
Werfen Imbricates Zone (90) – (85)
The sedimentary sequence of the NCA starts in the Permian with continental red beds,
conglomerates, sandstones and shales of the Prebichl Formation (90, 89), transgressing
onto Lower Palaeozoic rocks of the Greywacke Zone. The Permian age is assumes due to
local intercalations of acid tuffs and pebbles of quartz porphyry, which are widespread in the
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European Permian. Locally occurs a body of Quartz porphyry (88), tectonically embedded
in Werfen shales.
The Lower Triassic is characterized by uniform shallow shelf siliciclastics of the Werfen
Formation (87), containing limestone beds (86) in its uppermost part with a poor fauna
including Scythian ammonoids.
Tectonized Anisian dolomites form elongated bodies of Rauwacke (85) within and on top of
the siliciclastics.
1.2 Meliaticum (84)
Along one of the main thrust planes we find two Klippen of sedimentary rocks of a deep
water origin, unknown elsewhere in the NKA, but well known as Meliaticum in the Western
Carpathians. These rocks represent the transition from the Triassic Hallstatt carbonatic
depositional realm into oceanic conditions with radiolarites. We have hints on the existence
of such an oceanic realm only in form of olistolites of Ladinian red radiolarite in the Middle
Jurassic silicious shales of Florianikogel Formation (84) - see MANDL & ONDREJICKOVA
1991, 1993, KOZUR & MOSTLER 1992.
1.3 Juvavic Nappe System
Within a distinct zone of tectonic disturbance several partly recrystallized carbonate rocks
occure, which have been assigned in older maps to the Carnian Opponitz Formation. No
fossils have been found until now; lithology and discordant position do not confirm this
opinion. Therefore these rocks are summarized here as carbonates of unknown
stratigraphic origin (83).
PERMIAN – LOWER TRIASSIC (83) – (79)
A marine facies of Permian sediments is the so called Haselgebirge (82), a sandstone-clayevaporite
association, containing gypsum and salt. This facies is frequent in the Juvavic
units, exposed for example in the Pfenningbach gypsum open pit mine east of village
Puchberg. The Upper Permian age is proved paleontologically by pollen/spores at several
localities in the NCA and confirmed by sulfur isotopes.
The Lower Triassic is represented again by siliciclastics of Werfen Formation (81, 80),
accompanied by Anisian Rauwacke (79) - see also above.
MIDDLE TRIASSIC TO LOWER CARNIAN (78) – (61)
Beginning with the Middle Triassic carbonate sedimentation became dominant.
The dark Gutenstein Limestone (76) and Dolomite (77) is present in most of the NCA
nappes. A local variety is a multicolored Flaser Limestone (78).
The Gutenstein carbonates can be laterally replaced in the upper part by light dasycladacean
bearing carbonates, the Steinalm Limestone/Dolomite (75, 74).
During the Middle Anisian a rapid deepening and contemporary block faulting of the so
called Reifling Event has caused a sea floor relief, responsible for the following differentiation
into shallow carbonate platforms (Wetterstein Formation and lateral slope sediments) and
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basinal areas.The basins can be distinguished into the wide spread Reifling basins, local
intraplattform basins of Grafensteig type and the Hallstatt deeper shelf, the latter one was
bordering the open Tethys.
Rocks of transitional nature between Middle Triassic platforms and basins are relatively rare
in the NCA due to structural complexities. Basinal facies often are tectonically isolated from
formerly contiguous platform deposits. In general within the project area we know four
different types of Anisian to Lower Carnian carbonatic slope to basinal sediments, the
Reifling Limestone, the Hallstatt Limestone and multicolored allodapic limestones and the
dark allodapic Grafensteig Limestone.
The Reifling Limestone (73) is the characteristic basinal facies in the Bajuvaric and Tyrolic
nappes, locally also occuring in the Juvavic nappes. It consists of grey well bedded nodular
limestone with thin yellowish to greenish clay intercalations of partial tuffitic origin. A silica
content often is concentrated in chert-nodules or -layers. Microfacies shows (pel-) micrites
with abundant radiolarians and „filaments” (thin shells of planctonic bivalves) and conodonts,
the macrofauna consists of ammonites, molluscs (Daonella) and local brachiopods.
The Hallstatt Limestone (72) comprises a lot of different lithologies, mostly of multicolored
micritic limestones with abundant pelagic fauna like conodonts and ammonites. Hallstatt
Limestones are restricted almost to the uppermost respectively southernmost tectonic units
of the Juvavic Nappe System, representing the sediment of areas of low deposition.
Sometimes a secundary dolomitization has transformed the Hallstatt limestones and
allodapic slope limestones into multicolored Dolomites (71).
Along the Wetterstein platform margins locally multicolored allodapic limestones (70)
became deposited, mixtures of reddish hemipelagic carbonat ooze and finegrained
carbonate debris of platform origin.
The Grafensteig Limestone (68) is characterized by darkgrey to black well bedded
limestones, mainly with even bedding planes, more oder less abundant chert-nodules or -
layers and - as a main feature - with intercalated allodapic beds of platform origin. It is
overlain in the northern Schneebergarea by grossoolite-breccia facies of an upper slope
environment. The Grafensteig facies represents a restricted intraplatform-basin with only
minor connection to open marine conditions. Pelagic faunal elements like conodonts seem to
be restricted to sporadic beds and are in general poor. The Grafensteig Limestone comprises
a maximal time span from Middle Anisian to Lowermost Carnian in the basin interior. At the
basin-margins it ends earlier according to the prograding Wetterstein platform. Greenish
layers of very fine grained material without carbonate content are interpreted as volcanic
tuffite (69).
Wetterstein reef and reef debris facies (67)
The most intensely studied part of the Wetterstein Limestone is by far the reefal facies.
These builtups are composed of diverse biotic assemblages of calcisponges, corals and
hydrozoans, tubiphytes, bryozoans, codiacean and solenoporacean algae, brachiopods,
molluscs and rather rare foraminifers. Rock textures of reefal deposits generally are
wackestones and packstones. Boundstones resulting mainly from syndepositional marine
cementation are also very common. It seems that a biogenic reef framework in the sense of
a wave-breaking structure did not exist in the Wetterstein reefs of the eastern NCA.
Practically all reef-organisms are of small dimensions of several centimeters only. Coralbuildups
of large dimensions are missing as well as other potential wave-breaking
organisms. It seems that a rigid framework could have been constructed by a combination of
pervasive submarine early diagenetic cementation and various encrusting organisms. The
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fact of immediate interfingering of the „reef” with lagoonal birdseye limestones is considered
as a prove for platform-edge reefs and not an upper slope situation. Typical assemblages of
a deeper water slope (ammonites, radiolarians, silicisponges) are missing. Such biota
occures only in very rare small lenses of Hallstatt-type within the reef of Heukuppe (summit
of Rax-plateau).
A conspicuous feature of platform-edge facies in the Wetterstein Limestone is the
development of coarse breccias. The term „Grossoolite” refers to thick, laminated,
isopachous coatings of radiaxial-fibrous calcite cement and calcite-replacive dolomite around
lithoclasts and skeletal particles. Although initially interpreted as being of organic origin
(“Evinospongia”), these coatings are now regarded as inorganic or microbial initiated
cements. The component clasts are commonly angular and often poorly sorted, ranging in
size from a few centimeters to several decimeters in diameter. They are mainly composed of
reefal lithologies. In places the grossoolitic breccias are the only remaining evidence of the
former existence of in-situ shelf-margin reefs. Syndepositional tectonism, oversteepening of
the platform margin, slope instability, or a combination of these processes must have been
causative factors in the formation of such widespread breccia deposits.
Wetterstein lagoonal facies (66)
Rocks of this facies are generally massive to thick bedded, locally bioturbated limestones
with a diverse biota of various dasycladacean, solenoporacean and codiacean algae,
molluscs (mainly gastropods), echinoderms, rare framebuilding organisms, brachiopods,
foraminifers and ostracodes. Textures vary from wackestones to grainstones. Patch reefs
inside the lagoon are very rare. The immediate transitional area behind the reef - the nearreef
lagoon - is often characterized by boundstones or birdseye-limestones with mixed biota
consisting of reef debris and the dasycladacean Teutloporella herculea, which one is the
dominant algal species in the Rax-Schneeberg area. In the uppermost part of the lagoon
additionally Poikiloporella duplicata occurs and indicates an Early Carinan age.
Wetterstein dolomite (65)
Parts of the Wetterstein limestone have been affected by a secondary dolomitization. In the
Rax and Schneeberg area a local dolomitization took place mainly within the reef and reef
breccia facies. These dolomites form bodies of irregular size, which cannot be assigned to
distinct stratigraphic levels. Prediction of the extent of subsurface dolomite bodies can be
given only schematic – see cross sections.
In the Schneealpe the dolomitization has affected the Wetterstein platform nearly complete.
Also adjacent slope sediments of Grafensteig limestone have been partly dolomitized.
Northern Alpine Raibl-Group ( 64) - (61)
The Wetterstein platforms in general show a platform progradation over the adjacent basinal
sediments until the Earliest Carnian ("Cordevolian"). Then carbonate production decreased
rapidly due to a sealevel lowstand. The platforms emerged, the remainig basins received
siliciclastics from the European hinterland in form of marine black shales, the Reingraben
shale (64). The shales are interbedded with dark cherty limestones (63), dolomites (61)
and dark biodetrital limestone (62), derived from small surviving reef mounds at the basin
margins.
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UPPER CARNIAN TO RHAETIAN (60) - (52)
As sealevel started rising up again in the Upper Carnian, rather slowly in the beginning,
carbonate production increased, locally filling a relief in the drowning platforms with the
dasycladacean bearing lagoonal Waxeneck Limestone (60). The relief (several 10th up to
about 100 meters) may have been caused by erosion during the lowstand time and /or by
tectonic movements.
A transgressive pulse just below the Carnian/Norian boundary caused an onlap of pelagic
limestones over the shallow water carbonates and initiated the rapid growth of the Norian
carbonate platform. Due to local differences in platform growth conditions we can distinguish
two different developments:
In the central part of the NCA (Hochkönig, Tennengebirge, Dachstein area etc.) the pelagic
onlap represents only a short time interval and became covered by the prograding Dachstein
carbonate platform – in these areas the Upper Triassic reefs approximately are situated
above the Middle Triassic ones.
Another situation characterizes the eastern sector of the NCA. There the Uppermost Carnian
pelagic transgression continues until the Upper Norian and has been termed Mürztal Type of
Hallstatt facies. Dachstein reefs are only known from the Upper Norian and these ones are
situated above the former platform interior, several kilometers behind the former Wetterstein
reef front. This "backstepped" reefs show transitions into the partly restricted basinal facies of
the Aflenz Limestone (59), a bedded black limestone with chert layers or nodules.
In contrary the "Southern Marginal Reefs" of central NCA are connected by the allodapic
Gosausee Limestone to the Pötschen Limestone (58), a bedded grey limestone with chert,
representing the basinal realm of Hallstatt deep shelf.
The Hallstatt-Group (57) - (54) shows a great variability of multicolored limestones often
with rapidly changing sedimentary features due to the mobile basement:
The Hallstatt Limestone at Nasswald (57) consists of massive to bedded grey pelagic
limestones with a Norian fauna.
Hallstatt Limestone of Mürztal facies (55)
The grey, pink and reddish, more or less massive limestones represent sediments on a
„pelagic plateau“ above the drowned Waxeneck limestone and Wetterstein platform. The
uppermost part, consisting of well bedded dark limestone (56), is shown separately on the
map.
Hallstatt Limestone of Salzberg facies (54)
At Losenheim there occurs massive white limestone (“Massiger Hellkalk”) und well bedded
red limestone (“Hangend Rotkalk”). It is comparable to the Salzberg facies of the classical
Hallstatt area in the Salzkammergut, representing the reduced sedimentation above local
uplifts due to diapirism of Permian evaporites.
Zlambach Formation (53, 52)
In the Triassic basinal realms Zlambach marls (53) and bedded black limestones (53)
have been deposited. Along the basin margins they onlap and interfinger with the the
Dachstein platform slope sediments.
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Fig. 2:

KATER II Geology of the Rax-Schneeberg-region
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Fig. 3

KATER II Geology of the Rax-Schneeberg-region
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1.4 Tyrolic Nappe System (Göller Nappe)
TRIASSIC ROCKS (51) – (44)
In the southernmost parts of the Göller Nappe only a few occurences of Wetterstein
dolomite (51) are preserved due to tectonic dissection. In this area they are mainly of
lagoonal origin.
According to the Early Carnian regression the marin to brackish Lunz Sandstone (50) has
filled up the basins between the Wetterstein platforms. In areas outside the project area they
locally contain coal seams. A subsequent following transgression has lead to partly
hypersalinar conditions, causing the deposition of limestones and dolomites with local
evaporites (gypsum) - the Opponitz Formation (49) .
Far behind the Dachstein reef barrier a large lagoonal environment extended all over the
NCA with the intertidal Hauptdolomit (48) in distal parts, “Plattenkalk” (47) as a transitional
facies and thick bedded Dachstein limestone (46) in the subtidal lagoon.
In the Uppermost Triassic ("Rhaetian") once again increasing terrigenious influx has reduced
the carbonate platforms. The Hauptdolomit area and parts of the Dachstein lagoon became
covered by the marly Kössen Formation (45) borderd by Rhaetian reefs. A local recurrence
of carbonatic sedimentation has lead to the deposition of an “Upper” Dachstein limestone
(44).
JURASSIC ROCKS (43) – (34)
At the beginning of Jurassic the Austroalpine shelf drowned completely, basinal conditions
prevailed until the Early Cretaceous with the only exception of local Plassen carbonate
platforms (Late Jurassic - Earliest Cretaceous) in southern parts of the NCA, especially in the
realm of Juvavic nappes.
Parts of the Hettangian are often missing at the base of the Jurassic limestones. The reason
- subaereal exposure or submarine non-deposition - is still in discussion. Neptunian sills and
dykes filled with red or grey Liassic limestones are known, cutting down several meters into
the Norian shallow water carbonates.
Irregular drowning and synsedimentary faulting has caused a complex seafloor topography
with reddish/grey crinoidal limestones (Hierlatz Limestone, 43) and red ammonoid
limestones (Adnet Limestone, 42) mainly above subsided former shallow carbonate
platforms. Grey marly/cherty limestones of Allgäu Formation (40) have been deposited in
the deeper troughs between.
Very thin condensed sequences of these and other Jurassic red limestones are summarized
as Jurassic condensed limestones in general (41). Jurassic red limestones are bioclastic
wackestones, mainly made of nannoplankton (Schizosphaerella, coccoliths) and very
finegrained biodetritic material. After globigerinids had evolved in the Middle Jurassic, they
also became a major component of these sediments along with the tiny shells ("filaments") of
the probably planctonic juvenile forms of the bivalve Bositra. The macrofauna mainly consists
of crinoids and in some places brachiopods and ammonites. Ferromanganese hardgrounds
and nodules are frequent.
Less condensed sequences are composed of grey limestones with chert (39), with
limestone breccias (38) and red limestones with chert nodules or intercalated layers of
thin bedded red radiolarite (37).
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The greatest water depth has been reached in Oxfordian, characterized by the Ruhpolding
radiolarite (36). Contemporaneous breccias, olistolites and large sliding blocks occure as a
consequence of the Juvavic gravitational nappe movements. This first pulse of alpine
orogeny has caused a new seafloor topography during Late Jurassic. Pelagic Oberalm
Limestone (35) became deposited in the remaining basins whereas above local uplifted
areas new platform growth produced the Plassen and Tressenstein Limestone (34). This
carbonate production has persisted into the early Cretaceous.
In the more northern tectonic units increasing terrigenous input and synorogenic clastic
deposits represent the Lower Cretaceous, caused by the Alpine orogenetic movements and
crustal shortening within the Austroalpine basement. This tectonic process caused an uplift
of southern parts of the NCA, overthrusting of NCA nappes and metamorphism in the
Austroalpine crystalline nappes below.
1.5 Gosau Group
CRETACEOUS TO PALEOCENE ROCKS (33) – (24)
During the Cretaceous orogeny the sedimentary succession of the Northern Calcareous Alps
and their Palaeozoic substratum (Greywacke Zone) had been sheared off from their
crystalline basement. North-verging folds, thrusts and nappe structures developed. The
unconformable deposition of the Gosau-Group began after this tectonic event, sealing folds
and thrust structures. A second phase of compressive deformation affected the NCA latest at
the end of Eocene, terminating the sedimentation.
Today only relatively small remnants of the formerly widespread Late Cretaceous to
Palaeogene sedimentary cover of the NCA are still preserved. As a consequence of the
complex deformation history the paleogeographic relationships between individual Gosau
occurences are often obscured.
Despite the very early knowledge of rich macrofaunas (SUMMESBERGER, 1985) in the
sediments of the Gosau-Group the biostratigraphic framework for modern investigation is
mainly based on planktonic foraminifera and calcareous nannoplankton. A comprehensive
description of stratigraphy and facies was given by WAGREICH & FAUPL (1994), FAUPL &
WAGREICH (1996), also including paleogeographic maps and geodynamic/palaeotectonic
conclusions.
After a periode of non deposition or erosion sedimentation has started diachronously from
the Late Turonian onwards.
A succession of breccias, sandstone and rauhwacke (33) south of Schneealpe is assigned
with questionmarks to the Gosau-Group (no fossil proof).
The basal Kreuzgraben Formation (32) consists of reddish breccias, conglomerates and
subordinate sandstones and pelitic sediments of an alluvial fan environment. Locally it can
be replaced be marine red marls with conglomerate layers (31) of Early Campanian age.
The Grünbach Formation (30) is a clastic succession with several coal seams, worked at
the former coal mines of Grünbach.
Occurrences of biodetritic limestone with rudists (29) point to local carbonate production
during Campanian times.
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Widespread is the finegrained, carbonatclastic Orbitoid sandstone (28). It is superimposed
by and lateral interfingering with marly sandstones of the Piesting Formation (27), bearing
inoceramid shells and few ammonoids of Late Campanian to Maastrichtian age.
Mainly south of the NCA area a carbonatic shallow-marine shelf facies was developed,
serving as a source of bio- and lithoclasts during Maastrichtian to Paleocene. Only a few
examples of this bioherms are preserved within the southermost parts of NCA. The project
area contains the type locallity of the Kambühel Limestone (26), a red and white colored
bioclastic limestone with coralls, corallinacean alges, high diverse dasycladacean alges and
several more reef building and reef inhabiting organisms of Early Paleocene age (Danian).
A turbiditic sandstone (25) marks a renewed subsidence from the shelf to greater depth
during the earliest Paleocene. It contains debris from the Kambühel bioherms and is
superimposed by coarse grained to blocky olistostromatic clastics (24), which are also
dominated by clasts of Kambühel limestone. These are the youngest rocks which are
affected by the last, toward south directed thrusting in southern parts of the NCA.
1.6 Inneralpine Molasse, Vienna Basin
PALAEOGENE – NEOGENE (23) – (21)
At the NCA karstified plateau mountains fluviatile gravel or individual “Augenstein” pebbles
(23) of metamorphic rocks can be found, often together with red clay/soil (22). These are
multiple redeposited remnants of weathering products and fluviatil sediments of Paleogene
(?Oligocene) age, which had covered the NCA before the final uplift. The metamorphic
debris came from erosional uncovered metamorphic areas in the earlier uplifted Central Alps.
The Early Pliocene fluviatile Rohrbach conglomerate (21) belongs to the final stage of the
sedimentary filling of the Vienna basin.
1.7 Quaternary
PLEISTOCENE (20) - (13)
The oldest preserved quaternary sediment is a conglomerate (20) south of Klostertaler
Gscheid which is superimposed by significant cemented slope breccias (19) from the
Mindel/Riss interglacial time. The only remnant of Riss-Glacial is a ground moraine (18)
west of Altenberg. It contains components of the former mentioned slope breccia.
Another slope breccias /old slope debris (17) is only partly cemented and must be of
younger origin. Due to superposition and morphology it is clearly separated from the older
one and from the recent slope debris.
A thick sequence of fluviatle gravel (16), deposited in front of the prograding Würm glacier,
is preserved at Klostertal Gscheid and superimposed by Würm-Glacial moraine (14) and
terminal moraine circles (15).
Along the Schwarza valley as well as in the Puchberg area fluviatile gravel of Würm-Glacial
is forming terraces up to 20 meters above the recent valley floor – “Niederterrasse” (13).
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LATE PLEISTOCENE TO HOLOCENE (12) - (1)
Within the terminal moraine circle at Tränkwiese (north of Schneeberg) a completely flat area
is supposed to represent late Pleistocene lake deposits (12). Also of late Pleistocene ages
are two fluviatile fans (11) at Klostertaler Gscheid, which belong to an older drainage
system. The recent one has changed its direction and is crosscutting the fans.
Late Pleistocene to recent mass movements have created typical features like tension
cracks (10), landslide scars (9), creeping soil/debris (8) and blocky debris (7) of rock
fall.
Recent deposits are slope debris and debris fans (6) at the foot of steep mountain slopes,
fluviatile fans (5) from tributary valleys, swamp/moor deposits (4) and recent fluviatile
gravel (2) and erosional features (3).
Anthropogene deposits (1) are mainly caused by former mining activities (Iron ores).
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2 TEKTONIK
2.1 Principles of NCA structural evolution
The sequence of Mesozoic sediments of the NCA has lost its former crustal basement during
Alpidic Orogeny. During Upper Jurassic to Tertiary times several events of folding,
gravitational gliding, thrusting and final faulting have created a complex pile of nappes which
rests in the north with overthrust contact on the Rhenodanubian Flysch Zone and in the
south with a tectonically disturbed transgressiv contact on the Greywacke Zone.
The following nappe scheme of Northern Calcareous Alps can be given today:
The northern (=frontal) part of the NCA (outside of the project area) is built by the Bajuvaric
nappes, which one show narrow synclines and anticlines. They dip down toward the south
below the overthrusted Tyrolic nappe system. Due to their widespread rigide dolomitic
lithology the Tyrolic nappes exhibit internal thrusting and faulting and only minor folding. The
southernmost nappe is the Göller Nappe with a stratigraphic succession from Triassic
shallow water carbonates to Jurassic red limestones, marls and radiolarite.
The Juvavic Nappe System represent the uppermost tectonic element, overlying Mesozoic
rocks (Tyrolic Göller Nappe) in the north and the Greywacke Zone and its transgressiv
Permoscythian cover (Werfen Imbricates Zone) in the south. It can be subdivided into a few
large units (up to tens of kilometers), the Mürzalpen Nappe, Schneeberg Nappe, Hohe Wand
Nappe and several smaller ones (hundreds of meters to about a kilometer), forming Klippen
below or outliers above the larger ones.
The contact between NCA and Greywacke Zone was a matter of long lasting controversial
discussions: on the one hand there is a transgressive contact of Permo-Skythian clastics
over Lower Palaeozoic rocks of the Greywacke Zone visible; on the other hand the Skythian
clastics (Werfen Fm.) are followed by Middle Triassic carbonates. Many authors have seen
here an undisturbed sedimentary sequence. Local missing members of the sequence have
been explained by only minor thrusting. Other authors claimed that this sedimentary contact
is only a virtual one. They postulated a major overthrust, separating the Permoscythian of a
Tyrolic nappe system from carbonates of the Juvavic Nappe System – see PLÖCHINGER
1996, TOLLMANN 1985. This question is crucial for prediction of the deep subsurface
structures, especially of the position of the aquifer/aquiclude boundary. New mapping of this
southern margin has revealed a clear evidence for the overthrust concept. The thrust plane is
marked by slices and small Klippen-like bodies of tectonized Middle to Upper Triassic rock
sequences of the Hallstatt realm and of the Meliata realm - see MANDL & ONDREJICKOVA
1993, KOZUR & MOSTLER 1992.
In this sense the Noric-Tyrolic Nappe System consists of the former Palaeozoic basement
(Greywacke Zone) and the relictic preserved transgressiv Permotriassic (Werfen Imbricates
Zone) of the Tyrolic Nappes. In the eastern NCA it has been left behind several kilometers in
the south during the nappe movements.
Today there is a common agreement that the NCA depositional realm during the
Permotriassic was a passive continental margin between Variscian (=Hercynian)
consolidated Pangäa and the Tethys ocean – see HAAS et al. 1995.
Beginning in the Jurassic the Austroalpine realm (including the NCA) became separated
from its European hinterland by the birth of the transtensional basin of the Penninic Ocean,
which was linked by large transform faults to the opening of the Northern Atlantic Ocean.
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KATER II Geology of the Rax-Schneeberg-region
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Fig. 4: Tectonic sketch of the south-eastern part of the NCA.
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KATER II Geology of the Rax-Schneeberg-region
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Contemporaneous compressional tectonics has affected the Tethyan Ocean and the
adjacent shelf of the Austroalpine realm, causing the first displacements of the Juvavic
Nappe System. The concept of Jurassic gravitational nappe movements, which was
developed in the central NCA, seems to be also useful in the eastern NCA - see
TOLLMANN 1987. The stratigraphic sequence of the Göller nappe ends with the Jurassic
Allgäu Formation and red limestones and chert and dips down below the Schneeberg Nappe,
also visible in the Hengst- and Ödenhof Window. Unfortunately transgressiv Upper Jurassic
sediments, sealing the Jurassic movements like in the Salzkammergut, or Lower Cretaceous
syntectonic clastics are not preserved. Therefore the Jurassic or Early Cretaceous age of the
oldest transversal movements cannot be proven directly.
Subduction processes at the southern margin of the Penninic Ocean have started during the
Early Cretaceous, accompanied by heating and crustal shortening within the Austroalpine
crystalline basement and by wide spread synorogenic clastics and thrust movements in its
sedimentary cover, forming the Bajuvaric, Tyrolic and Noric Nappe Systems - DECKER et al.
1987, FAUPL & WAGREICH 2000.
For details of metamorphic evolution of the Eastern Alps and controversial discussions see
FRANK 1987. Apart from slightly metamorphosed beds at the basal parts - mainly within the
siliciclastic Permoscythian rocks - it was assumed that most parts of the NCA do not exhibit
any metamorphic overprint - see KRALIK et al. 1987. Investigations of Conodont Color
Alteration Index during the last years have revealed a considerable thermal event in parts of
the Juvavic nappes, predating the oldest (presumed Late Jurassic) transversal movements -
GAWLICK et al. 1994, KOZUR & MOSTLER 1992 , MANDL 1996.
Upper Cretaceous clastic sediments of the Gosau-Group transgressed after a periode of
erosion over the NCA nappe stack. The sediments of the Gosau-Group show a facies
change in time from shallow water clastics to flysch-like deep water sediments, WAGREICH
& FAUPL 1994. The latter ones are also typical for the adjacent Penninic trough, where
beside other structural units (e.g. ophiolite-bearing metamorphic Bündnerschiefer-Group of
the Tauern-Window) the Rhenodanubian Flysch Zone originates from.
Ongoing subduction of the Penninic realm toward the south below the Austroalpine units led
to the closure of the Penninic Ocean. The sediments of the Rhenodanubian Flyschzone
became deformed, lost their oceanic basement (only preserved in form of some Klippen) and
became partly overthrusted by the nappes of the NCA, beginning in the late Eocene. This
tectonic event is responsible for reactivation of older thrusts within the NCA, causing an
incorporation of Gosau Group rocks into the nappe stack by local thrusting toward the north
as well as backthrusting toward the south.
The remaining sea between the alpine orogenic front and the European foreland during
Oligocene and Early Miocene has been the depositional site of the Molasse Zone, which
one collected the erosional debris of the uplifting Alps – see KUHLEMANN & KEMPF 2002.
The southernmost part of the Molasse Zone became also incorporated into the alpine
orogeny due to the youngest subduction pulses.
The uplift of the central part of the Eastern Alps during Miocene was accompanied by large
strike slip movements on its northern part (sinistral Salzach-Ennstal and Mur-Mürz fault
systems; responsible also for the genesis of the Vienna Basin and also affecting the NCA) -
see for example LINZER et al. 1995, DECKER et al. 1994.
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2.2 Structural frame of the Rax/Schneeberg aquifer system
The karstified plateau mountains of Rax and Schneeberg are forming the catchment areas of
several springs of the Vienna Water Supply, for example the Kaiserbrunn-, Hölltal, Fronbachand
Stixenstein spring.
The aquifer is mainly built by Middle to Early Upper Triassic carbonate rocks of shallow water
origin – the Gutenstein, Steinalm and Wetterstein limestones and dolomites. Limestones
from slope to basinal depositional sites – the Grafensteig limestones – are of some relevance
only in the northern Schneeberg area, see stratigraphic scheme Figs. 2 and 3.
SCHNEEBERG NAPPE
During the alpine tectonics this Wetterstein platform was detached from its basement and
from adjacent basinal carbonate rocks and became a tectonically isolated mass of rocks, the
Schneeberg Nappe.
The Lower Triassic Werfen Formation, which may act as an aquitard or aquiclude, was used
as a shear horizon during the nappe movements. Therefore only parts of it remained in the
stratigraphic succession of the Schneeberg Nappe, large parts got lost during thrusting. We
cannot expect it anymore as a continous layer below the carbonates.
The lateral boundaries of the Schneeberg Nappe can be drawn today without any doubt:
On the northern side the Triassic rocks of the Schneeberg Nappe are thrusted over Early to
Middle Jurassic basinal sediments of the Göller Nappe. The same situation is visible within
two tectonic windows, the Ödenhof- and the Hengst-Window.
On the western side the tectonic contact shows two different situations. In the northern part
the Schneeberg Nappe again superimposes Middle Jurassic basinal sediments of the Göller
Nappe. In the southern part Middle Triassic to Carnian rocks of the Schneealpe (Mürzalpen
Nappe) are dipping down toward east below the Schneeberg nappe.
On its southern side there is an overthrust contact to the Palaeozoic to Lower Triassic
shales and siliciclastics of the underlying Werfen Imbricates Zone. The tectonic nature of the
contact is proved by the intercalation of several slices of Middle to Upper Triassic rocks of
deep shelf and oceanic origin. An additional deformation has affected the southern margin of
Schneeberg nappe subsequent to the deposition of the Gosau-Group, resulting in recumbant
folds and backthrusting toward south.
On its eastern side the Schneeberg nappe is dipping down below transgressive Neogene
sediments of the Vienna basin, where it continues in the subsurface (proof by several oil
drillings).
21

KATER II Geology of the Rax-Schneeberg-region
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Fig. 5: Tectonic sketch Rax-Schneeberg.
Fig. 6: Schematic cross-section Rax-Schneeberg.
22

KATER II Geology of the Rax-Schneeberg-region
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INTERNAL THRUSTS
An east-west directed compression has caused a synkline west of Heukuppe, which contains
the tectonic outlier of Hohe Gupf. Folding and westward directed thrusting in the adjacent
Altenberg valley is also ascribed to this deformation act.
Much more prominent for the hydrogeology of the Schneeberg-Nappe is a west directed
internal thrust (Markgraben thrust) in the western Gahns plateau – see also cross section 4.
The southern margin of the Schneeberg-Nappe has been affected by backthrusting after the
deposition of the Upper Cretaceous to Palaeocene Gosau-Group. This Gahnsleiten
Imbricates contain slices of Wetterstein reef and slope deposits with transgressively
connected Gosau formations, as well as lenticular bodies of Wetterstein limestone and
Werfen shales. The main part of the Schneeberg-Nappe is following above, beginning with
the Anisian Gutenstein Formation.
FAULT SYSTEMS
The Krummbach fault system seems to be a strike slip fault (local flower structures in
Krummbach valley and at Brettschacher) combined with a vertical offset: the Schneeberg
side has been uplifted, exposing older rocks and the underlying Göller Nappe in tectonic
windows, while the Rax side exposes the youngest part of the Wetterstein Limestone near to
the Schwarza valley floor.
A younger fault system shows extensional character:
The Weichtal normal fault has caused a displacement of about 600 m between
Hochschneeberg (hangingwall) and Kuhschneeberg (footwall). The faults in the Großes
Höllental seem to be a direct continuation of the Weichtal fault, but they exhibit quite opposite
movements: the western block (Heukuppe-Klobenwand) has been relatively uplifted about
200 m compared with the eastern block (Preinerwand-Grünschacher).
The Breitensohl normal fault forms the western margin of the tectonic window of Hoher
Hengst, displaces the Krummbach fault some hundred meters and continues into the eastern
Gahns massive. The normal displacement east of Hengst is 800 m as a minimum and
degrees toward south to about 400 m.
The NNE-SSW directed fault system at Bodenwiese has squeezed up Lower Triassic Werfen
shales probably by strike slip movements.
MÜRZALPEN NAPPE
The northern margin of the Mürzalpen-Nappe is often affected by younger faults or covered
by tectonic outliers. Its eastern end is dipping down under the Schneeberg-Nappe and at its
southern margin it is thrusted over rocks of the Werfen Imbricates Zone.
The Mürzalpen-Nappe has only minor influence on the Rax-Schneeberg-aquifere, therefore it
is not treated here in detail.
GÖLLER NAPPE
The Göller-Nappe consists here mainly of Hauptdolomite, which is gradually replaced toward
the south by lagoonal Dachstein limestone. Sandy shales of the Carnian Raibl-Group act as
a shear horizon during internal thrusting.
The sedimentary succession continues into Jurassic red limestones and marly/cherty basinal
sediments of Allgäu Formation and locally into red radiolarite.
23

KATER II Geology of the Rax-Schneeberg-region
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Die Göller-Nappe dips down toward south under the Schneeberg-Nappe, forming a wide
west-east striking syncline. The southern flank of this syncline is visible in the Lahngraben-,
Hengst- and Ödenhof-windows. Here it is cut off by the Krummbach fault system. The
continuation of the Göller-Nappe in the south of these faults cannot be proven directly. It is
probable due to the occurrence of Wettersteindolomite in the surrounding of Hinternaßwald,
which one must be part of the Göller-Nappe in such a southern position.
The former mentioned syncline is dissected by the Weichtal normal fault into an eastern and
a western part. In the eastern part of the syncline the Jurassic Allgäu Formation and the
Werfen Formation of Schneeberg-Nappe are forming a thick aquiclude layer below the
carbonates of Hochschneeberg. In the western part of the syncline the Allgäu Formation is
gradually replaced by red limestones and radiolarite of minor thickness. Also the Werfen
formation may wedge out locally. Therefore no continuous aquiclude can be expected in the
subsurface of the western Kuhschneeberg and Fegenberg.
WERFEN IMBRICATES ZONE
As mentioned above the Permo-Triassic siliciclastic rocks of this zone exhibit a transgressive
contact to the Early Palaeozoic rocks of the Grauwacken Zone. The tectonic contact to the
Schneeberg-Nappe is proven by intercalated Juvavic slices and Meliata Klippen. Additional
internal thrusting is probable due to incorporated younger rauwacke and ?Permian
quartzporphyry. This zone is forming a thick aquiclude layer below the carbonates in the
southern part of the Schneeberg-Nappe.
24

KATER II Geology of the Rax-Schneeberg-region
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Acknowledgements
Early mapping activities in the area between Schneeberg and Naßwald have started in 1993
in the frame of Project WA 4a. Financial support was given in the frame of the
“Bund/Bundesländerkooperation for raw material research” by the government of Vienna /
MA 31 and by the Austrian ministry for science and research.
Additional mapping in 2004-05, compilation and actualisation of maps, construction of cross
sections, GIS – operating etc. have been supported in the frame of KATER II by the
government of Vienna and by the European Union program Interreg III C.
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