Messinian forced regressions in the Adana Basin: a near ... - Tübitak
Messinian forced regressions in the Adana Basin: a near ... - Tübitak
Messinian forced regressions in the Adana Basin: a near ... - Tübitak
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Turkish Journal of Earth Sciences<br />
http://journals.tubitak.gov.tr/earth/<br />
Research Article<br />
Turkish J Earth Sci<br />
(2013) 22:<br />
© TÜBİTAK<br />
doi:10.3906/yer-1208-3<br />
<strong>Mess<strong>in</strong>ian</strong> <strong>forced</strong> <strong>regressions</strong> <strong>in</strong> <strong>the</strong> <strong>Adana</strong> Bas<strong>in</strong>: a <strong>near</strong>-co<strong>in</strong>cidence of tectonic and<br />
eustatic forc<strong>in</strong>g<br />
Ayhan ILGAR 1, *, Wojciech NEMEC 2 , Aynur HAKYEMEZ 1 , Erhan KARAKUŞ 1<br />
1 Department of Geological Research, General Directorate of M<strong>in</strong>eral Research and Exploration (MTA), 06520 Ankara, Turkey<br />
2 Department of Earth Science, Faculty of Ma<strong>the</strong>matics and Natural Sciences, University of Bergen, 5007 Bergen, Norway<br />
Received: 10.08.2012 Accepted: 19.12.2012 Published Onl<strong>in</strong>e: 00.00.2013 Pr<strong>in</strong>ted: 00.00.2013<br />
Abstract: This sedimentological and sequence-stratigraphic study focuses on <strong>the</strong> late Miocene deposits <strong>in</strong> one of <strong>the</strong> largest peri-<br />
Mediterranean bas<strong>in</strong>s of sou<strong>the</strong>rn Turkey, <strong>the</strong> <strong>Adana</strong> Bas<strong>in</strong>, which formed as a Tauride foreland depression accumulat<strong>in</strong>g molasse<br />
deposits. The Tortonian–<strong>Mess<strong>in</strong>ian</strong> shallow-mar<strong>in</strong>e Handere Formation, previously <strong>in</strong>terpreted as a regressive succession, appears to<br />
have recorded several relative sea-level changes. The formation base recorded a <strong>forced</strong> regression attributed to <strong>the</strong> end-Serravalian (Tor-<br />
1) eustatic fall <strong>in</strong> sea level. The lower to middle part of <strong>the</strong> formation is transgressive, culm<strong>in</strong>at<strong>in</strong>g <strong>in</strong> offshore mudstones. The upper part<br />
is regressive and its 3 isolated conglomeratic members represent sharp-based Gilbert-type deltas with <strong>in</strong>cised fluvial valley-fill deposits,<br />
record<strong>in</strong>g a <strong>forced</strong> regression followed by mar<strong>in</strong>e reflood<strong>in</strong>g. The time of this regression is biostratigraphically constra<strong>in</strong>ed to ~7.8 to<br />
6.4 Ma B.P. on <strong>the</strong> basis of planktonic foram<strong>in</strong>ifera <strong>in</strong> delta bottomset deposits. The regression is attributed to <strong>the</strong> tectonic conversion<br />
of <strong>the</strong> <strong>Adana</strong> foreland shelf <strong>in</strong>to a piggyback bas<strong>in</strong>, as <strong>in</strong>dicated by seismic sections and compressional bas<strong>in</strong>-marg<strong>in</strong> deformation. The<br />
reflood<strong>in</strong>g of <strong>the</strong> bas<strong>in</strong> ~6.4 Ma B.P. is ascribed to a postthrust<strong>in</strong>g flexural subsidence of <strong>the</strong> foreland under <strong>in</strong>creased crustal load. The<br />
mar<strong>in</strong>e transgression brought an almost immediate evaporitic sedimentation, which suggests <strong>in</strong>vasion of hypersal<strong>in</strong>e Mediterranean<br />
water. The bas<strong>in</strong> was subsequently emerged and its gypsiferous deposits were extensively eroded due to a second <strong>Mess<strong>in</strong>ian</strong> <strong>forced</strong><br />
regression, attributed to <strong>the</strong> early evaporative drawdown <strong>in</strong> <strong>the</strong> Mediterranean Sea (~6 Ma B.P.). The postorogenic isostatic uplift of<br />
<strong>the</strong> Taurides had meanwhile elevated <strong>the</strong> bas<strong>in</strong> enough to prevent its reflood<strong>in</strong>g by <strong>the</strong> Zanclean regional transgression. Stratigraphic<br />
comparison with coeval peri-Mediterranean bas<strong>in</strong>s to <strong>the</strong> west demonstrates that <strong>in</strong>terbas<strong>in</strong>al correlations are difficult, and that a<br />
superficial l<strong>in</strong>k<strong>in</strong>g of comparable events may be quite mislead<strong>in</strong>g. The local tim<strong>in</strong>g of <strong>the</strong> late Miocene relative sea-level changes and <strong>the</strong><br />
landward extent of <strong>the</strong> Zanclean flood<strong>in</strong>g were apparently determ<strong>in</strong>ed by <strong>the</strong> comb<strong>in</strong>ation of eustasy, tectonics, bas<strong>in</strong> topography, and<br />
sediment supply, whereby <strong>the</strong> eustatic signal was modulated and often obscured by local conditions. However, <strong>the</strong> <strong>in</strong>dividual bas<strong>in</strong>-fill<br />
successions bear a high-resolution record of local events and give unique <strong>in</strong>sights <strong>in</strong>to <strong>the</strong> local role of tectonics, sediment yield, and<br />
sea-level changes.<br />
Key Words: Sedimentology, sequence stratigraphy, Taurides, piggyback bas<strong>in</strong>, Gilbert-type delta, <strong>in</strong>cised valley-fill, <strong>Mess<strong>in</strong>ian</strong> sal<strong>in</strong>ity<br />
crisis, stratigraphic correlation<br />
1. Introduction<br />
The late Miocene Mediterranean event known as <strong>the</strong><br />
<strong>Mess<strong>in</strong>ian</strong> sal<strong>in</strong>ity crisis was triggered by a glacioeustatic<br />
sea-level fall comb<strong>in</strong>ed with <strong>the</strong> region’s tectonic<br />
separation from <strong>the</strong> Atlantic at <strong>the</strong> latest stages of <strong>the</strong><br />
Alp<strong>in</strong>e orogeny (Hsü et al. 1972; Ryan & Cita 1978; Cita &<br />
McKenzie 1986; Ryan 2009; Hüs<strong>in</strong>g et al. 2010). The event<br />
culm<strong>in</strong>ated <strong>in</strong> <strong>the</strong> evaporitic Lago Mare phase of partial or<br />
<strong>near</strong>ly complete desiccation and ended with <strong>the</strong> Zanclean<br />
mar<strong>in</strong>e flood<strong>in</strong>g, when <strong>the</strong> Atlantic waters reclaimed <strong>the</strong><br />
Mediterranean Bas<strong>in</strong>. A consentient 3-phase scenario<br />
for <strong>the</strong> <strong>Mess<strong>in</strong>ian</strong> event postulates (Roveri & Manzi<br />
2006): (1) a preevaporitic phase 7.25–5.96 Ma B.P., when<br />
organic-rich eux<strong>in</strong>ic deposits recorded a significantly<br />
* Correspondence: ayhan_ilgar@yahoo.com<br />
reduced circulation of Mediterranean deep waters and<br />
when microbial stromatolitic limestones formed <strong>in</strong> some<br />
peripheral bas<strong>in</strong>s; (2) <strong>the</strong> deposition phase of Lower<br />
Evaporites 5.96–5.60 Ma B.P., when <strong>the</strong> precipitation of<br />
gypsum occurred <strong>in</strong> shallow-water peripheral bas<strong>in</strong>s; and<br />
(3) <strong>the</strong> deposition phase of Upper Evaporites 5.60–5.33<br />
Ma B.P., when <strong>the</strong> nonmar<strong>in</strong>e Lago Mare environment<br />
formed <strong>in</strong> <strong>the</strong> lowest parts of a desiccat<strong>in</strong>g Mediterranean<br />
Bas<strong>in</strong>. The bulk amplitude of relative sea-level fall is<br />
estimated at 2000 to 3000 m (Ryan 2009).<br />
It may thus seem surpris<strong>in</strong>g that a regional event<br />
of such a great magnitude, orig<strong>in</strong>ally recognised from<br />
thick evaporites <strong>in</strong> <strong>the</strong> centre of <strong>the</strong> Mediterranean<br />
Bas<strong>in</strong>, is much less conspicuous at <strong>the</strong> bas<strong>in</strong> marg<strong>in</strong>s,<br />
1
where stratigraphic correlations of relative sea-level<br />
changes are difficult and controversial (Ryan 2009).<br />
One of <strong>the</strong> most contentious issues is <strong>the</strong> tim<strong>in</strong>g of <strong>the</strong><br />
onsets of hypersal<strong>in</strong>ity and evaporative drawdown <strong>in</strong><br />
<strong>the</strong> Mediterranean Sea, with direct implications for <strong>the</strong><br />
negative imbalance between <strong>the</strong> rate of water <strong>in</strong>flux from<br />
<strong>the</strong> Atlantic and <strong>the</strong> regional rate of evaporation. Regional<br />
studies suggest that <strong>the</strong> first precipitates at <strong>the</strong> deep<br />
bottom of <strong>the</strong> Mediterranean Bas<strong>in</strong> were preceded by a<br />
long stepwise advance towards hypersal<strong>in</strong>ity, with gypsum<br />
<strong>in</strong> peripheral bas<strong>in</strong>s precipitated well before <strong>the</strong> nom<strong>in</strong>al<br />
onset of <strong>the</strong> regional sal<strong>in</strong>ity crisis (see review by Ryan<br />
2009). Most researchers also suggest that <strong>the</strong> sal<strong>in</strong>ity crisis<br />
was preceded by a considerable early drawdown, with <strong>the</strong><br />
isolation of peripheral bas<strong>in</strong>s as evaporat<strong>in</strong>g lagoons and<br />
<strong>the</strong>ir eventual emergence (Rouchy 1982; Rouchy & Sa<strong>in</strong>t<br />
Mart<strong>in</strong> 1992; Clauzon et al. 1996; Rid<strong>in</strong>g et al. 1999; Soria<br />
et al. 2005; Maillard & Mauffret 2006; Rouchy & Caruso<br />
2006; Roveri & Manzi 2006). The early drawdown might<br />
not exceed 200 m (Dronkert 1985; Krijgsman et al. 1999),<br />
but would mark a negative water budget and would<br />
expectedly have a major impact on <strong>the</strong> peripheral bas<strong>in</strong>s<br />
and <strong>the</strong>ir stratigraphy. However, <strong>the</strong> peri-Mediterranean<br />
late Miocene stratigraphic record is fuzzy, comb<strong>in</strong><strong>in</strong>g<br />
relative sea-level changes caused by eustatic and local<br />
tectonic forc<strong>in</strong>g.<br />
The diversified tectono-geomorphic conditions<br />
of peripheral bas<strong>in</strong>s resulted <strong>in</strong> <strong>in</strong>tricate stratigraphic<br />
successions that are difficult to correlate and also difficult<br />
to relate to <strong>the</strong> evaporitic successions <strong>in</strong> offshore wells.<br />
Regional correlations are complicated by <strong>the</strong> fact that<br />
evaporites are found <strong>in</strong> only some of <strong>the</strong> peripheral<br />
bas<strong>in</strong>s, where <strong>the</strong>y may ei<strong>the</strong>r predate or postdate <strong>the</strong><br />
Mediterranean desiccation (Rid<strong>in</strong>g et al. 1999). The<br />
key <strong>in</strong>dicator of <strong>the</strong> early evaporative drawdown <strong>in</strong> <strong>the</strong><br />
peripheral bas<strong>in</strong>s might thus be not evaporites, but a<br />
regional surface of erosion (Ryan 2009). However, nei<strong>the</strong>r<br />
feature can easily be recognised and correlated <strong>in</strong> <strong>the</strong> bas<strong>in</strong>s<br />
(Rid<strong>in</strong>g et al. 1991, 1998; Roep et al. 1998; Soria et al. 2005;<br />
Roveri & Manzi 2006). The <strong>Mess<strong>in</strong>ian</strong> surface of subaerial<br />
erosion is highly irregular due to <strong>the</strong> varied rates of local<br />
denudation and it is not marked by any significant climatic<br />
change. It has been elevated by tectonics and overtaken<br />
by Plio–Pleistocene erosion <strong>in</strong> many bas<strong>in</strong>s (Glover et al.<br />
1998; Dilek et al. 1999; Deynoux et al. 2005; Monod et al.<br />
2006), and it splits <strong>in</strong>to 2 or more erosion surfaces towards<br />
<strong>the</strong> deep part of <strong>the</strong> Mediterranean Bas<strong>in</strong> (Ryan 2009) and<br />
commonly also landwards <strong>in</strong> <strong>the</strong> peripheral bas<strong>in</strong>s (Butler<br />
et al. 1995; Clauzon et al. 1996; Rid<strong>in</strong>g et al. 1998; Soria et<br />
al. 2003).<br />
The evidence of late Miocene <strong>regressions</strong>, commonly<br />
multiple, has been recognised <strong>in</strong> virtually all peri-<br />
Mediterranean bas<strong>in</strong>s at both active and passive marg<strong>in</strong>s<br />
2<br />
ILGAR et al. / Turkish J Earth Sci<br />
(Ryan 2009), but <strong>the</strong>se events are difficult to correlate and<br />
have been variously attributed to eustasy, high sediment<br />
supply, or local tectonic uplift (e.g., Clauzon et al. 1996;<br />
Rid<strong>in</strong>g et al. 1999; Karabıyıkoğlu et al. 2000; Larsen 2003;<br />
Soria et al. 2003, 2005; Deynoux et al. 2005; Flecker et al.<br />
2005; Roveri & Manzi 2006; Ç<strong>in</strong>er et al. 2008). Regional<br />
studies have po<strong>in</strong>ted to <strong>the</strong> importance of local tectonics<br />
<strong>in</strong> controll<strong>in</strong>g <strong>the</strong> late Miocene palaeogeography (Butler<br />
et al. 1995; Roveri & Manzi 2006). Many areas of <strong>the</strong><br />
Mediterranean were still subject to <strong>the</strong> f<strong>in</strong>al stages of <strong>the</strong><br />
Alp<strong>in</strong>e orogeny at that time, whereas it is generally difficult<br />
to dist<strong>in</strong>guish between eustatically <strong>forced</strong> and tectonically<br />
<strong>forced</strong> <strong>regressions</strong>, particularly if both factors were<br />
potentially <strong>in</strong>volved. The local tim<strong>in</strong>g of <strong>the</strong> late Miocene<br />
relative sea-level changes and <strong>the</strong> landward extent of<br />
<strong>the</strong> Zanclean mar<strong>in</strong>e reflood<strong>in</strong>g were probably both<br />
determ<strong>in</strong>ed by <strong>the</strong> comb<strong>in</strong>ation of eustasy, local tectonics,<br />
bas<strong>in</strong> topography, and sediment supply.<br />
This regional issue is addressed by <strong>the</strong> present study<br />
from <strong>the</strong> <strong>Adana</strong> Bas<strong>in</strong> at <strong>the</strong> north-eastern corner of <strong>the</strong><br />
Mediterranean (Figure 1a), where a regression due to<br />
tectonic <strong>in</strong>version of <strong>the</strong> bas<strong>in</strong> <strong>near</strong>ly co<strong>in</strong>cided with <strong>the</strong><br />
<strong>Mess<strong>in</strong>ian</strong> evaporative drawdown. The pr<strong>in</strong>cipal aims of<br />
<strong>the</strong> study are to: (1) give a palaeontologically constra<strong>in</strong>ed<br />
revised sequence stratigraphy of <strong>the</strong> <strong>Adana</strong> Bas<strong>in</strong>, with a<br />
focus on <strong>the</strong> late Miocene part of <strong>the</strong> bas<strong>in</strong>-fill succession;<br />
(2) assess <strong>the</strong> role of tectonics and eustasy <strong>in</strong> forc<strong>in</strong>g <strong>the</strong><br />
<strong>Mess<strong>in</strong>ian</strong> relative sea-level changes <strong>in</strong> <strong>the</strong> bas<strong>in</strong>; and (3)<br />
compare <strong>the</strong> late Miocene stratigraphy of <strong>the</strong> <strong>Adana</strong> Bas<strong>in</strong><br />
with that of <strong>the</strong> adjacent peri-Mediterranean bas<strong>in</strong>s <strong>in</strong><br />
order to draw regional implications.<br />
2. Term<strong>in</strong>ology<br />
The term “regression” denotes seaward displacement<br />
of shorel<strong>in</strong>e, result<strong>in</strong>g <strong>in</strong> a relative <strong>in</strong>crease of land area<br />
(Posamentier & Vail 1988; Posamentier et al. 1992).<br />
Regression reflects <strong>the</strong> <strong>in</strong>terplay between <strong>the</strong> relative<br />
sea-level change (i.e. <strong>the</strong> available accommodation)<br />
and <strong>the</strong> supply of sediment to <strong>the</strong> shorel<strong>in</strong>e (i.e. <strong>the</strong><br />
accommodation <strong>in</strong>fill<strong>in</strong>g). Their <strong>in</strong>terplay may result <strong>in</strong><br />
a normal or a <strong>forced</strong> regression (Posamentier et al. 1992;<br />
Posamentier & Morris 2000). A normal regression signifies<br />
relative sea-level stillstand or slow rise, with <strong>the</strong> high<br />
sediment supply caus<strong>in</strong>g seaward shorel<strong>in</strong>e displacement.<br />
A <strong>forced</strong> regression signifies a relative sea-level fall, with<br />
<strong>the</strong> latter caus<strong>in</strong>g seaward shorel<strong>in</strong>e displacement, even if<br />
<strong>the</strong> sediment supply to <strong>the</strong> shorel<strong>in</strong>e is negligible. A <strong>forced</strong><br />
regression may be caused by a eustatic sea-level fall, a<br />
tectonic uplift, or a co<strong>in</strong>cidental comb<strong>in</strong>ation of <strong>the</strong>se 2<br />
factors.<br />
The basic sequence-stratigraphic term<strong>in</strong>ology used here<br />
is accord<strong>in</strong>g to Catuneanu (2006). Stratigraphic sequence<br />
is a sedimentary succession deposited dur<strong>in</strong>g a full cycle of
A<br />
AGE FORMATION<br />
Holocene<br />
alluvium<br />
unconformity<br />
Pliocene-<br />
Pleistocene<br />
alluvial terraces<br />
unconformity<br />
Gökkuyu evaporitic mb<br />
Late Miocene<br />
Late Serravallia<strong>near</strong>ly<br />
Tortonian<br />
Middle Miocene<br />
Mesozoic<br />
Handere Fm.<br />
Karaisalı<br />
Fm.<br />
Güvenç<br />
Fm.<br />
deltaic members<br />
Handere Fm.<br />
conglomerates, sandstones<br />
mudstones & gypsum<br />
Kuzgun Fm.<br />
cong.,sst.& mudst<br />
unconformity<br />
Karaisalı Fm.<br />
reefal limestones, marls<br />
Güvenç Fm.<br />
mudstones, sandstones<br />
unconformity<br />
Carbonate bedrock<br />
ILGAR et al. / Turkish J Earth Sci<br />
5<br />
Muratlı<br />
Mb.<br />
7<br />
Middle<br />
Miocene<br />
Middle<br />
Miocene<br />
Lower<br />
Miocene<br />
Oligocene<br />
Palaeozoic<br />
& Mesozoic<br />
bedrock<br />
2<br />
6<br />
Tepeçaylak<br />
Mb.<br />
Taurus Orogenic Belt<br />
map C<br />
EXPLANATIONS<br />
deep-mar<strong>in</strong>e clastics Holocene<br />
fluvial-lagoonal clastics<br />
Pliocene-<br />
Pleistocene<br />
fluvial-lacustr<strong>in</strong>e clastics<br />
Upper<br />
Miocene<br />
lacustr<strong>in</strong>e carbonates<br />
Middle-Upper<br />
Miocene<br />
ophiolitic mélange<br />
limestones & clastics<br />
Middle-Upper<br />
Miocene<br />
Söğütlü<br />
Mb.<br />
alluvial terraces<br />
fluvial-shallow<br />
mar<strong>in</strong>e clastics<br />
mar<strong>in</strong>e<br />
marl-limestones<br />
reefal limestones<br />
Figure 1. (a) Topographic image of Anatolia (90-m resolution SRTM from Jarvis et al. 2008), show<strong>in</strong>g <strong>the</strong> location of <strong>the</strong> <strong>Adana</strong> Bas<strong>in</strong><br />
and o<strong>the</strong>r ma<strong>in</strong> peri-Mediterranean Miocene bas<strong>in</strong>s and major tectonic l<strong>in</strong>eaments referred to <strong>in</strong> <strong>the</strong> text. (b) Simplified geological<br />
map of <strong>the</strong> sou<strong>the</strong>rn part of <strong>the</strong> <strong>Adana</strong> Bas<strong>in</strong> and <strong>the</strong> adjacent Mut Bas<strong>in</strong> (based on Şenel 2002 and Ulu 2002); note <strong>the</strong> study area <strong>in</strong><br />
<strong>the</strong> former bas<strong>in</strong> (frame) and <strong>the</strong> location of a late Tortonian delta <strong>in</strong> <strong>the</strong> latter bas<strong>in</strong>. (c) Detailed geological map of <strong>the</strong> study area <strong>in</strong><br />
<strong>the</strong> <strong>Adana</strong> Bas<strong>in</strong>. Note <strong>the</strong> 3 isolated deltaic members of <strong>the</strong> uppermost Handere Formation. The po<strong>in</strong>ts 1–7 <strong>in</strong> maps B and C <strong>in</strong>dicate<br />
outcrop localities to which <strong>the</strong> paper’s o<strong>the</strong>r figures refer.<br />
1<br />
Çakıt river<br />
Kuzgun<br />
Salbaş<br />
3<br />
5 km<br />
4<br />
alluvium<br />
B<br />
C<br />
3
change <strong>in</strong> accommodation (i.e. its decrease and subsequent<br />
<strong>in</strong>crease), coupled with sediment supply. The term<br />
“sedimentary system” denotes a sedimentary environment<br />
and refers to its specific facies assemblage, whereas a<br />
systems tract is a succession of such palaeoenvironmental<br />
facies assemblages. A sequence is considered to be a<br />
vertical succession of relatively conformable systems<br />
tracts, bounded by unconformities (erosional surfaces<br />
of sediment bypass) that grade seawards <strong>in</strong>to correlative<br />
conformities. A parasequence is a succession of relatively<br />
conformable deposits bounded by flood<strong>in</strong>g surfaces and<br />
lack<strong>in</strong>g evidence of a relative base-level fall.<br />
Follow<strong>in</strong>g Helland-Hansen (2009), we dist<strong>in</strong>guish<br />
3 basic types of systems tracts as <strong>the</strong> build<strong>in</strong>g blocks<br />
of stratigraphic sequences: a <strong>forced</strong>-regressive systems<br />
tract (FRST) formed dur<strong>in</strong>g a relative sea-level fall; a<br />
transgressive systems tract (TST) formed dur<strong>in</strong>g a relative<br />
sea-level rise; and a normal-regressive systems tract<br />
formed dur<strong>in</strong>g ei<strong>the</strong>r highstand (HST) or lowstand (LST)<br />
and record<strong>in</strong>g sea-level stability or m<strong>in</strong>or relative rise.<br />
The basis for dist<strong>in</strong>guish<strong>in</strong>g systems tracts is <strong>the</strong> vertical<br />
stack<strong>in</strong>g of sedimentary facies assemblages and <strong>the</strong><br />
stratigraphic palaeoshorel<strong>in</strong>e trajectory (Helland-Hansen<br />
& Mart<strong>in</strong>sen 1996). A FRST has a fall<strong>in</strong>g trajectory, but<br />
<strong>the</strong> regressive shorel<strong>in</strong>e shift may <strong>in</strong>volve deposition or be<br />
fully erosional, depend<strong>in</strong>g on <strong>the</strong> sediment supply rate and<br />
<strong>the</strong> rate and magnitude of relative sea-level fall (Pl<strong>in</strong>t 1988;<br />
Helland-Hansen & Gjelberg 1994). With <strong>the</strong> sea-level fall<br />
compensated by tectonic subsidence, some sequences,<br />
referred to as <strong>the</strong> sequences of type 2 (Jervey 1988), may<br />
show no recognisable shorel<strong>in</strong>e fall and masquerade as<br />
parasequences (e.g., Gh<strong>in</strong>assi 2007; Mess<strong>in</strong>a et al. 2007).<br />
Parasequences consist of a TST overla<strong>in</strong> by a HST.<br />
The descriptive sedimentological term<strong>in</strong>ology used<br />
<strong>in</strong> this study is accord<strong>in</strong>g to Harms et al. (1975, 1982)<br />
and Coll<strong>in</strong>son and Thompson (1982). In biostratigraphic<br />
analysis, <strong>the</strong> Mediterranean planktonic foram<strong>in</strong>ifer zones<br />
of Iaccar<strong>in</strong>o et al. (2007) are followed, and <strong>the</strong> def<strong>in</strong>ition<br />
of species is based ma<strong>in</strong>ly on Kennett and Sr<strong>in</strong>ivasan<br />
(1973), Iaccar<strong>in</strong>o (1985), and Bolli and Saunders (1985).<br />
Biostratigraphic age estimates refer to <strong>the</strong> astronomically<br />
tuned ATNTS2004 scale (Lourens et al. 2004).<br />
3. Regional geological sett<strong>in</strong>g<br />
The Tauride orogen of sou<strong>the</strong>rn Turkey is <strong>the</strong> youngest of<br />
<strong>the</strong> eastern peri-Mediterranean Alp<strong>in</strong>e mounta<strong>in</strong> cha<strong>in</strong>s.<br />
It is arbitrarily divided <strong>in</strong>to 3 segments (Figure 1a): <strong>the</strong><br />
Western Taurides, west of <strong>the</strong> Isparta Angle, pass<strong>in</strong>g<br />
westwards <strong>in</strong>to <strong>the</strong> Hellenides and sometimes referred to<br />
as <strong>the</strong> Eastern Hellenides due to <strong>the</strong>ir tectonic l<strong>in</strong>k with<br />
<strong>the</strong> Hellenic subduction arc; <strong>the</strong> Central Taurides between<br />
<strong>the</strong> Isparta Angle and <strong>the</strong> Ecemiş Fault to <strong>the</strong> east; and<br />
<strong>the</strong> Eastern Taurides that pass eastwards <strong>in</strong>to <strong>the</strong> Zagros<br />
Mounta<strong>in</strong>s. The orogeny culm<strong>in</strong>ated at <strong>the</strong> end of <strong>the</strong><br />
4<br />
ILGAR et al. / Turkish J Earth Sci<br />
Eocene (Şengör 1987; Clark & Robertson 2002), but lowrate<br />
plate convergence <strong>in</strong> <strong>the</strong> Central Taurides persisted<br />
until <strong>the</strong> mid-Oligocene (Kell<strong>in</strong>g et al. 1987; Andrew<br />
& Robertson 2002), when <strong>the</strong> Cyprian subduction arc<br />
eventually stepped back to <strong>the</strong> south of Cyprus (Figure 1a).<br />
Orogenic deformation proceeded until <strong>the</strong> late Miocene<br />
<strong>in</strong> <strong>the</strong> Eastern Taurides, where <strong>the</strong> Misis Structural High<br />
popped up by fold<strong>in</strong>g and thrust<strong>in</strong>g (Michard et al. 1984;<br />
Aktaş & Robertson 1990; Dilek & Moores 1990; Yılmaz<br />
1993; Yılmaz et al. 1993; Robertson 2000; Sunal & Tüysüz<br />
2002), and also at <strong>the</strong> transition of <strong>the</strong> Western and<br />
Central Taurides, where <strong>the</strong> Lycian and Hoyran-Hadım<br />
nappe fronts collided north of <strong>the</strong> Isparta Angle (Coll<strong>in</strong>s<br />
& Robertson 1998, 2000; Poisson et al. 2003; Sagular &<br />
Görmüş 2006). The Miocene thus saw <strong>the</strong> last stages of<br />
localised compressional deformation, while <strong>the</strong> Taurides<br />
<strong>in</strong> general had already become subject to postorogenic<br />
isostatic uplift and crustal extension with <strong>the</strong> development<br />
of orogen-collapse bas<strong>in</strong>s (Seyitoğlu & Scott 1991, 1996;<br />
Jaffey & Robertson 2005; Bartol et al. 2011; Koç et al. 2011;<br />
Cosent<strong>in</strong>o et al. 2012).<br />
The peri-Mediterranean bas<strong>in</strong>s <strong>in</strong> sou<strong>the</strong>rn Turkey<br />
formed nonsynchronously dur<strong>in</strong>g <strong>the</strong> early Miocene and<br />
ranged from relatively simple <strong>in</strong>tramontane grabens or<br />
half-grabens (Alçiçek et al. 2005; Alçiçek 2010) to more<br />
complex extensional depressions (Flecker et al. 1995,<br />
2005; Larsen 2003; Şafak et al. 2005; Ç<strong>in</strong>er et al. 2008),<br />
strike-slip pull-apart features (Ilgar & Nemec 2005), and<br />
compressional foreland troughs (Hayward 1984a, 1984b;<br />
Burton-Ferguson et al. 2005; Alçiçek & Ten Veen 2008).<br />
The bas<strong>in</strong>-fill successions of <strong>the</strong>se isolated molasse bas<strong>in</strong>s<br />
are highly diversified <strong>in</strong> terms of sedimentary facies and<br />
sequence stratigraphy, and are difficult to correlate (Tekeli<br />
& Göncüoğlu 1984; Yetiş et al. 1995; Durand et al. 1999;<br />
Bozkurt et al. 2000; Kell<strong>in</strong>g et al. 2005). However, <strong>the</strong>y<br />
provide crucial <strong>in</strong>formation on an early postorogenic<br />
tectono-geomorphic evolution of <strong>the</strong> Tauride belt and its<br />
<strong>in</strong>teraction with <strong>the</strong> Mediterranean Sea. As po<strong>in</strong>ted out<br />
by Kell<strong>in</strong>g et al. (2005, pp. 1–13), <strong>the</strong> palaeogeographical<br />
and chronostratigraphical resolution of <strong>the</strong> local bas<strong>in</strong>-fill<br />
successions far exceeds that of geophysical lithospheric<br />
models and gives unique regional <strong>in</strong>sights <strong>in</strong>to <strong>the</strong> relative<br />
role of tectonics, climate, sediment yield, and sea-level<br />
changes. Detailed palaeogeographical reconstructions and<br />
<strong>the</strong> recognition of major sediment-transfer fairways to<br />
<strong>the</strong> offshore zone (Satur et al. 2005) are vital to regional<br />
hydrocarbon prospect<strong>in</strong>g (Görür & Tüysüz 2001).<br />
The <strong>Adana</strong> Bas<strong>in</strong> is one of <strong>the</strong> largest Miocene<br />
peripheral bas<strong>in</strong>s <strong>in</strong> sou<strong>the</strong>rn Turkey, located between<br />
<strong>the</strong> Taurus orogenic front to <strong>the</strong> north-west and <strong>the</strong> Misis<br />
Structural High to <strong>the</strong> south-east (Figure 1a). The SWtrend<strong>in</strong>g<br />
bas<strong>in</strong> passes offshore <strong>in</strong>to <strong>the</strong> Cilicia Bas<strong>in</strong> north<br />
of Cyprus. The <strong>Adana</strong> Bas<strong>in</strong> and its smaller counterpart,<br />
İskenderun Bas<strong>in</strong> on <strong>the</strong> o<strong>the</strong>r side of <strong>the</strong> Misis High,
form <strong>the</strong> Çukurova Bas<strong>in</strong> Complex at <strong>the</strong> Kahramanmaraş<br />
junction of <strong>the</strong> Afro-Arabian, Anatolian, and Eurasian<br />
plates (Ünlügenç et al. 1990). The structural development<br />
<strong>in</strong> this region <strong>in</strong>volved 3 major tectonic l<strong>in</strong>eaments<br />
(Figure 1a): <strong>the</strong> Bitlis-Zagros Suture Zone separat<strong>in</strong>g <strong>the</strong><br />
Arabian and Anatolian-Eurasian plates; <strong>the</strong> eastern arm<br />
of <strong>the</strong> Cyprian arc of <strong>in</strong>tra-Tethyan plate subduction; and<br />
<strong>the</strong> s<strong>in</strong>istral strike-slip Dead Sea Fault between Africa and<br />
Arabia, pass<strong>in</strong>g to <strong>the</strong> north-east <strong>in</strong>to <strong>the</strong> East Anatolian<br />
Fault (Kell<strong>in</strong>g et al. 1987; Ünlügenç et al. 1990; Williams et<br />
al. 1995; Robertson 2000). The system of <strong>the</strong> East Anatolian<br />
and North Anatolian faults lead <strong>the</strong> neotectonic westward<br />
“expulsion” of <strong>the</strong> compound Anatolian craton (Dewey &<br />
Şengör 1979; Şengör & Yılmaz 1981). Derivatives of this<br />
neotectonic strike-slip system <strong>in</strong>clude <strong>the</strong> Burdur-Fethiye-<br />
Pl<strong>in</strong>y Fault to <strong>the</strong> west and <strong>the</strong> Ecemiş Fault separat<strong>in</strong>g <strong>the</strong><br />
<strong>Adana</strong> Bas<strong>in</strong> from <strong>the</strong> coeval Mut Bas<strong>in</strong> (Figure 1a).<br />
The <strong>Adana</strong> Bas<strong>in</strong> formed <strong>in</strong> <strong>the</strong> early Miocene on<br />
a wedge-shaped sliver of <strong>the</strong> Tethyan shelf that was<br />
structurally entrapped between <strong>the</strong> Anatolian and Arabian<br />
plates and converted <strong>in</strong>to <strong>the</strong> local Tauride foreland. Seismic<br />
<strong>in</strong>terpretation by Burton-Ferguson et al. (2005) suggests<br />
that <strong>the</strong> <strong>Adana</strong> foreland developed by flexural subsidence<br />
under <strong>the</strong> load of a SE-advanc<strong>in</strong>g orogenic front and <strong>the</strong>n<br />
turned <strong>in</strong>to a piggyback bas<strong>in</strong> <strong>in</strong> <strong>the</strong> Tortonian, with <strong>the</strong><br />
Misis High pop-up ridge separat<strong>in</strong>g it from <strong>the</strong> İskenderun<br />
foredeep to <strong>the</strong> south-east (Figures 1a and 1b). The foreland<br />
model expla<strong>in</strong>s <strong>the</strong> Miocene strong subsidence and great<br />
thickness of sediments accumulated <strong>in</strong> <strong>the</strong> bas<strong>in</strong> as well as<br />
<strong>the</strong> bas<strong>in</strong>’s late Miocene compressional tectonic <strong>in</strong>version.<br />
4. Dynamic stratigraphy of <strong>the</strong> <strong>Adana</strong> Bas<strong>in</strong><br />
The stratigraphy of <strong>the</strong> <strong>Adana</strong> Bas<strong>in</strong> was established by<br />
Schmidt (1961) and ref<strong>in</strong>ed by subsequent studies (Yalçın<br />
& Görür 1984; Kell<strong>in</strong>g et al. 1987; Yetiş 1988; Ünlügenç<br />
et al. 1990; Görür 1992; Yetiş et al. 1995; Nazik 2004;<br />
Satur et al. 2005). The present study contributes fur<strong>the</strong>r<br />
to this topic. The bas<strong>in</strong>-fill succession comprises up to 6<br />
km of Miocene to Quaternary siliciclastic and calcareous<br />
deposits. Bedrock consists of Palaeozoic and Mesozoic<br />
sedimentary rocks, which <strong>in</strong>clude Devonian corall<strong>in</strong>e<br />
limestones and sandstones, Permo-Carbonifereous<br />
limestones, a Late Triassic to Cretaceous thick carbonate<br />
platform, and Late Cretaceous turbidites. These rocks were<br />
postdated by <strong>the</strong> tectonic emplacement of a nappe of Late<br />
Cretaceous ophiolitic mélange (Figure 1b).<br />
Sedimentation <strong>in</strong> <strong>the</strong> bas<strong>in</strong> commenced <strong>in</strong> <strong>the</strong> early<br />
Miocene with deposition of <strong>the</strong> alluvial fan redbeds of <strong>the</strong><br />
Gildirli Formation (Figure 2), <strong>in</strong>clud<strong>in</strong>g conglomerates,<br />
sandstones, and mudstones. The Burdigalian to early<br />
Langhian Kaplankaya Formation recorded <strong>the</strong> first<br />
episode of mar<strong>in</strong>e sedimentation <strong>in</strong> <strong>the</strong> bas<strong>in</strong>, with<br />
sandstones, siltstones, marlstones, and sandy limestones.<br />
ILGAR et al. / Turkish J Earth Sci<br />
This transgressive formation has a broader lateral extent,<br />
particularly northwards, and unconformably overlies<br />
bedrock palaeotopography. Reefal limestones formed<br />
<strong>in</strong> <strong>the</strong> marg<strong>in</strong>al zone of <strong>the</strong> bas<strong>in</strong>, while open-mar<strong>in</strong>e<br />
deep neritic conditions prevailed <strong>in</strong> <strong>the</strong> bas<strong>in</strong> <strong>in</strong>terior.<br />
The Kaplankaya Formation thus passes laterally <strong>in</strong>to and<br />
is partly overla<strong>in</strong> by <strong>the</strong> late Burdigalian–Serravalian<br />
reefal Karaisalı Formation, whose bas<strong>in</strong>al equivalents<br />
are sublittoral tempestitic sandstones of <strong>the</strong> C<strong>in</strong>göz<br />
Formation and offshore mudstones of <strong>the</strong> Güvenç<br />
Formation (Figure 2). There is also evidence of stormgenerated<br />
erosive turbidity currents transferr<strong>in</strong>g abundant<br />
sand across <strong>the</strong> shelf edge to <strong>the</strong> deep-water realm of <strong>the</strong><br />
adjo<strong>in</strong><strong>in</strong>g Cilicia Bas<strong>in</strong> (Satur et al. 2005). The reefal and<br />
coeval <strong>near</strong>shore to offshore deposits show an overall<br />
shallow<strong>in</strong>g-upwards trend, with <strong>the</strong> upper part of <strong>the</strong><br />
Güvenç Formation <strong>in</strong>creas<strong>in</strong>gly richer <strong>in</strong> sandstones<br />
(Figure 2).<br />
The mar<strong>in</strong>e sedimentation was <strong>in</strong>terrupted when<br />
<strong>the</strong> bas<strong>in</strong> emerged due to a relative sea-level fall at <strong>the</strong><br />
end of Serravalian (Figure 2). River valleys were <strong>in</strong>cised<br />
and <strong>the</strong>n filled with <strong>the</strong> fluvial deposits of <strong>the</strong> Kuzgun<br />
Formation, as <strong>the</strong> bas<strong>in</strong> was subsequently reflooded due<br />
to an early Tortonian relative sea-level rise. A transgressive<br />
rav<strong>in</strong>ement surface with a lag of wave-worked oysterbear<strong>in</strong>g<br />
gravel marks <strong>the</strong> mar<strong>in</strong>e reflood<strong>in</strong>g. The<br />
transgression <strong>in</strong>itiated shallow-mar<strong>in</strong>e sedimentation<br />
with a second generation of reefal limestones along<br />
<strong>the</strong> bas<strong>in</strong> marg<strong>in</strong>, <strong>the</strong> Tırtar Formation, superimposed<br />
directly on <strong>the</strong> older limestones of <strong>the</strong> Karaisalı Formation<br />
(Figure 2). The coeval Handere Formation <strong>in</strong> <strong>the</strong> bas<strong>in</strong><br />
<strong>in</strong>terior consists of shoreface sandstones that pass upward<br />
<strong>in</strong>to f<strong>in</strong>er-gra<strong>in</strong>ed sandstones, siltstones, and mudstones of<br />
an offshore-transition environment and fur<strong>the</strong>r <strong>in</strong>to thick<br />
offshore mudstones (Figure 2). The deposition of offshore<br />
mudstones <strong>in</strong> <strong>the</strong> upper part of <strong>the</strong> Handere Formation<br />
marked <strong>the</strong> maximum mar<strong>in</strong>e flood<strong>in</strong>g <strong>in</strong> <strong>the</strong> bas<strong>in</strong>,<br />
reached <strong>in</strong> <strong>the</strong> late Tortonian.<br />
These transgressive deposits are sharply overla<strong>in</strong> by<br />
<strong>the</strong> latest Tortonian–<strong>Mess<strong>in</strong>ian</strong> regressive deposits of<br />
<strong>the</strong> uppermost Handere Formation (Figure 2), which<br />
comprise shallow-mar<strong>in</strong>e sandstones and siltstones<br />
and <strong>in</strong>clude 3 isolated conglomeratic members (see <strong>the</strong><br />
Muratlı, Tepeçaylak, and Sögütlü members <strong>in</strong> Figure 1c).<br />
These conglomeratic deposits, previously <strong>in</strong>terpreted<br />
as fluvial, are <strong>the</strong> ma<strong>in</strong> topic of <strong>the</strong> present study, which<br />
documents <strong>the</strong>m as sharp-based deltas with associated<br />
<strong>in</strong>cised fluvial valley-fills. There are also erosional relics<br />
of <strong>the</strong> uppermost gypsiferous Gökkuyu Member of <strong>the</strong><br />
Handere Formation preserved <strong>in</strong> <strong>the</strong> sou<strong>the</strong>rn part of<br />
<strong>the</strong> bas<strong>in</strong> (Figures 1c and 2). The evaporites overlie both<br />
<strong>the</strong> deltaic conglomeratic members and offshore clastic<br />
deposits of <strong>the</strong> Handere Formation. However, <strong>the</strong>re is no<br />
evidence of <strong>the</strong> Zanclean regional mar<strong>in</strong>e transgression <strong>in</strong><br />
5
6<br />
0<br />
1<br />
2<br />
3<br />
4<br />
5<br />
6<br />
7<br />
8<br />
9<br />
10<br />
11<br />
12<br />
13<br />
14<br />
15<br />
16<br />
17<br />
18<br />
19<br />
20<br />
21<br />
22<br />
23<br />
Chronostratigraphy (Ma)<br />
Epoch Stage<br />
Holocene Tyrrhenian<br />
Ionian<br />
Pleistocene<br />
Pliocene<br />
Early Late<br />
Miocene<br />
Early Middle<br />
Late<br />
Calabrian<br />
1.81<br />
Gelasian<br />
2.59<br />
Piacenzian<br />
3.60<br />
Zanclean<br />
5.33<br />
<strong>Mess<strong>in</strong>ian</strong><br />
7.25<br />
Tortonian<br />
11.61<br />
Serravallian<br />
13.65<br />
Langhian<br />
15.97<br />
Burdigalian<br />
20.43<br />
Aquitanian<br />
Plankt.<br />
foram<br />
zones<br />
Mple2<br />
Mple1<br />
Mpl6<br />
Mpl5<br />
Mpl4<br />
Mpl3<br />
Mpl2<br />
Mpl1<br />
MMi13<br />
MMi12<br />
MMi11<br />
ILGAR et al. / Turkish J Earth Sci<br />
Nannofossil<br />
zones<br />
MNN21<br />
MNN20<br />
MNN19<br />
MNN18<br />
MNN17<br />
MNN16<br />
14-15<br />
MNN13<br />
MNN12<br />
Nondist<strong>in</strong>ctive Zone<br />
MMi10<br />
MMi9<br />
MMi8<br />
c<br />
MMi7 b<br />
a<br />
MMi6<br />
MMi5<br />
MMi4<br />
MMi3<br />
MMi2<br />
MMi1<br />
c<br />
b<br />
a<br />
b<br />
a<br />
MNN11<br />
MNN10<br />
MNN9<br />
MNN8<br />
MNN7<br />
MNN6<br />
MNN5<br />
MNN4<br />
MNN3<br />
MNN2<br />
MNN1<br />
c<br />
b<br />
a<br />
b<br />
a<br />
b<br />
a<br />
c<br />
b<br />
a<br />
Tırtar<br />
Fm.<br />
Muratlı<br />
deltaic mb<br />
Karaisalı<br />
Fm.<br />
ADANA BASIN<br />
Gökkuyu<br />
evaporitic mb<br />
Sequence<br />
stratigraphy<br />
?HST + FRST<br />
+ LST<br />
Figure 2. Revised stratigraphy of <strong>the</strong> <strong>Adana</strong> Bas<strong>in</strong> and its <strong>in</strong>terpretation <strong>in</strong> terms of systems tracts. The letter code is as used <strong>in</strong> <strong>the</strong> text<br />
(term<strong>in</strong>ology after Helland-Hansen 2009): LST – normal-regressive lowstand systems tract; TST – transgressive systems tract; HST –<br />
normal-regressive highstand systems tract; and FRST – <strong>forced</strong>-regressive systems tract.<br />
C<strong>in</strong>göz<br />
Fm.<br />
Kaplankaya Fm.<br />
MESOZOIC<br />
BEDROCK<br />
v v v v v v v<br />
v v v v v v v<br />
v v v v v<br />
v v v<br />
Handere Fm.<br />
Kuzgun Fm.<br />
Güvenç Fm.<br />
Gildirli Fm.<br />
Post - Miocene<br />
alluvium<br />
(fluvial terraces)<br />
FRST<br />
HST<br />
TST<br />
TST<br />
FRST + LST<br />
HST<br />
TST<br />
LST
<strong>the</strong> bas<strong>in</strong>. The post-Miocene deposits are fluvial terraces of<br />
coarse-gra<strong>in</strong>ed alluvium with caliche.<br />
The <strong>Mess<strong>in</strong>ian</strong> gypsum evaporites <strong>in</strong> <strong>the</strong> bas<strong>in</strong> are up to<br />
a few metres thick (Figure 3a) and <strong>the</strong>ir ma<strong>in</strong> varieties range<br />
from massive to lam<strong>in</strong>ated and enterolithic (Figure 3b),<br />
micro- to coarse-crystall<strong>in</strong>e (Figures 3c and 3d), nodular<br />
(Figure 3e), and wave-worked gypsarenitic (Figure 3f).<br />
X-ray diffraction data show that selenitic gypsum is <strong>the</strong><br />
sole evaporitic m<strong>in</strong>eral (Karakuş 2011). X-ray fluorescence<br />
analyses of major oxide composition <strong>in</strong>dicate that <strong>the</strong><br />
evaporitic precipitation occurred <strong>in</strong> homogeneous<br />
hydrochemical conditions, with a Sr-signature similar to<br />
<strong>the</strong> <strong>Mess<strong>in</strong>ian</strong> evaporites <strong>in</strong> adjacent peri-Mediterranean<br />
bas<strong>in</strong>s (Karakuş 2011).<br />
5. Facies architecture of deltaic members<br />
The study focuses on <strong>the</strong> 3 isolated conglomeratic members<br />
of <strong>the</strong> Handere Formation: <strong>the</strong> Muratlı, Tepeçaylak, and<br />
Sögütlü members (Figure 1c). They have been exhumed by<br />
Quaternary erosion and are laterally surrounded by sparsely<br />
preserved shallow-mar<strong>in</strong>e sandstones of <strong>the</strong> Handere<br />
Formation, with which <strong>the</strong>y sharply overlie <strong>the</strong> formation’s<br />
offshore mudstones (Figure 2). These conglomeratic<br />
members consist of 2 ma<strong>in</strong> facies associations, Gilberttype<br />
deltaic deposits and fluvial <strong>in</strong>cised valley-fill deposits,<br />
which are described and <strong>in</strong>terpreted <strong>in</strong> <strong>the</strong> present section.<br />
5.1. Gilbert-type delta deposits<br />
These conglomeratic deposits are generally well-bedded,<br />
form<strong>in</strong>g cl<strong>in</strong>oformal wedges that are stacked bas<strong>in</strong>wards<br />
<strong>in</strong> a downstepp<strong>in</strong>g pattern and are up to 15–40 m thick.<br />
The cl<strong>in</strong>oformal architecture consists of <strong>in</strong>cl<strong>in</strong>ed foreset<br />
beds overla<strong>in</strong> by horizontal topset beds (Figure 4a), as<br />
is generally characteristic of Gilbert-type deltas (Barrell<br />
1912; Colella 1988; Postma 1990).<br />
5.1.1. Foreset facies<br />
Foreset deposits are conglomerate and subord<strong>in</strong>ate<br />
sandstone beds <strong>in</strong>cl<strong>in</strong>ed bas<strong>in</strong>wards at up to 25°<br />
(Figure 4b). They show an overall coarsen<strong>in</strong>g-upwards<br />
trend and comprise facies commonly reported from<br />
Gilbert-type deltas (Postma 1984; Nemec et al. 1999;<br />
Lønne & Nemec 2004; Breda et al. 2007). Some outcrops<br />
show <strong>the</strong> foreset beds pass<strong>in</strong>g tangentially downdip <strong>in</strong>to<br />
<strong>the</strong> gently <strong>in</strong>cl<strong>in</strong>ed and f<strong>in</strong>er-gra<strong>in</strong>ed beds of delta toeset<br />
(Figure 4a). Conglomerate beds are 10–75 cm thick, but<br />
ma<strong>in</strong>ly 15–35 cm, and are tabular to mound-shaped. They<br />
consist of granule to coarse-pebble gravel and occasionally<br />
conta<strong>in</strong> scattered cobbles of up to 15 cm <strong>in</strong> size. The gravel<br />
is subrounded to rounded and has ma<strong>in</strong>ly a clast-supported<br />
texture (Figure 4c). Clasts are derived from <strong>the</strong> bedrock<br />
Mesozoic limestones and serpent<strong>in</strong>ite, and from <strong>the</strong> bas<strong>in</strong>marg<strong>in</strong><br />
Miocene reefal limestones. The matrix is moderately<br />
well-sorted sand with granules. Many conglomerate<br />
beds and <strong>the</strong> majority of associated sandstone beds<br />
ILGAR et al. / Turkish J Earth Sci<br />
show planar-parallel stratification (Figure 4b) <strong>in</strong>dicat<strong>in</strong>g<br />
tractional deposition from fully turbulent hyperpycnal<br />
flows (Bornhold & Prior 1990; Nemec 1990), which means<br />
river-generated low-density turbidity currents (sensu<br />
Lowe 1982). Massive conglomerate beds are nongraded or<br />
<strong>in</strong>versely graded (Figure 4d), tabular <strong>in</strong> dip section, and<br />
mound-shaped lenticular <strong>in</strong> strike section, <strong>in</strong>terpreted to<br />
be deposits of cohesionless debris flows (Nemec & Steel<br />
1984; Nemec 1990).<br />
Sandstones predom<strong>in</strong>ate <strong>in</strong> <strong>the</strong> down-dip part of <strong>the</strong><br />
foreset and at its toe, form<strong>in</strong>g tabular or wedge-shaped<br />
beds that are 5–30 cm thick, composed of very coarse- to<br />
f<strong>in</strong>e-gra<strong>in</strong>ed sand and alternat<strong>in</strong>g with th<strong>in</strong> beds of granule<br />
conglomerate (Figure 4a). Common are scattered pebbles<br />
of up to 5 cm <strong>in</strong> size. The sandstone beds show planarparallel<br />
stratification with or without normal grad<strong>in</strong>g<br />
and are often capped by current-ripple cross-lam<strong>in</strong>ation<br />
with down-dip transport direction. Some of <strong>the</strong> foreset<br />
beds, up to 40 cm thick, are isolated backsets of up-slope<br />
dipp<strong>in</strong>g cross-strata composed of coarse sand and/or f<strong>in</strong>epebble<br />
gravel (Figure 4e). They occur on <strong>the</strong> stoss side of<br />
mound-shaped massive conglomerate bodies (debris-flow<br />
deposits) or as <strong>the</strong> <strong>in</strong>fill of trough-shaped scours (deltaslope<br />
chutes). The backsets <strong>in</strong>dicate tractional deposition<br />
by low-density turbidity currents subject to hydraulic jump<br />
(Nemec 1990). There are also sporadic slump deposits of<br />
variable scale and thickness (Figure 4f).<br />
5.1.2. Topset facies<br />
The delta topset deposits (Figures 4a and 5) are pebble<br />
conglomerates and coarse-gra<strong>in</strong>ed sandstones. Their<br />
f<strong>in</strong><strong>in</strong>g-upwards bedsets, 60–140 cm thick, have erosional<br />
bases and are commonly stacked on top of one ano<strong>the</strong>r,<br />
apparently represent<strong>in</strong>g multistorey palaeochannels of<br />
braided streams a few metres wide (Coll<strong>in</strong>son 1996; Miall<br />
1996). Their laterally discont<strong>in</strong>uous basal layers of coarse<br />
clast-supported conglomerate are thought to be channelfloor<br />
lag deposits (Miall 1985; Nemec & Postma 1993).<br />
Planar parallel-stratified and cross-stratified beds, 10–45<br />
cm thick, are <strong>in</strong>terpreted, respectively, to be deposits of<br />
longitud<strong>in</strong>al and transverse or oblique midchannel bars<br />
(Miall 1985; Nemec & Postma 1993).<br />
The deltas suffered erosion and <strong>the</strong>ir topset deposits<br />
are <strong>in</strong>consistently preserved, generally better <strong>in</strong> <strong>the</strong><br />
upstream part (Figure 4a). The sparser downstream<br />
preservation of delta topset may be due to a negative<br />
subaerial accommodation (Bhattacharya & Willis 2001),<br />
or to removal by post-Miocene erosion (Figure 2). The<br />
relationship of <strong>the</strong> delta topset to <strong>the</strong> foreset is <strong>in</strong>variably<br />
oblique (erosional), which supports <strong>the</strong> notion of a fall<strong>in</strong>g<br />
delta-shorel<strong>in</strong>e trajectory (Breda et al. 2007, 2009) based<br />
on evidence that <strong>the</strong> horizontal topset was <strong>in</strong>crementally<br />
stepp<strong>in</strong>g down <strong>in</strong> <strong>the</strong> bas<strong>in</strong>ward direction, as discussed <strong>in</strong><br />
<strong>the</strong> next section.<br />
7
5.1.3. Bottomset facies<br />
The basal deltaic facies are only locally exposed, but are<br />
generally similar. The gently <strong>in</strong>cl<strong>in</strong>ed delta-toe deposits<br />
(Figures 4a and 6) are th<strong>in</strong>ly bedded, f<strong>in</strong>e-gra<strong>in</strong>ed<br />
sandstones and siltstones with plane-parallel stratification<br />
and m<strong>in</strong>or ripple cross-lam<strong>in</strong>ation. Delta bottomset<br />
consists of th<strong>in</strong> siltstone and sandstone beds <strong>in</strong>tercalated<br />
with mudstones (Figure 6). The microfauna content of<br />
<strong>the</strong>se deposits is described <strong>in</strong> a subsequent section.<br />
5.2. Incised valley-fill deposits<br />
This facies assemblage is exposed <strong>in</strong> a chance crosscut<br />
section <strong>in</strong> <strong>the</strong> proximal part of <strong>the</strong> Muratlı Member<br />
(Figures 1c and 5), but similar unexposed deposits<br />
presumably also occur <strong>in</strong> <strong>the</strong> 2 o<strong>the</strong>r coeval deltaic members<br />
8<br />
ILGAR et al. / Turkish J Earth Sci<br />
A B<br />
C<br />
1 m<br />
E F<br />
Figure 3. <strong>Mess<strong>in</strong>ian</strong> evaporites <strong>in</strong> <strong>the</strong> <strong>Adana</strong> Bas<strong>in</strong>. (a) An example outcrop of <strong>the</strong> evaporites at<br />
<strong>the</strong> top of Handere Formation. (b) Enterolithic gypsum. (c) Crystall<strong>in</strong>e gypsum with a chevron<br />
growth structure. (d) Crystall<strong>in</strong>e gypsum with a grassy growth structure. (e) Nodular gypsum.<br />
(f) Gypsarenite with wave-ripple cross-lam<strong>in</strong>ation. The co<strong>in</strong> (scale) is 2 cm.<br />
D<br />
of <strong>the</strong> Handere Formation, where no similar transverse<br />
sections are available. These deposits are recognisably<br />
coarser-gra<strong>in</strong>ed, compris<strong>in</strong>g pebble conglomerates and<br />
subord<strong>in</strong>ate coarse-gra<strong>in</strong>ed sandstones with scattered<br />
cobbles and boulders (Figure 5). Conglomerates are clastsupported,<br />
with a matrix of medium to coarse sand and<br />
granules. Gravel clasts are moderately sorted, ma<strong>in</strong>ly<br />
subangular to subrounded, and of <strong>the</strong> same provenance<br />
as <strong>the</strong> delta gravel. Scattered boulders are derived from<br />
<strong>the</strong> bas<strong>in</strong>-marg<strong>in</strong> Miocene reefal limestones. The deposits<br />
form erosionally based, vertically stacked f<strong>in</strong><strong>in</strong>g-upwards<br />
bedsets (Figure 5) <strong>in</strong>terpreted to be multistorey braidedstream<br />
palaeochannels (Coll<strong>in</strong>son 1996; Miall 1996),<br />
ma<strong>in</strong>ly 0.8–1.6 m thick and 10–25 m wide. Coarse gravelly<br />
channel-floor lags are poorly developed, but solitary
delta topset<br />
delta foreset<br />
ILGAR et al. / Turkish J Earth Sci<br />
B C<br />
E F<br />
foreset<br />
backset<br />
Figure 4. Outcrop details of <strong>the</strong> Muratlı delta, <strong>Adana</strong> Bas<strong>in</strong>. (a) Longitud<strong>in</strong>al outcrop section show<strong>in</strong>g an<br />
erosional angular contact between <strong>the</strong> delta’s foreset and topset deposits. (b) Conglomeratic foreset deposits<br />
compris<strong>in</strong>g planar parallel-stratified and massive beds. Note <strong>the</strong> rapid upward <strong>in</strong>crease <strong>in</strong> <strong>the</strong> bedd<strong>in</strong>g<br />
<strong>in</strong>cl<strong>in</strong>ation. (c) Close-up detail of <strong>the</strong> delta topset, show<strong>in</strong>g submature gravel composed of bedrock limestone<br />
and serpent<strong>in</strong>ite clasts mixed with large fragments of Miocene corals and reefal limestones. (d) Delta foreset<br />
deposits <strong>in</strong>clud<strong>in</strong>g massive, <strong>in</strong>versely graded, and nongraded conglomerate beds. (e) Delta foreset detail show<strong>in</strong>g<br />
a backset of upslope-dipp<strong>in</strong>g gravelly cross-strata. (f) Slump deposits with<strong>in</strong> <strong>the</strong> delta foreset. Picture A is from<br />
locality 1, pictures B–E from locality 2, and picture F from locality 3 <strong>in</strong> Figure 1c.<br />
D<br />
coral fragment<br />
A<br />
9
10<br />
°<br />
or multiple cross-strata sets, 25–60 cm thick, <strong>in</strong>dicate<br />
transverse or oblique midchannel bars (Miall 1985).<br />
This contrast<strong>in</strong>g facies assemblage <strong>in</strong> <strong>the</strong> Muratlı<br />
Member forms <strong>the</strong> <strong>in</strong>fill of an axial valley that was deeply<br />
<strong>in</strong>cised <strong>in</strong> <strong>the</strong> delta. The top part of <strong>the</strong> valley-fill and <strong>the</strong><br />
surround<strong>in</strong>g host delta are not preserved <strong>in</strong> <strong>the</strong> outcrop<br />
section, but <strong>the</strong> measured depth of <strong>in</strong>cision is at least<br />
15 m and <strong>the</strong> valley width is up to 60 m. The <strong>in</strong>cised<br />
valley is clearly not an <strong>in</strong>tegral part of <strong>the</strong> prograd<strong>in</strong>g<br />
delta’s topset (see discussion by Hampson et al. 1997) and<br />
<strong>in</strong>stead <strong>in</strong>dicates erosional cannibalisation of <strong>the</strong> delta by<br />
a deep <strong>in</strong>cision of its fluvial feeder system <strong>in</strong> response to<br />
pronounced base-level fall (see Mellere et al. 2002; Ilgar<br />
& Nemec 2005; Breda et al. 2009). The high depth/width<br />
ratio of <strong>the</strong> valley and <strong>the</strong> scattered boulders suggest<br />
relatively rapid <strong>in</strong>cision, with a m<strong>in</strong>imal lateral shift<strong>in</strong>g<br />
of <strong>the</strong> fluvial system (see Yoxall 1969; Wood et al. 1993)<br />
and with <strong>the</strong> stream competence significantly <strong>in</strong>creased by<br />
<strong>the</strong> topographic conf<strong>in</strong>ement (Schumm 1993). The valley<br />
<strong>in</strong>cision seems to have occurred concurrently with <strong>the</strong> late<br />
stages of <strong>the</strong> delta progradation, when <strong>the</strong> entrench<strong>in</strong>g<br />
fluvial system acted as a feeder for <strong>the</strong> youngest telescop<strong>in</strong>g<br />
parts of <strong>the</strong> delta (Figure 7a). The down-stepp<strong>in</strong>g pattern<br />
of delta topset (Figure 7b) strongly supports <strong>the</strong> notion of<br />
an <strong>in</strong>cremental fall of <strong>the</strong> delta shorel<strong>in</strong>e trajectory.<br />
The relatively narrow valley filled with fluvial deposits<br />
<strong>in</strong>dicates that <strong>the</strong> <strong>in</strong>fill<strong>in</strong>g of <strong>the</strong> valley was relatively rapid,<br />
under a high rate of sediment supply, with little lateral<br />
wander<strong>in</strong>g of <strong>the</strong> river and no significant valley-side<br />
collapses at <strong>the</strong> sea-level lowstand stage.<br />
ILGAR et al. / Turkish J Earth Sci<br />
Figure 5. An oblique transverse section through <strong>the</strong> Muratlı delta, <strong>Adana</strong> Bas<strong>in</strong>, show<strong>in</strong>g a gravel-filled axial fluvial valley deeply<br />
<strong>in</strong>cised <strong>in</strong> <strong>the</strong> delta deposits. Palaeotransport direction is away from <strong>the</strong> viewer, obliquely to <strong>the</strong> right. Picture from locality 2 <strong>in</strong><br />
Figure 1c.<br />
6. Sequence-stratigraphic <strong>in</strong>terpretation<br />
The late Tortonian shorel<strong>in</strong>e of <strong>the</strong> bas<strong>in</strong> is represented<br />
by <strong>the</strong> reefal limestones of <strong>the</strong> Tırtar Formation, which<br />
were superimposed directly on <strong>the</strong> earlier bas<strong>in</strong>-marg<strong>in</strong><br />
limestones of <strong>the</strong> Karaisalı Formation (Figure 2) and were<br />
later extensively eroded (Figure 1c). The 3 deltas <strong>in</strong> <strong>the</strong>ir<br />
location appear to have been offset bas<strong>in</strong>wards by ~25 km<br />
with respect to <strong>the</strong> late Tortonian shorel<strong>in</strong>e and emplaced<br />
directly onto <strong>the</strong> offshore mudstones of <strong>the</strong> Handere<br />
Formation, which <strong>in</strong>dicates a <strong>forced</strong>-regressive erosional<br />
shift of <strong>the</strong> shorel<strong>in</strong>e.<br />
A <strong>forced</strong> regression is <strong>in</strong>dicated by <strong>the</strong> downstepp<strong>in</strong>g<br />
geometry of <strong>the</strong> delta topset (Figure 7b), <strong>the</strong> cl<strong>in</strong>oformal<br />
foreset wedges that sharply downlapped <strong>the</strong> bas<strong>in</strong> floor<br />
(Figures 4a and 6), and fur<strong>the</strong>r by <strong>the</strong> <strong>in</strong>cision of fluvial<br />
valley along <strong>the</strong> delta axis (Figures 5 and 7a). The sharp,<br />
erosional basal surface of <strong>the</strong> delta marks an abrupt<br />
facies change and passes bas<strong>in</strong>wards <strong>in</strong>to a correlative<br />
depositional conformity (Figure 7a). The aggradational<br />
<strong>in</strong>fill<strong>in</strong>g of <strong>the</strong> <strong>in</strong>cised valley documents a subsequent rise<br />
of relative sea level, and <strong>the</strong> overly<strong>in</strong>g gypsiferous deposits<br />
<strong>in</strong>dicate a brief drown<strong>in</strong>g of <strong>the</strong> deltas. The evaporites<br />
occur as erosional relics of <strong>the</strong> latest mar<strong>in</strong>e deposits<br />
(HST) <strong>in</strong> <strong>the</strong> bas<strong>in</strong>, which implies yet ano<strong>the</strong>r subsequent<br />
<strong>forced</strong> regression (see <strong>the</strong> late <strong>Mess<strong>in</strong>ian</strong> erosional FRST<br />
<strong>in</strong> Figure 2).<br />
The Tortonian–<strong>Mess<strong>in</strong>ian</strong> deposits of <strong>the</strong> Kuzgun<br />
and Handere formations (Figure 2) have previously been<br />
<strong>in</strong>terpreted as a simple regressive succession (Yetiş 1988;<br />
Yetiş et al. 1995), which would imply a normal-regressive
Figure 6. Simplified vertical profile of <strong>the</strong> bottomset part of <strong>the</strong><br />
one of <strong>the</strong> Muratlı delta wedges, show<strong>in</strong>g <strong>the</strong> pattern of sediment<br />
sampl<strong>in</strong>g for biostratigraphic analysis. The dots numbered 1–24<br />
<strong>in</strong>dicate <strong>the</strong> location of samples. Log from locality 2 <strong>in</strong> Figure 1c.<br />
HST. The present study <strong>in</strong>dicates that this sedimentary<br />
succession, <strong>in</strong> reality, bears a high-resolution record of<br />
several major sea-level changes <strong>in</strong> <strong>the</strong> bas<strong>in</strong> and comprises<br />
2 stratigraphic sequences bounded by <strong>the</strong> erosional<br />
surfaces of <strong>forced</strong> regression. The follow<strong>in</strong>g <strong>in</strong>terpretive<br />
stratigraphic scenario is suggested (Figure 2):<br />
• The Kuzgun Formation represents a <strong>forced</strong> regression<br />
that is recognisable around <strong>the</strong> Mediterranean and<br />
attributed to <strong>the</strong> end-Serravalian (Tor-1) eustatic fall <strong>in</strong> sea<br />
level (Haq et al. 1988; Haq 1991); <strong>the</strong> formation’s erosional<br />
basal part is an erosional FRST, whereas <strong>the</strong> bulk of <strong>the</strong><br />
formation comprises a LST and possibly <strong>the</strong> earliest TST.<br />
• The ma<strong>in</strong> Tortonian part of <strong>the</strong> overly<strong>in</strong>g Handere<br />
Formation and <strong>the</strong> coeval Tırtar Formation (bas<strong>in</strong>-marg<strong>in</strong><br />
reefal platform) constitute a TST, record<strong>in</strong>g <strong>the</strong> subsequent<br />
eustatic sea-level rise (Haq et al. 1988; Haq 1991). Bas<strong>in</strong><br />
subsidence may have enhanced this mar<strong>in</strong>e transgression.<br />
• The upper part of <strong>the</strong> Handere Formation, with<br />
its isolated deltaic members, might have commenced<br />
its deposition as a normal-regressive HST, but <strong>the</strong>re is<br />
ILGAR et al. / Turkish J Earth Sci<br />
no facies evidence to support this notion. The lack of a<br />
recognisable HST suggests that <strong>the</strong> transgression was<br />
<strong>in</strong>terrupted by a relative sea-level fall, which would mean<br />
a TST overla<strong>in</strong> directly by a depositional FRST. This<br />
stratigraphic configuration of systems tracts may <strong>in</strong>dicate<br />
a eustatic transgression term<strong>in</strong>ated by a tectonically <strong>forced</strong><br />
stepwise regression.<br />
• The sharp base of <strong>the</strong> deltaic members and coeval<br />
littoral deposits of <strong>the</strong> Handere Formation (Figure 7a) is<br />
a regressive surface of mar<strong>in</strong>e erosion (Pl<strong>in</strong>t 1988; Pl<strong>in</strong>t<br />
& Nummedal 2000), expectedly pass<strong>in</strong>g bas<strong>in</strong>wards <strong>in</strong>to<br />
a correlative conformity (MacEachern et al. 1999). This<br />
surface was develop<strong>in</strong>g <strong>in</strong>crementally dur<strong>in</strong>g <strong>the</strong> entire<br />
time of <strong>the</strong> stepwise relative sea-level fall and hence is<br />
probably diachronous (Embry 2002).<br />
• The sharp-based gravelly deltas and coeval shallowmar<strong>in</strong>e<br />
deposits would thus represent a depositional <strong>forced</strong><br />
regression (Pl<strong>in</strong>t 1988; Helland-Hansen & Gjelberg 1994;<br />
Pl<strong>in</strong>t & Nummedal 2000). The bas<strong>in</strong>ward advance of <strong>the</strong><br />
deltas (FRST and LST) was followed by a relative sea-level<br />
rise (TST), when <strong>the</strong> <strong>in</strong>cised valleys were filled with fluvial<br />
deposits and <strong>the</strong> deltas were shallowly drowned with an<br />
abrupt landward shift of <strong>the</strong> shorel<strong>in</strong>e and river outlets.<br />
• The mar<strong>in</strong>e transgression brought an almost<br />
immediate deposition of evaporites (HST), which suggests<br />
flood<strong>in</strong>g by hypersal<strong>in</strong>e sea water (Figure 7b). The <strong>Adana</strong><br />
Bas<strong>in</strong> was subsequently emerged and its gypsiferous<br />
deposits were extensively eroded due to ano<strong>the</strong>r <strong>forced</strong><br />
regression (<strong>the</strong> late <strong>Mess<strong>in</strong>ian</strong> FRST, Figure 2). The<br />
evaporitic Gökkuyu Member of <strong>the</strong> uppermost Handere<br />
Formation (Figure 2) is sparsely preserved <strong>in</strong> <strong>the</strong> nor<strong>the</strong>rn<br />
part of <strong>the</strong> bas<strong>in</strong>, but its thickness reaches a few hundred<br />
metres <strong>in</strong> <strong>the</strong> sou<strong>the</strong>rn part and exceeds 1 km <strong>in</strong> <strong>the</strong><br />
adjo<strong>in</strong><strong>in</strong>g <strong>in</strong>ner Cilicia Bas<strong>in</strong> (Aksu et al. 2005; Burton-<br />
Ferguson et al. 2005). It can thus be precluded that <strong>the</strong>se<br />
evaporates are local deposits, formed <strong>in</strong> an isolated coastal<br />
lagoon or sabkha.<br />
It would <strong>the</strong>n appear that 2 consecutive <strong>forced</strong><br />
<strong>regressions</strong> occurred <strong>in</strong> <strong>the</strong> <strong>Adana</strong> Bas<strong>in</strong> <strong>in</strong> <strong>the</strong> <strong>Mess<strong>in</strong>ian</strong><br />
time, <strong>the</strong> first depositional and possibly <strong>forced</strong> by tectonics<br />
and <strong>the</strong> next erosional and probably eustatic. The key issue<br />
<strong>in</strong> this hypo<strong>the</strong>tical scenario is <strong>the</strong> exact tim<strong>in</strong>g and actual<br />
causes of <strong>the</strong> 2 <strong>regressions</strong>, which apparently followed<br />
each o<strong>the</strong>r closely.<br />
7. Biostratigraphic dat<strong>in</strong>g<br />
The heterolithic, f<strong>in</strong>e-gra<strong>in</strong>ed bottomset deposits of <strong>the</strong><br />
best-exposed Muratlı delta have been systematically<br />
sampled (Figure 6) to estimate <strong>the</strong> time of <strong>the</strong> delta<br />
progradation. The samples of mudstone and silty mudstone<br />
layers were disaggregated <strong>in</strong> a 30% hydrogen peroxide<br />
solution and washed over 63-, 125-, and 425-µm sieves.<br />
In total, 24 samples have been analysed (Figure 6), with a<br />
focus on planktonic foram<strong>in</strong>ifera.<br />
11
Planktonic foram<strong>in</strong>ifera occur throughout <strong>the</strong> studied<br />
section, except for 3 samples from its uppermost part<br />
(samples 18, 21, and 22 <strong>in</strong> Figure 6). The abundance of<br />
foram<strong>in</strong>ifer assemblages varies from medium to low,<br />
whereas <strong>the</strong>ir diversity and degree of preservation are<br />
generally moderate to high. The lowermost part of <strong>the</strong><br />
section (samples 1–5) lacks age-diagnostic species and<br />
12<br />
A<br />
B<br />
reefal limestone<br />
Surface of <strong>forced</strong><br />
regression<br />
Relic evaporitic cover<br />
on term<strong>in</strong>al delta slope<br />
<strong>Mess<strong>in</strong>ian</strong> evaporites<br />
topset<br />
delta wedge<br />
ILGAR et al. / Turkish J Earth Sci<br />
Delta progradation direction<br />
step-down<br />
topset<br />
25 km<br />
step-down<br />
delta wedge<br />
sea-level fall<br />
topset<br />
delta wedge<br />
offshore<br />
mudstones<br />
Figure 7. (a) Schematic model for <strong>the</strong> downstepp<strong>in</strong>g <strong>forced</strong>-regressive progradation of <strong>the</strong> Muratlı delta with concurrent<br />
<strong>in</strong>cision of an axial fluvial valley; diagram not to scale. (b) Panoramic view of <strong>the</strong> Muratlı delta longitud<strong>in</strong>al outcrop show<strong>in</strong>g<br />
<strong>the</strong> downstepp<strong>in</strong>g pattern of cl<strong>in</strong>oformal foreset wedges towards <strong>the</strong> left (SSE direction); picture from locality 2 <strong>in</strong> Figure 1c.<br />
200 m<br />
shows an assemblage of benthic forams (with Ammonia sp.<br />
and Elphidium spp.), ech<strong>in</strong>id sp<strong>in</strong>es, gastropods, and rare<br />
specimens of Globoturborotalita, Globiger<strong>in</strong>a, Orbul<strong>in</strong>a,<br />
Globiger<strong>in</strong>ella, and Globiger<strong>in</strong>oides.<br />
Planktonic foram<strong>in</strong>ifer assemblages are most<br />
diversified <strong>in</strong> <strong>the</strong> middle part of <strong>the</strong> section (samples<br />
6–16, Figure 6), <strong>in</strong>clud<strong>in</strong>g Globorotalia suterae Catalano
a1<br />
d2<br />
i1<br />
a2<br />
ILGAR et al. / Turkish J Earth Sci<br />
i2<br />
l1 l2<br />
r<br />
o<br />
a3<br />
d3 e<br />
s<br />
m2<br />
Figure 8. Selected planktonic foram<strong>in</strong>ifera identified <strong>in</strong> <strong>the</strong> latest Miocene delta bottomset deposits <strong>in</strong> <strong>the</strong> <strong>Adana</strong> and Mut bas<strong>in</strong>s: (a1) Turborotalita multiloba (Romeo) <strong>in</strong><br />
spiral, (a2) umbilical, and (a3) side view, sample 20 from <strong>Adana</strong> Bas<strong>in</strong>; (b) Turborotalita qu<strong>in</strong>queloba (Natland) <strong>in</strong> umbilical view, sample 9 from <strong>Adana</strong> Bas<strong>in</strong>; (c) Tenuilell<strong>in</strong>ata<br />
angustiumbilicata (Bolli) <strong>in</strong> umbilical view, sample 5 from Mut Bas<strong>in</strong>; (d1) Neogloboquadr<strong>in</strong>a acostaensis (Blow) <strong>in</strong> umbilical view and (d3) <strong>in</strong> spiral view, sample 2 from Mut<br />
Bas<strong>in</strong>; (d2) Neogloboquadr<strong>in</strong>a acostaensis (Blow) <strong>in</strong> umbilical view, sample 6 from <strong>Adana</strong> Bas<strong>in</strong>; (e) Globiger<strong>in</strong>ita glut<strong>in</strong>ata (Egger) <strong>in</strong> umbilical view, sample 4 from Mut Bas<strong>in</strong>;<br />
(f) Globiger<strong>in</strong>ita uvula (Ehrenberg) <strong>in</strong> side view, sample 2 from Mut Bas<strong>in</strong>; (g) Catapsydrax parvulus Bolli <strong>in</strong> umbilical view, sample 4 from Mut Bas<strong>in</strong>; (h) Globiger<strong>in</strong>oides<br />
bollii Blow <strong>in</strong> umbilical view, sample 2 from Mut Bas<strong>in</strong>; (i1) Neogloboquadr<strong>in</strong>a cont<strong>in</strong>uosa (Blow) <strong>in</strong> spiral and (i2) umbilical view, samples 4 and 2 from Mut Bas<strong>in</strong>; (j1)<br />
Globoturborotalita woodi (Jenk<strong>in</strong>s) <strong>in</strong> spiral and (j2) umbilical view, sample 13 from <strong>Adana</strong> Bas<strong>in</strong>; (k) Globoturborotalita apertura (Cushman) <strong>in</strong> umbilical view, sample 13 from<br />
<strong>Adana</strong> Bas<strong>in</strong>; (l1) Neogloboquadr<strong>in</strong>a humerosa (Takayanagi & Saito) <strong>in</strong> spiral and (l2) umbilical view, samples 11 and 9 from <strong>Adana</strong> Bas<strong>in</strong>; (m1) Globorotalia suterae Catalano<br />
and Sprovieri <strong>in</strong> oblique and (m2) spiral view, sample 24 from <strong>Adana</strong> Bas<strong>in</strong>; (n) Globoturborotalita decoraperta (Takayanagi & Saito) <strong>in</strong> spiral view, sample 24 from <strong>Adana</strong><br />
Bas<strong>in</strong>; (o) Orbul<strong>in</strong>a universa d’Orbigny, sample 6 from <strong>Adana</strong> Bas<strong>in</strong>; (p) Globiger<strong>in</strong>oides bulloideus Crescenti <strong>in</strong> spiral view, sample 1 from Mut Bas<strong>in</strong>; (q) Globiger<strong>in</strong>a bulloides<br />
d’Orbigny <strong>in</strong> spiral view, sample 6 from <strong>Adana</strong> Bas<strong>in</strong>; (r) Globiger<strong>in</strong>ella obesa (Bolli) <strong>in</strong> umbilical view, sample 13 from <strong>Adana</strong> Bas<strong>in</strong>; (s) Orbul<strong>in</strong>a suturalis Brönnimann,<br />
sample 9 from <strong>Adana</strong> Bas<strong>in</strong>; (t) Globiger<strong>in</strong>ella siphonifera (d’Orbigny) <strong>in</strong> side view, sample 6 from <strong>Adana</strong> Bas<strong>in</strong>; and (u) Globiger<strong>in</strong>oides seigliei Bermudez and Bolli <strong>in</strong> spiral<br />
view, sample 3 from Mut Bas<strong>in</strong>. The scale bar is 75 µm <strong>in</strong> pictures a–d and 100 µm <strong>in</strong> pictures e–u.<br />
j1<br />
m1<br />
b<br />
t<br />
f<br />
j2<br />
p<br />
n<br />
c<br />
g<br />
u<br />
k<br />
q<br />
d1<br />
h<br />
13
14<br />
Age (Ma)<br />
6 6.033<br />
7<br />
8<br />
9<br />
10<br />
11<br />
ATNTS2004<br />
C3A<br />
C3B<br />
and Sprovieri, Globoturborotalita apertura (Cushman), G.<br />
nepen<strong>the</strong>s (Todd), G. decoraperta (Takayanagi & Saito), G.<br />
woodi (Jenk<strong>in</strong>s), Globiger<strong>in</strong>elloides bulloideus Crescenti,<br />
G. obliquus Bolli, G. trilobus (Reuss), G. quadrilobatus<br />
(d’Orbigny), Globiger<strong>in</strong>a bulloides d’Orbigny, G.<br />
falconensis Blow, Globiger<strong>in</strong>ella siphonifera (d’Orbigny),<br />
G. obesa (Bolli), Orbul<strong>in</strong>a suturalis Brönnimann, O.<br />
universa d’Orbigny, Neogloboquadr<strong>in</strong>a acostaensis Blow, N.<br />
humerosa Takayanagi & Saito, Dentoglobiger<strong>in</strong>a altispira<br />
altispira (Cushman & Jarvis), Turborotalita qu<strong>in</strong>queloba<br />
(Natland), Tenuitell<strong>in</strong>ata angustiumbilicata (Bolli), and<br />
Globiger<strong>in</strong>ita uvula (Ehrenberg) (Figure 8). The presence<br />
of Globorotalia suterae Catalano & Sprovieri is particularly<br />
important, because its first stratigraphic occurrence<br />
serves to identify <strong>the</strong> base of subzone MMi12b (i.e. <strong>the</strong><br />
Globorotalia suterae subzone of Iaccar<strong>in</strong>o 1985) and is<br />
astronomically dated to 7.81 Ma B.P. (Figure 9; Sprovieri<br />
et al. 1999; Lourens et al. 2004; Iaccar<strong>in</strong>o et al. 2007).<br />
The coeval occurrence of Globorotalia suterae Catalano<br />
& Sprovieri, Globiger<strong>in</strong>oides bulloideus Crescenti, and<br />
Globoturborotalita woodi (Jenk<strong>in</strong>s) allows this part of<br />
<strong>the</strong> section to be assigned to undifferentiated biozone<br />
MMi12b–MMi13a (Figure 9; D’Onofrio et al. 1975;<br />
Iaccar<strong>in</strong>o 1985; Iaccar<strong>in</strong>o et al. 2007). The lack of <strong>the</strong><br />
Globorotalia miotumida group (particularly Globorotalia<br />
Polarity<br />
Magneto<br />
zones<br />
C3<br />
7.140<br />
7.528<br />
C4<br />
8.699<br />
C4A<br />
9.779<br />
C5<br />
Period<br />
ILGAR et al. / Turkish J Earth Sci<br />
Chronostratigraphy<br />
N E O G E N E<br />
M I O C E N E<br />
Epoch<br />
L A T E<br />
Stage<br />
<strong>Mess<strong>in</strong>ian</strong><br />
7.246<br />
Tortonian<br />
Mediterranean<br />
planktonic<br />
foram<strong>in</strong>iferal<br />
biostratigraphy<br />
Nondist<strong>in</strong>ctive<br />
Zone<br />
MMi11<br />
MMi9<br />
Figure 9. Mediterranean planktonic foram<strong>in</strong>iferal biozones plotted aga<strong>in</strong>st <strong>the</strong><br />
ATNTS2004 magnetic chronostratigraphy, with <strong>the</strong> stratigraphic distribution of<br />
diagnostic species <strong>in</strong> <strong>the</strong> outcrop section sampled <strong>in</strong> <strong>the</strong> <strong>Adana</strong> Bas<strong>in</strong> (Figure 6).<br />
MMi12 MMi13<br />
MMi10<br />
c<br />
b<br />
a<br />
b<br />
a<br />
Globoturborotalita woodi<br />
Globiger<strong>in</strong>oides bulloideus<br />
Globorotalia suterae<br />
Neogloboquadr<strong>in</strong>a humerosa<br />
Globiger<strong>in</strong>ella siphonifera<br />
conomiozea Kennett, G. sahel<strong>in</strong>a Catalano & Sprovieri,<br />
G. mediterranea Catalano & Sprovieri, and G. miotumida<br />
Jenk<strong>in</strong>s) <strong>in</strong> <strong>the</strong> samples does not permit a more precise<br />
assignment. O<strong>the</strong>r fauna <strong>in</strong> this part of <strong>the</strong> section <strong>in</strong>cludes<br />
scarce Bulim<strong>in</strong>a ech<strong>in</strong>ata d’Orbigny, representatives<br />
of Uviger<strong>in</strong>a and Bulim<strong>in</strong>a, miliolids, ech<strong>in</strong>id sp<strong>in</strong>es,<br />
gastropods, and bivalves.<br />
Sample 18 (Figure 6) bears no planktonic foram<strong>in</strong>ifers,<br />
but conta<strong>in</strong>s some benthic forms, gastropods, bivalves,<br />
and o<strong>the</strong>r shell fragments. The slightly higher sample 20<br />
(Figure 6) shows a planktonic foram<strong>in</strong>ifer assemblage<br />
that consists almost entirely of Turborotalita multiloba<br />
(Romeo), T. qu<strong>in</strong>queloba (Natland), and Tenuitell<strong>in</strong>ata<br />
angustiumbilicata (Bolli), accompanied by Bulim<strong>in</strong>a<br />
ech<strong>in</strong>ata d’Orbigny, miliolids, and ech<strong>in</strong>id sp<strong>in</strong>es. These<br />
foram species are known to have been most common prior<br />
to <strong>the</strong> deposition of <strong>the</strong> <strong>Mess<strong>in</strong>ian</strong> Lower Evaporites <strong>in</strong> <strong>the</strong><br />
Mediterranean Sea (Kouwenhoven et al. 2006; Manzi et<br />
al. 2007; Morigi et al. 2007; Iaccar<strong>in</strong>o et al. 2008; Orszag-<br />
Sperber et al. 2009; Di Stefano et al. 2010). Fur<strong>the</strong>rmore,<br />
Turborotalita multiloba (Romeo) is an important marker<br />
species <strong>in</strong> <strong>the</strong> Mediterranean, because its narrow<br />
stratigraphic range shortly predates <strong>the</strong> deposition of <strong>the</strong><br />
Lower Evaporites (D’Onofrio et al. 1975; Iaccar<strong>in</strong>o 1985).<br />
The first brief <strong>in</strong>flux of this taxon is dated to 6.42 Ma B.P.,<br />
Turborotalita multiloba
A<br />
5<br />
4<br />
Middle <strong>Mess<strong>in</strong>ian</strong><br />
ILGAR et al. / Turkish J Earth Sci<br />
NW SE<br />
6 Late <strong>Mess<strong>in</strong>ian</strong><br />
3<br />
2<br />
1<br />
N<br />
Inner<br />
Cilicia Bas<strong>in</strong><br />
Gökkuyu Mb. evaporites<br />
Latest Tortonian–early <strong>Mess<strong>in</strong>ian</strong><br />
Early <strong>Mess<strong>in</strong>ian</strong> erosional unconformity (<strong>forced</strong> regression)<br />
Gravelly deltaic member of Handere F.<br />
(cross-cut by <strong>in</strong>cised fluvial valley)<br />
Handere Fm. Misis High rises<br />
as a pop-up ridge<br />
Tortonian<br />
Late Burdigalian–Serravalian<br />
Karaisalı Fm.<br />
2.0<br />
0.5<br />
1.0<br />
2.5<br />
Late Aquitanian–early Burdigalian<br />
1.5<br />
3.0<br />
3.5<br />
4.0<br />
<strong>Adana</strong><br />
Bas<strong>in</strong><br />
Cross-section l<strong>in</strong>e<br />
C<strong>in</strong>göz Fm. - Güvenç Fm.<br />
Kaplankaya Fm.<br />
Base-Miocene erosional unconformity Gildirli Fm.<br />
0 km 50<br />
Present-day erosional<br />
marg<strong>in</strong> of Miocene bas<strong>in</strong><br />
(outcrop limit)<br />
37 00'N<br />
Modern shorel<strong>in</strong>e<br />
İskenderun<br />
Bas<strong>in</strong><br />
35 00'E 36 00'E<br />
B<br />
Late <strong>Mess<strong>in</strong>ian</strong> erosional unconformity (<strong>forced</strong> regression)<br />
Early Tortonian erosional unconformity<br />
Tırtar Fm. Handere Fm.<br />
Kuzgun Fm.<br />
Proto-Misis High<br />
Figure 10. (a) The relationship of <strong>Adana</strong> Bas<strong>in</strong> to adjacent structural units, with a seismic map of <strong>the</strong> base-Miocene unconformity <strong>in</strong> <strong>the</strong> bas<strong>in</strong> (depths below sea level<br />
<strong>in</strong> seconds of 2-way travel time); modified from Burton-Ferguson et al. (2005, Fig. 8). Note <strong>the</strong> trough-shaped, SW-plung<strong>in</strong>g bas<strong>in</strong>-floor palaeotopography and <strong>the</strong> high<br />
palaeotopographic relief along <strong>the</strong> bas<strong>in</strong>’s eastern marg<strong>in</strong> (Misis High). The NW–SE cross-section l<strong>in</strong>e perta<strong>in</strong>s to <strong>the</strong> cartoon below. (b) Schematic cartoon show<strong>in</strong>g <strong>the</strong><br />
<strong>in</strong>terpreted Miocene tectono-stratigraphic development <strong>in</strong> <strong>the</strong> <strong>Adana</strong> Bas<strong>in</strong> (based on key features revealed by <strong>the</strong> seismic sections <strong>in</strong> Burton-Ferguson et al. 2005; not<br />
to scale). The successive stages are: 1– The Mesozoic bedrock of <strong>the</strong> Tauride foreland, affected by thrust<strong>in</strong>g and elevated <strong>in</strong> <strong>the</strong> Eocene, is gradually denudated by erosion<br />
and eventually covered with alluvial deposits <strong>in</strong> <strong>the</strong> late Aquitanian to early Burdigalian; 2– The area becomes a foreland shelf zone as a result of mid-Burdigalian mar<strong>in</strong>e<br />
transgression, which drowns <strong>the</strong> bas<strong>in</strong> and is followed by a late Burdigalian to Serravalian normal regression; 3– The bas<strong>in</strong> is emerged by early Tortonian eustatic sea-level fall,<br />
and <strong>the</strong> result<strong>in</strong>g erosional unconformity is covered with alluvial deposits and <strong>the</strong>n drowned by mar<strong>in</strong>e transgression; 4– Orogenic thrust<strong>in</strong>g <strong>in</strong> <strong>the</strong> latest Tortonian to early<br />
<strong>Mess<strong>in</strong>ian</strong> converts <strong>the</strong> bas<strong>in</strong> <strong>in</strong>to a piggyback feature, with <strong>the</strong> thrust-<strong>in</strong>duced uplift caus<strong>in</strong>g a <strong>forced</strong> regression and progradation of Gilbert-type deltas <strong>in</strong>cised by fluvial<br />
valleys; 5– The foreland subsides under <strong>the</strong> <strong>in</strong>creased load of <strong>the</strong> orogen thrust-sheets, which <strong>in</strong>vites a mar<strong>in</strong>e transgression that br<strong>in</strong>gs <strong>in</strong> hypersal<strong>in</strong>e water; and 6– The bas<strong>in</strong><br />
is emerged and subject to erosion due to <strong>the</strong> late <strong>Mess<strong>in</strong>ian</strong> evaporative drawdown of <strong>the</strong> Mediterranean Sea. Post-Miocene extensional deformation not considered.<br />
37 30'N<br />
36 30'N<br />
15
with<strong>in</strong> subzone MMi13b, before its common occurrence<br />
<strong>in</strong> subzone MMi13c (Sierro et al. 2001; Dr<strong>in</strong>ia et al. 2004;<br />
Lourens et al. 2004; Kouwenhoven et al. 2006; Manzi et<br />
al. 2007). The higher samples show no occurrence of<br />
Turborotalita multiloba (Romeo) and <strong>the</strong> stratigraphic<br />
level of sample 20 is thus tentatively assigned to subzone<br />
MMi13b (Figure 9).<br />
Samples 21 and 22 (Figure 6) bear no planktonic<br />
foram<strong>in</strong>ifera and conta<strong>in</strong> miliolids, gastropods, ostracods,<br />
and ech<strong>in</strong>id sp<strong>in</strong>es. Sample 24 from <strong>the</strong> top of <strong>the</strong> section<br />
is rich <strong>in</strong> planktonic foram<strong>in</strong>ifera (Globorotalia suterae<br />
Catalano & Sprovieri, Globoturborotalita apertura<br />
(Cushman), G. nepen<strong>the</strong>s (Todd), G. decoraperta<br />
(Takayanagi & Saito), Neogloboquadr<strong>in</strong>a acostaensis<br />
(Blow), N. humerosa (Takayanagi & Saito), Globiger<strong>in</strong>a<br />
bulloides d’Orbigny, Orbul<strong>in</strong>a universa d’Orbigny,<br />
16<br />
ILGAR et al. / Turkish J Earth Sci<br />
Figure 11. Schematic <strong>in</strong>terpretation of <strong>the</strong> latest Miocene relative sea-level changes <strong>in</strong> <strong>the</strong> <strong>Adana</strong> Bas<strong>in</strong> (cf. Figure 2); <strong>the</strong><br />
suggested time <strong>in</strong>tervals are based on biostratigraphic dat<strong>in</strong>g. (a) The late Tortonian tectonic thrust<strong>in</strong>g lifts up <strong>the</strong> bas<strong>in</strong> and<br />
forces a gradual regression with <strong>the</strong> deposition of downstepp<strong>in</strong>g Gilbert-type deltas <strong>in</strong> FRST. (b) The postthrust<strong>in</strong>g foreland<br />
subsidence due to crustal load results <strong>in</strong> shallow reflood<strong>in</strong>g of <strong>the</strong> bas<strong>in</strong> by hypersal<strong>in</strong>e water, with evaporitic TST and HST. (c)<br />
The Mediterranean early evaporative drawdown causes <strong>the</strong> second eustatically <strong>forced</strong> and nondepositional regression (FRST)<br />
<strong>in</strong> <strong>the</strong> bas<strong>in</strong>.<br />
O. suturalis Brönnimann, O. bilobata d’Orbigny, and<br />
Globiger<strong>in</strong>ella siphonifera (d’Orbigny); Figure 8) and also<br />
conta<strong>in</strong>s benthic foram<strong>in</strong>ifers (Ammonia sp., Bulim<strong>in</strong>a<br />
ech<strong>in</strong>ata d’Orbigny, and some miliolids and nodosarids),<br />
gastropods, bivalves, and ech<strong>in</strong>id sp<strong>in</strong>es. However, it<br />
lacks Turborotalita multiloba (Romeo), Globiger<strong>in</strong>oides<br />
bulloideus Crescenti, and Globoturborotalita woodi<br />
(Jenk<strong>in</strong>s), which allows this stratigraphic level to be also<br />
assigned to subzone MMi13b (Figure 9).<br />
8. Discussion<br />
8.1. Interpretation of Miocene events <strong>in</strong> <strong>the</strong> <strong>Adana</strong> Bas<strong>in</strong><br />
In this section, <strong>the</strong> chronology and regional causes of<br />
<strong>the</strong> late Miocene relative sea-level changes <strong>in</strong> <strong>the</strong> <strong>Adana</strong><br />
Bas<strong>in</strong> are discussed with reference to <strong>the</strong> bas<strong>in</strong>’s tectonic<br />
development <strong>in</strong>terpreted from multichannel seismic
A<br />
B<br />
1 m<br />
sections by Burton-Ferguson et al. (2005). However, <strong>the</strong><br />
chronostratigraphy of tectonic events suggested by <strong>the</strong>se<br />
latter authors needs to be rectified <strong>in</strong> <strong>the</strong> light of outcropderived<br />
biostratigraphic data. The ma<strong>in</strong> corrections are as<br />
follows:<br />
• The Güvenç Formation was considered by Burton-<br />
Ferguson et al. (2005, Fig. 3) to be of a Langhian to end-<br />
Tortonian age, whereas <strong>in</strong> reality it is no younger than<br />
Serravalian, truncated by <strong>the</strong> base-Tortonian erosional<br />
unconformity (Figure 2). The time-span of <strong>the</strong> Güvenç<br />
Formation is <strong>the</strong> same as that of <strong>the</strong> C<strong>in</strong>göz Formation,<br />
which is its <strong>near</strong>shore time-equivalent.<br />
• The Kuzgun Formation was considered by Burton-<br />
Ferguson et al. (2005, Fig. 3) to be Tortonian to earliest<br />
<strong>Mess<strong>in</strong>ian</strong> <strong>in</strong> age, whereas <strong>in</strong> reality this terrestrial<br />
formation is of an earliest Tortonian age, covered<br />
transgressively by <strong>the</strong> mar<strong>in</strong>e Handere Formation whose<br />
basal part bears planktonic forams of zone MMi10 and<br />
nannofossils of <strong>the</strong> uppermost zone MNN7c (Figure 2).<br />
• The Handere Formation was considered by Burton-<br />
Ferguson et al. (2005, Fig. 3) to be of a Pliocene age and<br />
overly<strong>in</strong>g <strong>Mess<strong>in</strong>ian</strong> evaporites, whereas its actual age is<br />
Tortonian to <strong>Mess<strong>in</strong>ian</strong> and <strong>the</strong> <strong>Mess<strong>in</strong>ian</strong> evaporites<br />
occur at its top (Figure 2).<br />
ILGAR et al. / Turkish J Earth Sci<br />
C<br />
1 m 1 m<br />
Figure 12. (a) Late Miocene shallow-mar<strong>in</strong>e deposits folded by compressional tectonic deformation at <strong>the</strong> <strong>in</strong>ner<br />
marg<strong>in</strong> of <strong>the</strong> <strong>Adana</strong> Bas<strong>in</strong>; picture from locality 4 <strong>in</strong> Figure 1b. (b, c) The exhumed planes of extensional normal<br />
faults <strong>in</strong> Miocene limestones at <strong>the</strong> <strong>in</strong>ner marg<strong>in</strong> of <strong>the</strong> Mut Bas<strong>in</strong>; picture from locality 5 and <strong>in</strong> Figure 1b.<br />
SE<br />
Accord<strong>in</strong>gly, <strong>the</strong> tim<strong>in</strong>g of <strong>the</strong> Miocene events <strong>in</strong> <strong>the</strong><br />
bas<strong>in</strong> <strong>in</strong> our <strong>in</strong>terpretation, summarised <strong>in</strong> Figure 10,<br />
differs slightly from <strong>the</strong> chronology suggested by Burton-<br />
Ferguson et al. (2005).<br />
The seismic data <strong>in</strong>dicate that <strong>the</strong> Miocene bas<strong>in</strong> was<br />
<strong>in</strong>itially a trough plung<strong>in</strong>g towards <strong>the</strong> SW and pass<strong>in</strong>g<br />
<strong>in</strong>to <strong>the</strong> Cilicia Bas<strong>in</strong> (Figure 10a). The <strong>in</strong>cipient Misis<br />
Structural High was probably a low-relief horst (Figure 10b;<br />
see Aksu et al. 2005, Fig. 8), perhaps shallowly submerged.<br />
Progressive unconformities on its flanks (Burton-Ferguson<br />
et al. 2005, Fig. 9) <strong>in</strong>dicate that it became gradually elevated<br />
by differential subsidence dur<strong>in</strong>g <strong>the</strong> Langhian–Tortonian<br />
and eventually popped up as a northward extension of<br />
<strong>the</strong> Kyrenia fold-and-thrust ridge <strong>in</strong> <strong>the</strong> latest Tortonian<br />
to early <strong>Mess<strong>in</strong>ian</strong> time (see Aksu et al. 2005, Fig. 12),<br />
when <strong>the</strong> Miocene succession also evidently underwent<br />
thrust<strong>in</strong>g (Figure 10b; see Burton-Ferguson et al. 2005,<br />
Figs. 14 & 15). This event is thought to have marked <strong>the</strong><br />
tectonic conversion of <strong>the</strong> Miocene <strong>Adana</strong> foredeep <strong>in</strong>to a<br />
thrust-soled piggyback bas<strong>in</strong> (Figure 10b).<br />
The biostratigraphic data <strong>in</strong>dicate that <strong>the</strong> <strong>forced</strong><br />
regression which formed <strong>the</strong> Gilbert-type deltas and<br />
caused fluvial valley <strong>in</strong>cision (Figure 11a) occurred <strong>in</strong><br />
<strong>the</strong> latest Tortonian to early <strong>Mess<strong>in</strong>ian</strong>, ~7.8 to 6.4 Ma<br />
17
B.P. (Figure 9), predat<strong>in</strong>g <strong>the</strong> <strong>Mess<strong>in</strong>ian</strong> early evaporative<br />
drawdown of <strong>the</strong> Mediterranean Sea (dated to 5.96 ±<br />
0.02 by Krijgsman et al. 1999). The cause of this stepwise<br />
and depositional <strong>forced</strong> regression is thought to have<br />
been <strong>the</strong> late Tortonian tectonic conversion of <strong>the</strong> <strong>Adana</strong><br />
foredeep shelf <strong>in</strong>to a thrust wedge-top (piggyback) bas<strong>in</strong>,<br />
as is also evidenced by <strong>the</strong> compressional deformation<br />
of late Miocene bas<strong>in</strong>-marg<strong>in</strong> deposits (Figure 12a).<br />
The tectonic thrust<strong>in</strong>g would likely cause a stepwise<br />
bas<strong>in</strong>-floor uplift and relative sea-level fall (Figure 7b).<br />
The biostratigraphically constra<strong>in</strong>ed time frame for<br />
18<br />
A<br />
15<br />
10<br />
5<br />
thickness (metres)<br />
0<br />
delta topset<br />
Delta foreset<br />
B<br />
30<br />
25<br />
20<br />
mudstone samples for<br />
planktonic foram<strong>in</strong>ifera<br />
Tırtar Fm.<br />
clay sand gravel<br />
silt<br />
ILGAR et al. / Turkish J Earth Sci<br />
delta foreset<br />
Delta topset<br />
coral and Miocene<br />
limestone blocks<br />
large coral<br />
fragments<br />
upslope-dipp<strong>in</strong>g<br />
backset deposits with<br />
large coral fragments<br />
Delta foreset<br />
bioturbated sandstones<br />
and oyster shells<br />
foreset direction<br />
C<br />
coral and reefal<br />
limestone fragments<br />
D<br />
backset<br />
coral<br />
fragments<br />
Figure 13. (a) Longitud<strong>in</strong>al outcrop section of <strong>the</strong> latest Tortonian Gilbert-type delta <strong>in</strong> <strong>the</strong> Mut Bas<strong>in</strong>. (b) Vertical sedimentological<br />
log of <strong>the</strong> delta deposits, show<strong>in</strong>g a coarsen<strong>in</strong>g-upwards coarse-gra<strong>in</strong>ed succession overly<strong>in</strong>g directly <strong>the</strong> Tırtar limestone. (c) Closeup<br />
view of <strong>the</strong> delta topset conglomerates, rich <strong>in</strong> pebble- to cobble-sized fragments of Miocene reefal limestones and corals. (d) A<br />
backset of upslope-dipp<strong>in</strong>g cross-strata with<strong>in</strong> <strong>the</strong> delta conglomeratic foreset. Pictures and log from locality 7 <strong>in</strong> Figure 1b.<br />
<strong>the</strong> regression thus gives a more accurate tim<strong>in</strong>g of this<br />
tectonic event <strong>in</strong> <strong>the</strong> <strong>Adana</strong> Bas<strong>in</strong> (cf. Burton-Ferguson et<br />
al. 2005).<br />
The formation of a piggyback bas<strong>in</strong> would signify<br />
<strong>the</strong> climax of <strong>the</strong> structural contraction and thicken<strong>in</strong>g<br />
of <strong>the</strong> orogen, which would normally be followed by a<br />
regulat<strong>in</strong>g flexural subsidence of <strong>the</strong> foreland under <strong>the</strong><br />
<strong>in</strong>creased crustal load (DeCelles & Giles 1996). Such an<br />
episode of postthrust<strong>in</strong>g isostatic subsidence is thought<br />
to have term<strong>in</strong>ated <strong>the</strong> bas<strong>in</strong>ward advance of <strong>the</strong> deltas<br />
(LST) and caused <strong>the</strong>ir shallow mar<strong>in</strong>e drown<strong>in</strong>g (TST)
<strong>in</strong> an estimated period between ~6.4 and ~6.0 Ma B.P.<br />
(Figure 11b). The mar<strong>in</strong>e highstand sedimentation (HST)<br />
was evaporitic, which <strong>in</strong>dicates flood<strong>in</strong>g by hypersal<strong>in</strong>e<br />
water and thus suggests that <strong>the</strong> hypersal<strong>in</strong>ity <strong>in</strong> <strong>the</strong><br />
eastern Mediterranean Sea was reached at least ~6.5<br />
Ma B.P. The deposition of gypsiferous HST was term<strong>in</strong>ated<br />
by <strong>the</strong> regional onset of <strong>the</strong> early evaporative drawdown <strong>in</strong><br />
<strong>the</strong> Mediterranean Sea ~6 Ma B.P. (Krijgsman et al. 1999),<br />
which caused <strong>the</strong> second, erosional <strong>forced</strong> <strong>Mess<strong>in</strong>ian</strong><br />
regression <strong>in</strong> <strong>the</strong> <strong>Adana</strong> Bas<strong>in</strong> (Figure 11c).<br />
The early evaporative drawdown <strong>in</strong> <strong>the</strong> Mediterranean<br />
Sea might not exceed 200 m (Dronkert 1985; Krijgsman<br />
et al. 1999), but it was more than sufficient to emerge <strong>the</strong><br />
shallow-mar<strong>in</strong>e peripheral bas<strong>in</strong>. Dur<strong>in</strong>g <strong>the</strong> ensu<strong>in</strong>g<br />
desiccation of <strong>the</strong> Mediterranean Sea, <strong>the</strong> postorogenic<br />
regional isostatic uplift (Jaffey & Robertson 2005;<br />
Cosent<strong>in</strong>o et al. 2012) had apparently elevated <strong>the</strong> <strong>Adana</strong><br />
Bas<strong>in</strong> sufficiently high to prevent its reflood<strong>in</strong>g by <strong>the</strong><br />
Zanclean regional transgression dated to 5.3 Ma B.P.<br />
The bas<strong>in</strong> thus rema<strong>in</strong>ed terrestrial and accumulated<br />
a succession of Pliocene–Quaternary fluvial terraces<br />
(Figure 2) <strong>in</strong> response to <strong>the</strong> cont<strong>in</strong>u<strong>in</strong>g uplift of <strong>the</strong><br />
Taurides comb<strong>in</strong>ed with concurrent eustatic sea-level<br />
changes (Haq et al. 1988).<br />
8.2. Comparison with <strong>the</strong> Mut Bas<strong>in</strong><br />
The end-Serravalian fall and rise of relative sea level<br />
recorded <strong>in</strong> <strong>the</strong> <strong>Adana</strong> Bas<strong>in</strong> (Figure 2) are also well<br />
recognisable <strong>in</strong> <strong>the</strong> o<strong>the</strong>r Mediterranean peripheral bas<strong>in</strong>s<br />
of sou<strong>the</strong>rn Turkey (Kell<strong>in</strong>g et al. 2005), such as <strong>the</strong><br />
adjacent Mut-Ermenek Bas<strong>in</strong> (Atabey et al. 2000; Ilgar &<br />
Nemec 2005) and <strong>the</strong> Antalya Bas<strong>in</strong> far<strong>the</strong>r to <strong>the</strong> west<br />
(Figure 1a; Flecker et al. 1995; Karabıyıkoğlu et al. 2000;<br />
Deynoux et al. 2005; Monod et al. 2006; Ç<strong>in</strong>er et al. 2008).<br />
An array of fan deltas prograded and became drowned<br />
<strong>in</strong> <strong>the</strong> Antalya Bas<strong>in</strong> at that time (Larsen 2003), whereas<br />
an <strong>in</strong>cised fluvial valley filled with a Gilbert-type delta,<br />
stratigraphically equivalent to <strong>the</strong> Kuzgun Formation <strong>in</strong><br />
<strong>the</strong> <strong>Adana</strong> Bas<strong>in</strong> (Figure 2), separates <strong>the</strong> amalgamated<br />
Burdigalian–Serravalian and Tortonian reefal platforms <strong>in</strong><br />
<strong>the</strong> Ermenek Bas<strong>in</strong> (Ilgar et al. unpublished data). The great<br />
amplitude of this early Tortonian eustatic cycle (see Haq et<br />
al. 1988) rendered it widely recognisable and correlative.<br />
However, <strong>the</strong> subsequent relative sea-level changes that<br />
occurred <strong>in</strong> <strong>the</strong>se peripheral bas<strong>in</strong>s <strong>in</strong> Tortonian over a<br />
period of <strong>near</strong>ly 4 Ma are by no means correlative.<br />
In contrast to <strong>the</strong> <strong>Adana</strong> Bas<strong>in</strong>, <strong>the</strong> o<strong>the</strong>r peripheral<br />
bas<strong>in</strong>s formed as postorogenic <strong>in</strong>tramontane collapse<br />
depressions and <strong>the</strong>ir <strong>in</strong>dividual sedimentation history<br />
had recorded <strong>the</strong> <strong>in</strong>terplay between lower-amplitude<br />
eustatic cycles and <strong>the</strong> gradual isostatic uplift of <strong>the</strong><br />
orogen, local extensional tectonics and variable sediment<br />
supply. The gravelly deltas that formed <strong>in</strong> <strong>the</strong>se bas<strong>in</strong>s <strong>in</strong><br />
<strong>the</strong> Tortonian are ma<strong>in</strong>ly noncorrelative local sequences<br />
ILGAR et al. / Turkish J Earth Sci<br />
and parasequences. As an <strong>in</strong>structive example, we discuss<br />
here <strong>the</strong> development of a late Tortonian Gilbert-type<br />
delta <strong>in</strong> <strong>the</strong> <strong>near</strong>by Mut Bas<strong>in</strong> (Figure 13a; see locality <strong>in</strong><br />
Figure 1b).<br />
The late Tortonian deltaic deposits <strong>in</strong> <strong>the</strong> Mut<br />
Bas<strong>in</strong> belong to <strong>the</strong> shallow-mar<strong>in</strong>e Ballı Formation<br />
(stratigraphic equivalent of <strong>the</strong> Handere Formation <strong>in</strong> <strong>the</strong><br />
<strong>Adana</strong> Bas<strong>in</strong>, Figure 2) and overlie sharply an erosional<br />
ramp of <strong>the</strong> bas<strong>in</strong>-marg<strong>in</strong> reefal limestones of <strong>the</strong> Tırtar<br />
Formation. The Gilbert-type delta prograded from <strong>the</strong><br />
bas<strong>in</strong>’s nor<strong>the</strong>rn marg<strong>in</strong> towards <strong>the</strong> SSW and formed a<br />
coarsen<strong>in</strong>g-upwards clastic succession up to 30 m thick<br />
(Figure 13b). The delta’s fluvial topset has an erosional<br />
base and consists of coarse conglomerates and subord<strong>in</strong>ate<br />
sandstones, rich <strong>in</strong> pebble- to cobble-sized coral fragments<br />
and Miocene limestone debris (Figure 13c). The gravel is<br />
ma<strong>in</strong>ly angular to subangular and moderately sorted, with<br />
a clast-supported texture and a matrix of poorly sorted<br />
coarse sand and granules. F<strong>in</strong><strong>in</strong>g-upwards bedsets of planar<br />
parallel-stratified gravel, 40–90 cm thick, are thought to<br />
be multistorey palaeochannels of braided streams filled<br />
ma<strong>in</strong>ly by <strong>the</strong> deposition of longitud<strong>in</strong>al bars (Nemec<br />
& Postma 1993; Miall 1996). Nonstratified gravel beds<br />
relatively richer <strong>in</strong> sand matrix, with or without normal<br />
grad<strong>in</strong>g, are probably deposits of hyperconcentrated flows<br />
and debris flows generated by <strong>the</strong> sediment-sweep<strong>in</strong>g<br />
action of stream floods (Wasson 1977, 1979; Nemec &<br />
Muszyński 1982; Ridgway & DeCelles 1993).<br />
The erosional, oblique contact between <strong>the</strong> topset<br />
and foreset deposits (Figures 13a and 13b) <strong>in</strong>dicates a<br />
nonris<strong>in</strong>g trajectory of <strong>the</strong> delta shorel<strong>in</strong>e (Breda et al.<br />
2007), which may suggest a normal or a <strong>forced</strong> regression.<br />
Foreset beds are ma<strong>in</strong>ly tabular, 10–45 cm thick, and<br />
<strong>in</strong>cl<strong>in</strong>ed at up to 25°, composed of f<strong>in</strong>e- to very coarsegra<strong>in</strong>ed<br />
sandstones rich <strong>in</strong> granules and scattered pebbles<br />
of up to 4 cm <strong>in</strong> size. Scattered oyster shells and isolated<br />
burrows are also common. The beds have erosional bases<br />
and show plane-parallel stratification, with or without<br />
normal grad<strong>in</strong>g. Their tractional deposition is attributed to<br />
fully turbulent hyperpycnal flows, or river-generated lowdensity<br />
turbidity currents (sensu Lowe 1982). Among <strong>the</strong><br />
foreset beds are backsets of upslope-dipp<strong>in</strong>g cross-strata<br />
(Figures 13b and 13d), which occur as <strong>the</strong> <strong>in</strong>fill of deltaslope<br />
chutes, up to 250 cm deep. The chute-fill deposits are<br />
rich <strong>in</strong> large coral fragments and reefal limestone debris,<br />
up to 100 cm <strong>in</strong> size, derived from <strong>the</strong> bas<strong>in</strong>-marg<strong>in</strong><br />
Miocene carbonate platform. Delta bottomset consists of<br />
th<strong>in</strong> siltstone and f<strong>in</strong>e-gra<strong>in</strong>ed sandstone beds <strong>in</strong>tercalated<br />
with mudstones (Figure 13b).<br />
The delta, thus built out directly on a wave-cut<br />
carbonate ramp, shows an erosional topset/foreset contact<br />
and conta<strong>in</strong>s debris derived from denudation of <strong>the</strong> bas<strong>in</strong>marg<strong>in</strong><br />
reefal limestones. Fur<strong>the</strong>rmore, <strong>the</strong> delta <strong>in</strong> its distal<br />
19
part is covered with th<strong>in</strong>ly bedded reefal limestones, which<br />
<strong>in</strong>dicates a shallow drown<strong>in</strong>g, cessation of fluvial supply,<br />
and thus a considerable landward shift of <strong>the</strong> shorel<strong>in</strong>e.<br />
There are no younger mar<strong>in</strong>e deposits <strong>in</strong> <strong>the</strong> bas<strong>in</strong>, which<br />
implies its subsequent emergence. Taken toge<strong>the</strong>r, <strong>the</strong><br />
evidence <strong>in</strong>dicates a <strong>forced</strong> regression followed by limited<br />
mar<strong>in</strong>e reflood<strong>in</strong>g, and <strong>the</strong> delta’s association with <strong>the</strong><br />
upper part of <strong>the</strong> Tırtar Formation might thus render it<br />
correlative with <strong>the</strong> deltas <strong>in</strong> <strong>the</strong> <strong>Adana</strong> Bas<strong>in</strong>. In reality,<br />
<strong>the</strong> delta <strong>in</strong> <strong>the</strong> Mut Bas<strong>in</strong> is significantly older than <strong>the</strong><br />
deltas <strong>in</strong> <strong>the</strong> <strong>Adana</strong> Bas<strong>in</strong>, as evidenced by biostratigraphic<br />
data.<br />
The age of <strong>the</strong> deltaic deposits <strong>in</strong> <strong>the</strong> Mut Bas<strong>in</strong> has<br />
been determ<strong>in</strong>ed on <strong>the</strong> basis of planktonic foram<strong>in</strong>ifera<br />
<strong>in</strong> 10 mudstone samples from a vertical outcrop section<br />
of <strong>the</strong> delta bottomset deposits. Planktonic foram<strong>in</strong>ifera<br />
are abundant and well preserved, but show a relatively low<br />
to moderate diversity and are accompanied by benthic<br />
foram<strong>in</strong>ifers (representatives of Ammonia, Elphidium,<br />
Bulim<strong>in</strong>a, Boliv<strong>in</strong>a, Uviger<strong>in</strong>a, Nonion, miliolids, and<br />
nodosarids), gastropods, bivalves, ostracods, and<br />
ech<strong>in</strong>id sp<strong>in</strong>es. The dom<strong>in</strong>ant planktonic species are<br />
Globiger<strong>in</strong>a and Globiger<strong>in</strong>oides, accompanied by<br />
abundant globoturborotalids, neogloboquadr<strong>in</strong>ids, and<br />
orbul<strong>in</strong>ids. All samples consistently conta<strong>in</strong> Globiger<strong>in</strong>a<br />
bulloides d’Orbigny, Globiger<strong>in</strong>oides trilobus (Reuss), G.<br />
quadrilobatus (d’Orbigny), G. obliquus Bolli, G. bulloideus<br />
Crescenti, Globiger<strong>in</strong>ella obesa (Bolli), Neogloboquadr<strong>in</strong>a<br />
acostaensis (Blow), N. cont<strong>in</strong>uosa (Blow), and<br />
Globoturborotalita woodi (Jenk<strong>in</strong>s). Species that are less<br />
consistently present or rare <strong>in</strong>clude Globoturborotalita<br />
decoraperta (Takayanagi & Saito), Tenuitell<strong>in</strong>ata<br />
angustiumbilicata (Bolli), Catapsydrax parvulus Bolli,<br />
Loeblich & Tappan, Globorotalia scitula (Brady),<br />
Globiger<strong>in</strong>ita uvula (Ehrenberg), Globiger<strong>in</strong>ita <strong>in</strong>crusta<br />
Akers, G. glut<strong>in</strong>ata (Egger), and Globiger<strong>in</strong>oides seigliei<br />
Bermudez & Bolli. The majority are long-range species,<br />
but <strong>the</strong> cooccurrence of Neogloboquadr<strong>in</strong>a cont<strong>in</strong>uosa<br />
(Blow), N. acostaensis (Blow), Globiger<strong>in</strong>oides bollii Blow,<br />
and G. seigliei Bermudez & Bolli <strong>in</strong>dicates a Tortonian age<br />
of <strong>the</strong> deposits. The cooccurrence of <strong>the</strong>se last 3 species<br />
suggests an age probably not older than biozone MMi11<br />
(Figure 9; D’Onofrio et al. 1975; Iaccar<strong>in</strong>o 1985; Iaccar<strong>in</strong>o<br />
et al. 2007). The age can be constra<strong>in</strong>ed fur<strong>the</strong>r by <strong>the</strong><br />
presence of Neogloboquadr<strong>in</strong>a cont<strong>in</strong>uosa Blow, whose last<br />
stratigraphic occurrence <strong>in</strong> <strong>the</strong> Mediterranean is <strong>in</strong> <strong>the</strong><br />
subzone Globiger<strong>in</strong>oides obliquus extremus/G. bulloideus<br />
(Iaccar<strong>in</strong>o 1985) or subzone MMi12a of Iaccar<strong>in</strong>o et<br />
al. (2007). The deltaic bottomset deposits, coeval with<br />
<strong>the</strong> delta built-out, can thus be assigned to <strong>the</strong> biozone<br />
<strong>in</strong>terval MMi11–MMi12a (Figure 9; D’Onofrio et al.<br />
1975; Iaccar<strong>in</strong>o 1985; Iaccar<strong>in</strong>o et al. 2007). The delta<br />
thus appears to have prograded <strong>in</strong> an approximate time of<br />
20<br />
ILGAR et al. / Turkish J Earth Sci<br />
8.5–7.8 Ma B.P., which corresponds to <strong>the</strong> regressive part<br />
(8.3–7.8 Ma B.P.) of <strong>the</strong> third-order eustatic sea-level cycle<br />
TB3.2 of Haq et al. (1988).<br />
In summary, <strong>the</strong> isolated late Tortonian delta <strong>in</strong> <strong>the</strong> Mut<br />
Bas<strong>in</strong>, although seem<strong>in</strong>gly correlative with similar deltas <strong>in</strong><br />
<strong>the</strong> <strong>Adana</strong> Bas<strong>in</strong>, is significantly older. Its development and<br />
drown<strong>in</strong>g were apparently related to a third-order eustatic<br />
sea-level cycle, ra<strong>the</strong>r than local tectonics. There was no<br />
compressional Neogene deformation <strong>in</strong> <strong>the</strong> Mut Bas<strong>in</strong>,<br />
whose marg<strong>in</strong> <strong>in</strong>stead shows normal faults <strong>in</strong>dicat<strong>in</strong>g<br />
postorogenic tectonic extension (Figures 12b and 12c).<br />
The amplitude of eustatic cycle TB3.2 did not exceed 30 m<br />
(Haq et al. 1988), but <strong>the</strong> sea-level change was recognised<br />
<strong>in</strong> several o<strong>the</strong>r peri-Mediterranean bas<strong>in</strong>s (e.g., Rouchy<br />
& Sa<strong>in</strong>t Mart<strong>in</strong> 1992; Larsen 2003; Roveri & Manzi 2006).<br />
However, this eustatic cycle was also modulated by<br />
local tectonics and became recorded differently <strong>in</strong> different<br />
bas<strong>in</strong>s. The mar<strong>in</strong>e reflood<strong>in</strong>g of <strong>the</strong> Mut Bas<strong>in</strong> was<br />
probably outpaced by <strong>the</strong> regional isostatic uplift of <strong>the</strong><br />
Central Taurides, whereby <strong>the</strong> bas<strong>in</strong> became emerged well<br />
before <strong>the</strong> hypersal<strong>in</strong>ity state and evaporative drawdown<br />
of <strong>the</strong> Mediterranean Sea. In <strong>the</strong> <strong>Adana</strong> Bas<strong>in</strong>, this<br />
eustatic cycle went unrecognisable (Figure 2), probably<br />
because <strong>the</strong> low-amplitude eustatic sea-level fall was fully<br />
compensated by <strong>the</strong> postthrust<strong>in</strong>g isostatic subsidence of<br />
<strong>the</strong> foreland bas<strong>in</strong>. In <strong>the</strong> Antalya Bas<strong>in</strong>, <strong>in</strong> contrast, <strong>the</strong><br />
Tortonian succession as a whole is regressive (Flecker et<br />
al. 1995; Deynoux et al. 2005; Ç<strong>in</strong>er et al. 2008), yet shows<br />
no less than 4 cycles of a mar<strong>in</strong>e drown<strong>in</strong>g and renewed<br />
progradation of <strong>the</strong> bas<strong>in</strong>-marg<strong>in</strong> fan deltas (Larsen<br />
2003). Their exact tim<strong>in</strong>g is uncerta<strong>in</strong> and none of <strong>the</strong>se<br />
cyclo<strong>the</strong>ms is recognisably <strong>forced</strong>-regressive, but at least<br />
some of <strong>the</strong>m may be third-order eustatic sequences of<br />
type 2.<br />
These regional comparisons illustrate <strong>the</strong> difficulty<br />
with <strong>in</strong>terbas<strong>in</strong>al stratigraphic correlations and serve as a<br />
warn<strong>in</strong>g aga<strong>in</strong>st a superficial l<strong>in</strong>k<strong>in</strong>g of seem<strong>in</strong>gly similar<br />
events <strong>in</strong> <strong>the</strong> late Miocene peri-Mediterranean bas<strong>in</strong>s (see<br />
also discussions by Clauzon et al. 1996; Soria et al. 2003;<br />
Roveri & Manzi 2006). Reliable stratigraphic correlations<br />
require biostratigraphic constra<strong>in</strong>ts, a good understand<strong>in</strong>g<br />
of <strong>the</strong> bas<strong>in</strong>’s bathymetric conditions and sedimentary<br />
systems, and a careful account of <strong>the</strong> bas<strong>in</strong>’s tectonic<br />
development. False hypo<strong>the</strong>tical correlations of regional<br />
events lead to mistaken regional <strong>in</strong>terpretations.<br />
9. Conclusions<br />
This comb<strong>in</strong>ed sedimentological, sequence-stratigraphic,<br />
and biostratigraphic study of <strong>the</strong> late Miocene deposits<br />
<strong>in</strong> <strong>the</strong> <strong>Adana</strong> Bas<strong>in</strong> has shown that <strong>the</strong> shallow-mar<strong>in</strong>e<br />
Handere Formation of Tortonian–<strong>Mess<strong>in</strong>ian</strong> age,<br />
previously <strong>in</strong>terpreted as a simple regressive succession,<br />
bears a high-resolution record of several major relative
sea-level changes <strong>in</strong> <strong>the</strong> bas<strong>in</strong>. The base of this formation<br />
recorded a <strong>forced</strong> regression correspond<strong>in</strong>g to <strong>the</strong> end-<br />
Serravalian (Tor-1) eustatic fall <strong>in</strong> sea level. The lower to<br />
middle part of <strong>the</strong> formation is transgressive, culm<strong>in</strong>at<strong>in</strong>g<br />
<strong>in</strong> offshore mudstones. The upper part is regressive and<br />
its 3 isolated conglomeratic members represent sharpbased<br />
Gilbert-type deltas with axially <strong>in</strong>cised fluvial<br />
valleys that recorded a depositional <strong>forced</strong> regression,<br />
biostratigraphically dated to ~7.8 to 6.4 Ma B.P. on <strong>the</strong> basis<br />
of planktonic foram<strong>in</strong>ifera <strong>in</strong> delta bottomset deposits.<br />
This latest Tortonian–early <strong>Mess<strong>in</strong>ian</strong> regression is<br />
attributed to <strong>the</strong> tectonic conversion of <strong>the</strong> <strong>Adana</strong> foredeep<br />
shelf <strong>in</strong>to a piggyback bas<strong>in</strong>, as is <strong>in</strong>dependently <strong>in</strong>dicated<br />
by seismic profiles and compressional bas<strong>in</strong>-marg<strong>in</strong><br />
deformation. The mar<strong>in</strong>e reflood<strong>in</strong>g of <strong>the</strong> bas<strong>in</strong>, estimated<br />
at ~6.4 to 6 Ma B.P., is ascribed to a postthrust<strong>in</strong>g flexural<br />
subsidence of <strong>the</strong> foreland under <strong>in</strong>creased crustal load.<br />
The transgression brought <strong>in</strong> evaporitic sedimentation,<br />
which suggests <strong>in</strong>vasion of hypersal<strong>in</strong>e Mediterranean<br />
water. The Mediterranean Sea <strong>in</strong> its eastern part would thus<br />
appear to have reached hypersal<strong>in</strong>ity around 6.5 Ma B.P.<br />
The bas<strong>in</strong> was subsequently emerged and its<br />
gypsiferous deposits were extensively eroded due to<br />
ano<strong>the</strong>r <strong>Mess<strong>in</strong>ian</strong> <strong>forced</strong> regression, which is attributed<br />
to <strong>the</strong> early evaporative drawdown of <strong>the</strong> Mediterranean<br />
Sea, regionally dated to ~6 Ma B.P. The Mediterranean<br />
Sea <strong>the</strong>n desiccated. The postorogenic regional isostatic<br />
uplift of <strong>the</strong> Taurides had meanwhile elevated <strong>the</strong> <strong>Adana</strong><br />
Bas<strong>in</strong> sufficiently to prevent its reflood<strong>in</strong>g by <strong>the</strong> Zanclean<br />
regional transgression at 5.3 Ma B.P. The bas<strong>in</strong> rema<strong>in</strong>ed<br />
terrestrial <strong>in</strong> <strong>the</strong> post-Miocene time, accumulat<strong>in</strong>g a<br />
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Acknowledgments<br />
The field study was funded by <strong>the</strong> General Directorate of<br />
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