Turkish Journal of Earth Sciences Turkish J Earth Sci (2013) 22: 820-838 http://journals.tubitak.gov.tr/earth/ © TÜBİTAK Research Article doi:10.3906/yer-1208-2
Middle-Upper Miocene paleogeography of southern Turkey: insights from stratigraphy and calcareous nannofossil biochronology of the Olukpınar and Başyayla sections (Mut-Ermenek Basin)*
1,2 3 4 1,2, Paola CIPOLLARI , Eva HALÁSOVÁ , Kemal GÜRBÜZ , Domenico COSENTINO * 1 Department of Geological Sciences, Roma Tre University, Rome, Italy 2 Institute of Environmental Geology and Geoengineering (IGAG-CNR), Monterotondo, Rome, Italy 3 Department of Geology and Paleontology, Comenius University, Bratislava, Slovakia 4 Department of Geological Engineering, Faculty of Engineering and Architecture, Çukurova University, Balcalı, Adana, Turkey
Received: 08.08.2012 Accepted: 01.07.2013 Published Online: 26.08.2013 Printed: 25.09.2013
Abstract: The age of the marine succession capping the basement rocks of the central Taurides in the Mut-Ermenek Basin is constrained using calcareous nannofossil biochronology. The Olukpınar section, which correlates with the biozones between MNN5a and MNN6b (late Langhian-late Serravallian), represents a deeper marine environment developed lateral to the Ermenek platform. The long-term transgressive–regressive cycle of the Olukpınar section, which corresponds to the middle-upper part of the TB2 supercycle, can be subdivided into 2 large-scale (106 years) cycles (TB2.4 and TB2.5) based on the occurrence of 2 major debris flow deposits linked to sea-level drop. The younger late Tortonian Başyayla section represents a transgressive–regressive sedimentary cycle (TB3.2 cycle) responsible for the major transgressive event that occurred at the southern margin of the Central Anatolian Plateau during the Late Miocene. This major transgressive event is responsible for the migration of the coastal onlap of the Mediterranean Sea towards the interior of the Anatolian Peninsula, almost 100 km inland from the present Eastern Mediterranean coast line. The ~8 Ma age of the younger marine sediments deposited during the TB3.2 cycle, which onlap the basement rocks of the central Taurides at an elevation of ~2 km, represents a maximum age for the start of surface uplift of the Central Anatolian Plateau’s southern margin.
Key words: Stratigraphy, calcareous nannofossils biostratigraphy, Middle-Late Miocene, Mut-Ermenek Basin, southern Turkey
1. Introduction Several authors have provided biostratigraphic age The southern margin of the Central Anatolian plateau constraints for those Miocene marine deposits. Bassant (CAP) is characterized by a postorogenic Oligocene- et al. (2005) identified the NN4 calcareous nannofossil Miocene succession that unconformably overlies highly biozone (late Burdigalian-early Langhian; Martini & deformed Paleozoic and Meso-Cenozoic Central Tauride Müller 1986) in the lower part of the marine succession on basement rocks. The Miocene marine deposits capping the eastern side of the Mut Basin. According to the same the southern margin of the CAP in the Mut-Ermenek authors, the upper part of the same marine succession Basin belong to the Köselerli and Mut formations, and should be part of the NN5 biozone (Langhian). In the show nearly underformed primary depositional geometry, Mut-Ermenek Basin, Tanar and Gökçen (1990) identified suggesting a tectonic quiescence during their deposition marine deposits as young as Serravallian. Similar ages (Bassant et al. 2005). In the Başyayla area (Figures 1A and for the Miocene marine succession cropping out north 1B), the uppermost part of the Miocene marine succession of the Mut-Ermenek Basin horizontally caps (Cosentino et of Ermenek were provided by Janson et al. (2010). al. 2012) the highly deformed Mesozoic rocks of the Bozkır These authors identified 3 chronostratigraphic units unit and the Hadim nappe (Akay & Uysal 1988). In the within the mainly carbonate marine sediments of the same area, the maximum elevation of those undeformed Ermenek area. The first chronostratigraphic unit, which marine sediments is around 2000 m, suggesting substantial includes the lowermost part of the marine succession, long-wavelength uplift of the area after the deposition of is poorly dated as the upper part of the NN4 calcareous those marine sediments (Cosentino et al. 2012; Schildgen nannofossil biozone (latest Burdigalian-early Langhian). et al. 2012a, 2012b). The second chronostratigraphic unit, which includes * Correspondence: [email protected] 820 CIPOLLARI et al. / Turkish J Earth Sci
A 30°E 35°E 40°E Post-orogenc rocks Black Sea n t d Elevaton Mocene nertc lmestones P o e s (km) NAF Mocene cont. clastcs NAF 2.0 Mocene lake sedments 40°N Btls-Zagros and lmestones Western Aegean Collson 1.5 Central Pre-orogenc rocks Extensonal Zone Provnce Anatolan Plateau 1.0 Cretaceous lmestones and shales Btls-Zagr os S EAF ut ur e 0.5 Jurassc lmestones T s a e Trassc lmestones, schst, u r d Araban Plate 0 tu te, basalt, cont. clactcs Medterranean Fgs. Cambran/Precambran 1B, 1C marbles, dolomte, schst 35°N Sea 30°E 35°E 40°E 35°N
B 32°E 33° 34° C 32°E 33° 34°
Ce ntral 37° Ta 37° 37°N 37°N urdes ntral Fg. 2 Ce urdes Ta Başyayla section Başyayla secton N Mut Basn N Ermenek Basn Olukpınar Olukpınar section secton 50 km 50 km 32°E 33° 34° 36°N 36° 36°N 32°E 33° 34° 36° Figure 1. Tectonic and geologic setting of field area. (A) Regional plate tectonic setting with major structures and topography (from Shuttle Radar Topography Mission 90-m resolution data; Jarvis et al. 2008). NAF: North Anatolian fault, EAF: East Anatolian fault. (B) Southern margin topography with location of Olukpınar and Başyayla sections. (C) Geology simplified from 1:500,000 scale geologic maps (Şenel 2002; Ulu 2002) with location of the study sections. Black lines delineate tectonic contacts within basement rocks. Modified from Cosentino et al. (2012). most of the marine succession of the Ermenek area, geometries that characterize the carbonate deposits of the corresponds to the NN5 calcareous nannofossil biozone Mut Formation point to a regressive trend. This regressive (middle-late Langhian). The third chronostratigraphic trend led to the sedimentation of the carbonate ramp unit, which includes the uppermost part of the local deposits of the Mut Formation throughout the Mut Basin marine succession of the Ermenek area, pertains to the (Tanar & Gökçen 1990). NN6 calcareous nannofossil biozone (early Serravallian). In the Ermenek area, above a subtropical flat platform Finally, in the Başyayla area (Mut-Ermenek Basin), of late Burdigalian age (NN4), a platform-basin system Cosentino et al. (2012) identified planktonic foraminifera developed during the Langhian (Janson et al. 2010). At assemblages that constrain the upper part of the section that time, a composite platform system developed to the to the MMi 12a biozone (8.35–7.81 Ma; Iaccarino et al. NE of the town of Ermenek, including an aggradational 2007). Paleomagnetic and biostratigraphic results from barrier at the platform edge and several platform-banks the uppermost part of the marine deposits of the Başyayla prograding into intraplatform depression deposits. In this section point to C4r.1r or C4r.2r chrons within the C4 paleogeographic framework, foreslope and basin deposits magnetozone, limiting the potential age range of the upper were deposited SW of the Langhian aggradational barrier part of the section to the interval of 8.35–8.108 Ma (late that was developing in the vicinity of the present position Tortonian; Cosentino et al. 2012). of the town of Ermenek (Janson et al. 2010). In the late Burdigalian-Langhian deposits of the Mut Due to the excellent exposure of the carbonate deposits area, Bassant et al. (2005) recognized 2 high-amplitude of the Mut-Ermenek Basin (Mut Formation) and their (100–150 m) sea-level cycles, which are interpreted as tectonically undisturbed setting, recent studies focused eustatic cycles (third-order cyclicity) driven by the 400- mainly on the sequence stratigraphic architecture and kyr orbital cyclicity (eccentricity). The progradational carbonate sedimentology of the Mut Formation (Bassant
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1999; Bassant et al. 2005; Janson et al. 2010; Pomar et al. Beydağlan) and several allochthonous units (Aladağı, 2012). Less attention was given to the deeper depositional Bolkardağı, Bozkır, Hadim, Alanya, and Antalya) (Akay & environment at the slope-to-basin transition (Köselerli Uysal 1988; Bozkaya & Yalçin 2000). The Bozkır unit was Formation), which in both the published maps (e.g., thrust onto the Bolkardağı and Aladağı units in the Upper Gedik et al. 1979; Şenel 2002; Ulu 2002) and in the Cretaceous, and in the Middle-Late Eocene these 3 units derived paleogeographical schemes (e.g., Bassant et al. were thrust, from north to south, onto the Geyikdağı unit 2005; Janson et al. 2010; Pomar et al. 2012) appears to be (Akay & Uysal 1988; Özgül 1997; Bozkaya & Yalçin 2000). underestimated in terms of extent. To the south and to In the Mut-Ermenek Basin, the fold-and-thrust belt the west of the town of Ermenek, in the Olukpınar and of the central Taurides is characterized by some thrust Başyayla areas, deeper marine marls (Köselerli Formation) planes within the Bozkır unit, which separate different extensively crop out, challenging the extent of the Miocene subunits, and the lateral juxtaposition of the Hadim nappe carbonate platform in those areas. with the Bozkır unit, along the NW-SE right-lateral strike- The Miocene deeper marine deposits of the Mut- slip Bozkır fault (Akay & Uysal 1988). The tectonic units Ermenek Basin (Köselerli Formation) were dated upper of this fold-and-thrust belt are unconformably overlain Burdigalian-Serravallian by using ostracods, planktonic by continental clastic deposits (Yenimahalle and Fakırca foraminifera, and calcareous nannofossils (Tanar & formations) connected with the development of widespread Gökçen 1990; Atabey et al. 2000). More recently, referring land areas in southern Turkey, as a consequence of the to the calcareous nannofossil biostratigraphy of Martini general uplift induced by the Taurus orogeny during the and Müller (1986), Bassant et al. (2005) identified the Late Eocene-Early Oligocene in that area (Figure 1C). upper part of the marine succession on the east side of According to some authors (Akay et al. 1985; Aksu et al. the Mut Basin to be part of the NN5 biozone, whereas 1992; Görür 1992; Williams & Ünlügenç 1992; Robertson Janson et al. (2010) identified in the uppermost strata of & Grasso 1995), intramontane extension was initiated the Ermenek platform calcareous nannofossil assemblages throughout the Taurides during the Late Eocene-Early of the NN6 biozone, confirming a Serravallian age for the Miocene, which gave rise to suprasutural sedimentary topmost part of the Miocene marine deposits in the Mut- basins (Manavgat, Mut, Adana, Karsantı, Maraş, etc.). Ermenek Basin. This extensional phase, which may be linked to the retreat Here we present a micropaleontological analysis of the African plate (Kempler & Ben-Avraham 1987; of calcareous nannofossils, by using an updated Robertson 1998, 2000; Jolivet & Faccenna 2000), yielded biostratigraphical scheme (Fornaciari et al. 1996), on mainly tectonically controlled sedimentary basins with samples from 2 marine sections, the Olukpınar section the deposition of 2 second-order cycles (supercycles, and the Başyayla section (Figures 1A and 1B), located sensu Haq et al. 1988), which consist of thick continental south and northwest of the town of Ermenek, respectively. deposits of the Yenimahalle Formation (Lower Oligocene) Our new analyses allow us to 1) better constrain the age and the Fakırca Formation (Upper Oligocene-Aquitanian) of the marine succession capping the southern margin of (Figure 2A). the CAP (consequently constraining the maximum age for The Yenimahalle Formation is mainly characterized its uplift), 2) correlate the slope-to-basin deposits of the by coarse clastic beds of a fluviolacustrine environment. Mut-Ermenek Basin (Köselerli Formation) to the shallow- The younger Fakırca Formation consists of fine-grained water limestones of the Mut Formation, and 3) improve lacustrine deposits, with occasional coarser clastic the middle-late Miocene paleogeography at the southern intercalations (e.g., Gedik et al. 1979; Tanar & Gökçen margin of the CAP. 1990). These Oligocene-Lower Miocene continental deposits are generally tilted and faulted by mainly 2. Geological setting extensional tectonics. In the northwestern part of the Mut- The Central Taurides (Figure 1B), which extend from the Ermenek Basin (Başyayla area), this extensional tectonic Ecemiş Fault in the east to the Antalya Miocene basin phase reactivated an ancient strike-slip regional fault zone in the west, consist of oceanic- and continental-derived (Bozkır fault), which locally controlled the formation of an units of Cambrian to Tertiary age that were shortened Oligocene-Early Miocene sedimentary basin (Cosentino and overthrust in latest Cretaceous-Eocene time, during et al. 2012). the closure of the Mesozoic Neo-Tethyan Ocean and In the Mut-Ermenek Basin, the mainly marine Mut subsequent collision between the Taurus carbonate and Köselerli formations, which rest unconformably above platforms and the crystalline complex of central Anatolia the Oligocene-Early Miocene continental deposits (Figure (Şengör & Yilmaz 1981; Dixon & Robertson 1984). 2A), were deposited in a tectonically quiescent period, The tectonostratigraphic units of the Central Taurides corresponding to the TB2 p.p. and TB3 p.p. supercycles include 2 relatively autochthonous units (Geyikdağı and of Haq et al. (1988). In some places, the lower part of
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A - B
TIGR . STRATIGRAPHY OF OLUKPINAR SECTION CHRONO- LITHO
STRATIGR. STRA MUT-ERMENEK BASIN N 36° 29’ 40.46” E 33° 00’ 36.30” (base) N 36° 29’ 41.50” E 33° 00’ 31.94” (top) Depth Samples Depth Samples L thology L thology (m) (m) nanno forams+Sr
Mess n. OLUKPINAR SECTION EKN 130 55 110 m EKN 125
Mut F EKN 120 on an rt 50 105
To EKN 115
EKN 110 . m avall 45 EKN 105 100 EKN 235 EK01451-P Serr EKN 230 EKN 225 EKN 100 EKN 220 Köselerl F EKN 95 EKN 215 Langh an 40 95
EKN 90 EKN 210 m MIOCENE y F EKN 85 EK01406-P EKN 205 35 90 EKN 80 Der nça EKN 200 Burd gal an
EKN 75
30 EKN 70 85 EKN 195 m u tan an EKN 65
Aq EKN 190
EKN 60 EKN 185 25 80 EK01361-P
rca F EKN 55 EKN 180 EKN 50
kı EKN 175
Fa 20 EKN 45 75 EKN 170 Chatt an EKN 165 EKN 40 EKN 160 EKN 35 15 70 EK01311-P m . . .. EKN 155 . EKN 30 . . . .
EKN 150 OLIGOCENE EKN 25 . . 10 65 . . .. en mahalle F Rupel an
Y EKN 20 EKN 145 EKN 15 5 60 EKN 10 EKN 140
Fm EKN 135 EKN 5 EK01258-P -Rupel an OLIGOCENE
orogen c 0 EKN 1 55
e- m lm m lm Pre PRE-
Pr mc cm mc cm
Figure 2. (A) Synthetic stratigraphic log of the Olukpınar-Başyayla area and (B) measured stratigraphic log of the Olukpınar section. Abbreviations for the Olukpınar section include mc: marly clay, m: marl, cm: calcareous marl, and lm: limestone.
823 CIPOLLARI et al. / Turkish J Earth Sci the TB2 supercycle is characterized by lower Burdigalian shallow-water carbonates and bioclasts coming from the continental red-beds, deposited in fluvial environment surrounding Middle Miocene carbonate platforms. (lower Burdigalian Derinçay Formation), with lateral and These deeper marine deposits of the Olukpınar section vertical transitions to a lagoon-marine environment (Eris (103.5 m thick) pertain to the lower and middle parts of et al. 2005; Şafak et al. 2005). the Köselerli Formation, which pass upward into coralgal The younger marine deposits, which are mainly limestones of the Mut Formation (Figure 2A). The deep marls with intercalations of resedimented carbonate marine marls are characterized by a high-frequency in channelized bodies (Köselerli Formation) passing cyclicity of calcareous marls and marls, containing laterally and upwards to shallow-water carbonate deposits planktonic foraminifera, sponge spicules, and traces of (bryomol/foramol and rhodalgal limestones, Mut bioturbation (mainly Thalassinoides and Chondrites) in Formation), are related to the evolution of a platform-basin some places. The Köselerli Formation at the Olukpınar system (Janson et al. 2010). These marine sediments were section indicates a deeper marine environment compared deposited in the Mut-Ermenek Basin during long-term to the ‘depression marly deposits’ within the Ermenek (105–106 years) transgressive/regressive cycles (middle platform system (e.g., planktonic rich wackestone facies; Burdigalian-late Tortonian; Bassant et al. 2005; Janson et Janson et al. 2010). In fact, according to Janson et al. al. 2010; Cosentino et al. 2012), giving rise to shallowing- (2010), the Köselerli Formation in the Ermenek platform upward marine successions. system consists of very fine-grained deposits (mainly In the Late Miocene (late Tortonian-early Messinian), marls) with common planktonic foraminifera associated the occurrence of marine sediments both in the Beyşehir with rotaliids, Heterostegina spp. fragments, scaphopod area (Schildgen et al. 2012b), to the NW of the Mut- tubes, and rare, small, reworked miliolids. Ermenek Basin, and in the Adana Basin (Faranda et al. In the Olukpınar section, the deep marine deposits of 2013), to the SE of the CAP southern margin, is consistent the Köselerli Formation are punctuated by 4 channelized with the notion of a marine environment distributed bodies (debris flow deposits) of mainly coarse-grained throughout the present southern margin of the CAP, prior bioclastic resedimented carbonate and blocks of shallow to the most recent phase of surface uplift (Cosentino et al. water limestones, showing N-S channel axes. These 2012; Schildgen et al. 2012a, 2012b). At that time, the Mut- channelized bodies occur at the following stratigraphic Ermenek Basin was a part of the marginal Mediterranean depths from the base of the measured section: 1) from 2 m Sea, which during the Late Miocene transgression phase to 2.5 m; 2) from 8 m to 21.75 m; 3) from 45.75 m to 47.30 reached the interior of the Anatolian Peninsula, connecting m; and 4) from 61.35 m to 68.75 m (Figure 2B). the Beyşehir area with the Adana Basin (Schildgen et al. The first 2 debris flows consist of coarse-grained 2012b). biocalcarenites, containing bioclasts mainly from corals, echinoids, mollusks, benthic foraminifera, and red algae, as 3. Sampled sections and methods well as some minor cemented clasts. The last 2 debris flows 3.1. The Olukpınar section include carbonate clasts and blocks showing an upwards The Olukpınar section (base section: 36°29′40.46″N, increase of the mean particle size from 10 cm (debris flow 33°00′36.30″E; top section: 36°29′41.50″N, 33°00′31.94″E) 3) up to 70 cm and more (debris flow 4). Slump structures mainly includes wackestones and mudstones rich in were observed in the basal part of both of the thicker planktonic foraminifera with rare intercalations of coarse- channelized bodies (debris flows 2 and 4), whereas some grained deposits, such as calcarenites, calcirudites, and bioturbations (mainly Thalassinoides) were found just channelized bodies, containing huge blocks (of more than within the uppermost debris flow (debris flow 4). 1 m in size) of calcarenites and shallow-water limestones The facies analysis of the Olukpınar area, although in a fine-grained matrix. Benthic fauna within the based on just one section, and the field observations of the wackestones and mudstones of the Olukpınar section are spatiotemporal relationship between Mut and Köselerli quite rare, while sponge spicules and fragments of thin formations in the Ermenek-Olukpınar area point to a pelecypod shells pointing to a deeper marine environment deeper marine environment to the south of the Ermenek are very common. Bioclasts mainly from echinoids, carbonate platform, characterized by the deposition of mollusks, red algae, corals, and bryozoans are abundant planktonic-rich, fine-grained deposits, with common within the coarse-grained deposits of the study section, sponge spicules, and carbonate debris flows containing which often show slumping structures. Here we interpret shallow-water bioclasts, sporadically arriving far from the Olukpınar section as related to a deeper marine the carbonate factory of the Ermenek platform. Thus, the environment characterized mainly by the deposition of Köselerli Formation in the Olukpınar section could be planktonic-rich, fine-grained sediments (mainly marls), related to a slope-to-basin depositional environment in episodically reached by debris-flows of resedimented connection with the Ermenek carbonate platform to the
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north, in agreement with the late Early to Middle Miocene A - STRATIGRAPHY OF B TIGR . BAŞYAYLA SECTION CHRONO- paleogeographical reconstruction of the Ermenek LITHO MUT-ERMENEK BASIN STRATIGR. STRA N 36° 46’ 20.68” E 32° 40’ 41.02” (top) carbonate platform suggested by Janson et al. (2010). BAŞYAYLA SECTION Depth L thology Samples From the deep marine deposits of the Olukpınar section, (m)
Mess n. EK02 238 samples were collected at 0.5-m regular spacing from 55 the marly horizons of the Köselerli Formation (Figure 2B) m for biostratigraphical analysis using calcareous nannofossil Mut F on an
assemblages. This micropaleontological analysis was rt 50 carried out on smear slides, which were prepared from To unprocessed sediment following standard techniques. . The smear slides were analyzed with light microscope m techniques at 1000× magnification. After a preliminary avall 45 investigation, which generally showed a low abundance Serr of calcareous nannofossil associations without any rapid change in the fossil assemblage, it was decided to analyze Köselerl F Langh an 40 just 112 samples, with a spacing of approximately 1 m.
A semiquantitative study was performed by counting m MIOCENE at least 500 specimens per slide, based on the following ay F abundance categories: A = abundant (>10 specimens per 35 Der nç field of view), C = common (1–10 specimens per field of Burd gal an view), F = frequent (1 specimen per field of view), R = rare BAS 24 BAS 23 (<1 specimen per field of view), VR = very rare (1 specimen 30 BAS 22 per 10 fields of view). Finally, for a biochronological m BAS 21 qu tan an analysis of the calcareous nannofossil assemblages, we A BAS 20 BAS 19 adopted, as a reference, the Mediterranean zonal scheme BAS 18 b of Fornaciari et al. (1996). 25 rca F 3.2. The Başyayla section k The Başyayla section (top section: 36°46′20.68″N, BAS 18
32°40′41.02″E) contains the uppermost part of the Fa 20 BAS 17
Chatt an BAS 16 Köselerli Formation (about 40 m of intraplatform/ BAS 15 offshore marls) and the transition up to the shallow-water BAS 14 BAS 13 limestones of the Mut Formation (about 20 m of foramol/ 15 BAS 12 bryomol and rhodalgal limestones) (Figure 3A). The ...... BAS 11 sampled section in the Başyayla area consists mainly of . . BAS 10
marls of the Köselerli Formation, rich in mollusks, benthic OLIGOCENE BAS 9 . . 10 foraminifera, ostracods, and planktonic foraminifera . . .. BAS 8 en mahalle Fm in some levels (Cosentino et al. 2012). In the Başyayla Rupel an Y BAS 7 section, we collected 25 samples (BAS 1–BAS 24 and BAS BAS 6 18b; Figure 3B) from the clayey and marly horizons for 5 BAS 5 BAS 4 calcareous nannofossil analysis. m BAS 3 BAS 2
Rupel an BAS 1 4. Results of the calcareous nannofossil analysis from OLIGOCENE e-
orogen c F 0
e- c m ml Pr the Mut-Ermenek Basin PRE-
Pr mc cm lm 4.1. The Olukpınar section The state of preservation of the calcareous nannofossils Figure 3. (A) Synthetic stratigraphic log of the Olukpınar- Başyayla area and (B) measured stratigraphic log of the Başyayla varies depending on the samples examined and on the section. Abbreviations for the Başyayla section include c: clay, mc: abundance of the assemblages as well. Several samples were marly clay, m: marl, cm: calcareous marl, ml: marly limestone, completely barren. Nonetheless, significant biostratigraphic and lm: limestone. events were identified within the Olukpınar section, which includes the lower–middle part of the Köselerli Formation. The results of the semiquantitative analysis are shown in The common presence of Sphenolithus heteromorphus Table 1, whereas some representative species are shown in was detected starting from the base of the section. This Figure 4. marker species is present up to sample EKN 149, about 64
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Table 1. Results of the semiquantitative analysis of the calcareous nannofossils assemblages from the Olukpınar section. A: abundant (>10 specimens per field of view), C: common (1–10 specimens per field of view), F: frequent (1 specimen per field of view), R: rare (<1 specimen per field of view), VR: very rare (<<1 specimen per field of view). spp. spp. spp. Samples H. carteri H. walbersdorfensis H. intermedia S. moriformis S. heteromorphus R. pseudoumbilicus Reticulofenestra floridanus Cy. C. leptoporus C. premacintyrei C. macintyrei jafari U. C. pelagicus C. miopelagicus Dictyococcites Pontosphaera
EKN 1 F - VR R F - C F - VR - R F VR A VR EKN 3 F - VR F R - A F VR - - - R VR A R EKN 5 F - VR R F - A R - - - R A - A R EKN 7 F - VR F R - A F - - - R R - C R EKN 9 ------R - - - - EKN 11 F - VR R F - A R VR R R A R EKN 13 F - VR R F - C VR R VR - - R - C VR EKN 15 F - R F F - A VR R VR - VR R - A VR EKN 17 F - VR R F - A VR VR VR - VR R - A F EKN 19 R . . R VR . VR VR - - - - VR - R EKN 21 F - R F R - A F VR . . . R - C R EKN 23 F - R R F - A F F R - F F - A R EKN 25 ------EKN 27 F - - VR - - C R VR - - R - C - EKN 29 F - - R VR - C - VR - - - - - C VR EKN 31 R - - - - - F - - - - VR - F VR EKN 33 ------EKN 35 ------EKN 37 ------EKN 39 F - - VR VR - F - - - - - VR VR F VR EKN 41 ------EKN 43 ------EKN 45 ------EKN 47 - - - - VR - F - - - - - F - C - EKN 49 ------EKN 51 ------EKN 53 ------EKN 55 ------EKN 57 VR - - VR - - VR - - - - - VR - VR - EKN 59 ------EKN 61 ------EKN 63 - - - VR VR - VR - - - - - VR - F - EKN 65 - - - VR VR - VR - - - - - VR - F - EKN 67 VR . . . VR . F VR . VR . . VR VR C - EKN 69 VR - - VR VR - F - - - - - VR - - - EKN 71 R VR - R VR - F - - VR - - R - C VR EKN 73 R VR - R VR - F - - VR - - R - C VR EKN 75 F R - R F - F R - - - - C VR C VR EKN 77 F VR - VR R - F VR - - - - F VR C - EKN 79 R - - VR R - C F - - - - R - C - EKN 81 F - - F F - A F - - - - C - A VR EKN 83 F - VR F F - A C F F - VR F - A -
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Table 1. (continued). spp. spp. spp. Samples H. carteri H. walbersdorfensis H. intermedia S. moriformis S. heteromorphus R. pseudoumbilicus Reticulofenestra floridanus Cy. C. leptoporus C. premacintyrei C. macintyrei jafari U. C. pelagicus C. miopelagicus Dictyococcites Pontosphaera
EKN 85 C R - F R - A F - - - C - A C EKN 87 F VR - F C - C - - - - - C - F F EKN 89 R VR - F R - A F - R - C C - A F EKN 91 VR - - R VR - C C - - - R R - A R EKN 93 VR - - VR - - C F - - - - F - C VR EKN 95 VR - - VR R - C F - - - - C - C VR EKN 97 R - R R - C F - - - - A - C - EKN 99 R - - R F - C F - - - - C - A VR EKN 101 R - VR F R - C F - VR - C F - A - EKN 103 F - R C R - A R - - - - C - A R EKN 105 R - VR VR F - F R - - - - F - C - EKN 107 VR - - VR R - R - - - - - F - C - EKN 109 ------EKN 111 ------EKN 113 VR - - - - - C R - - - R R - C VR EKN 115 R VR - - - - C - - VR - VR F - C - EKN 117 F R - - - VR C F - F - - C - A - EKN 119 R - - F F - C F - - - - C - A - EKN 121 F - - F F - A C R VR - R A - EKN 123 F - - F VR - F C - - - - F - A - EKN 125 VR - - R VR - F - - - - - F - C - EKN 127 VR - - - - - F - - - - - R - F - EKN 129 VR VR ------F - F - EKN 131 R VR - VR - - A R - - - - C - A - EKN 133 C F VR R F - C F - - - - C - A - EKN 135 F R - R F - C C - - - C F - A VR EKN 137 R R - VR - - F R - VR - - F - C - EKN 139 R VR - VR - VR F VR - - - - F - C - EKN 141 F R - R F - F F VR - - - A VR A - EKN 143 F VR - VR F - C VR - - VR - C VR A - EKN 145 R - - VR R - C C - - - - C - A - EKN 147 F VR - VR VR - F F - - - - F - C - EKN 149 F R - R F - C F - - - - C - A - EKN 151 ------EKN 153 F VR R R - VR C F - - - F C - C - EKN 155 F F - R - - C VR - - - F F - A - EKN 157 F R - F VR - C F - R - - C - C - EKN 159 ------EKN 161 R - - VR - - R - - - - - F - C - EKN 163 R - - - - - R R - - - - F - F - EKN 165 R ------F - C - EKN 167 VR VR - F - VR C R - - - F C - A -
827 CIPOLLARI et al. / Turkish J Earth Sci
Table 1. (continued). spp. spp. spp. Samples H. carteri H. walbersdorfensis H. intermedia S. moriformis S. heteromorphus R. pseudoumbilicus Reticulofenestra floridanus Cy. C. leptoporus C. premacintyrei C. macintyrei jafari U. C. pelagicus C. miopelagicus Dictyococcites Pontosphaera
EKN 169 F - - F - VR C VR - - - R F - F - EKN 171 F F - VR - - C - - R - R C - A - EKN 173 VR - - VR - - R - - - - R F - C - EKN 175 ------EKN 177 F VR - F - - F - - - - F C - A - EKN 179 F VR - F - - F - - - - F C - A - EKN 181 R - - R - - F VR - VR - - C - C - EKN 183 ------EKN 185 ------EKN 187 VR ------VR - R - EKN 189 ------EKN 191 R VR - VR - - R - - - - C R - F - EKN 192 - VR ------R - C - EKN 195 VR - - VR - - F - VR VR - - F - C - EKN 198 R VR - R - R F - VR VR - - C - A - EKN 201 C F R R - VR C - - - - - C - F - EKN 204 F F VR R - VR C - - VR - - C - A - EKN 207 F C VR F - F F - - VR - - C - A - EKN 210 F R - - - R F - - VR - - A - A - EKN 213 C R - C - F C - - - VR - - - A - EKN 216 F VR - F - R F - - - - - F - A - EKN 219 R VR - VR - F C - - - - - F - C- EKN 222 R - - - - VR R - - - - - R - F - EKN 225 R R R R - VR R - - - - - F - C - EKN 228 R R - R - C A - - - - - C - A - EKN 231 F F - C - F F - - - - R C - A R EKN 234 F F R F - C C - - F - F C - A F EKN 237 F VR F F - C C - - R - - C VR C - m above the base of the section. The continuous presence of Calcidiscus premacintyrei occurs throughout the entire Helicosphaera walbersdorfensis was observed only starting section, whereas C. macintyrei is virtually absent in all from sample EKN 129 and, even if it is never abundant, samples except for 2, where it is very rare. this event could be interpreted as the first common In addition to the above-mentioned bioevents, occurrence (FCO) of H. walbersdorfensis. Moreover, the the assemblages observed in the Olukpınar section last occurrence (LO) of Cyclicargolithus floridanus was are characterized by the quite continuous presence recognized in sample EKN 169, about 10 m above the LO of Helicosphaera carteri, by rare and scattered H. of S. heteromorphus. Finally, the FCO of Reticulofenestra intermedia, rare H. walbersdorfensis, mainly rare S. pseudoumbilicus was detected in sample EKN 198, 87 m moriformis, common or abundant Reticulofenestra spp., above the base and 13 m above the LO of C. floridanus. common Coccolithus pelagicus, very rare and scattered
828 CIPOLLARI et al. / Turkish J Earth Sci
2µm 1 2µm 2 3 2µm 4 2µm
2µm 2µm 2µm 2µm 5 6 7 8
2µm 9 2µm 10 11 2µm 12 2µm
2µm 2µm 2µm 13 2µm 14 15 16 Figure 4. Microphotographs of some representative species of calcareous nannofossils from Olukpınar and Başyayla sections. 1, 2 - Sphenolithus moriformis (Bronnimann and Stradner, 1960) Bramlette and Wilcoxon, 1967, sample EKN 17. 3, 4 - Sphenolithus heteromorphus Deflandre 1953, sample EKN 17. 5, 6 - Calcidiscus premacintyrei Theodoridis, 1984, sample EKN 23. 7 - Helicosphaera walbersdorfensis Muller, 1974, sample EKN 234. 8 - Helicosphaera intermedia Martini, 1965, sample EKN 103. 9 - Reticulofenestra pseudoumbilicus (Gartner, 1967) Gartner, 1969, sample EKN 207. 10 - Reticulofenestra sp. Hay, Mohler and Wade, 1966, sample EKN 167. 11 - Umbilicosphaera jafari, Muller, 1974 sample BAS 16. 12 - Helicosphaera stalis, Theodoridis, 1984 sample BAS 24. 13, 14 - Coccolithus miopelagicus Bukry, 1971, sample EKN 67. 15 - Helicosphaera carteri (Wallich, 1877) Kamptner, 1954, sample EKN 23. 16 - Cyclicargolithus floridanus (Roth and Hay in Hay et al., 1967) Bukry, 1971, sample EKN 133.
C. miopelagicus, generally abundant Dictyococcites spp., lower 64 m of the study section to the MNN5a subzone rare or very rare Pontosphaera, and, finally, very rare (Fornaciari et al. 1996) (Figure 5). The interval between Umbilicosphaera jafari. the continuous presence of H. walbersdorfensis and the The presence of S. heteromorphus together with LO of S. heteromorphus (between 55.5 m and 66.5 m of the absence of H. ampliaperta allows us to refer the depth) points to the MNN5b subzone. Moving upward,
829 CIPOLLARI et al. / Turkish J Earth Sci
Chrono- Calcareous nannofossls ATNTS 2004 stratgraphy bostratgraphy o y . ry net tn & Stage ada & Medterranean calcareous nannofossls boevents et al rnacar ones ge (Ma) Buk olart (1996) (1986) (1981) Müller Ok Mag Z P A Epoch Mar Fo C4n 8 NN11 CN9 C4r FO D. berggren C4An FO D. pentaradatus 9 NN10 CN8 MNN10
C4Ar onan LO D. hamatus late 10 rt NN9 CN7 MNN9
C5n To FO D. hamatus MNN8b NN8 a FCO H. stals
CN 6 FO D. coaltus 11 MNN C5r NN7 CN5 b 7 FO D. kugler 12 LCO C. premacntyre C5An MNN C5Ar NN6 CN5 6b 13 a C5AAn avallan MNN6a LO FCO R. pseudoumblcus -C5ABr C5ACn MNN LO S. heteromorphus 14 Serr 5b FCO H. walbersdorfenss C5An mddle -Dr NN5 CN4 15 C5Bn MNN 5a C5Br LO H. amplaperta paracme S. heteromorphus 16 MNN4b Langhan C5Cn ocene LCO H. amplaperta M 17 C5Cr MNN NN4 CN3 4a C5Dn 18 C5Dr FO S. heteromorphus C5En MNN LCO S. belemnos C5Er NN3 CN2 3a-b 19 FO S. belemnos
C6n Burdgalan 20 MNN2b
C6r early C6An 21 NN2 c MNN2a H. euphrats acme end
C6Ar CN 1 22 C6AAn FCO H. carter -AAr MNN1d
C6Bn qutanan 23 C6Br A FO D. drugg FO S. dsbelemnos a+b MNN1c C6Cn NN1 24 MNN1a+b LO S. delphx C6Cr Olgocene NP25 CP19 b LO R. bsectus Figure 5. Biostratigraphic scheme of the late Oligocene and Miocene Mediterranean calcareous nannofossils used as a reference in this paper. The gray bands correspond to the proposed age of the Başyayla section (upper band) and the Olukpınar section (lower band). ATNTS 2004 is from Lourens et al. (2004); calcareous nannofossils biozonations are from Martini and Müller (1986), Okada and Bukry (1981), and Fornaciari et al. (1996). FO: first occurrence, LO: last occurrence, FCO: first common occurrence, LCO: last common occurrence. the LO of C. floridanus and the FCO of R. pseudoumbilicus study section is rare and discontinuous, and consequently associate the upper part of the section with the MNN6b not very useful for biostratigraphical analysis, the presence subzone. These 2 bioevents are generally considered coeval of C. premacintyrei up to the top of the section suggests and mark the base of the MNN6b subzone, although in the that the uppermost part of the Olukpınar section should studied section, they occur stratigraphically 12 m apart. be referred to the MNN6b subzone. Nonetheless, the discrepancy in the LO of C. floridanus In conclusion, our analysis of the calcareous nannofossil and the FCO of R. pseudoumbilicus with respect to other assemblages allows us to place the study section in a Mediterranean sections is not a real problem since the range between biozone MNN5a and biozone MNN6b, disappearance of C. floridanus has been recognized to be corresponding to a time interval between ~15.6 Ma and dependent on latitude and, therefore, it should not be used ~12.5 Ma. As a result, we can say that the Olukpınar for time correlation (Fornaciari et al. 1993; Raffi et al. 1995). section crosses the Langhian/Serravallian boundary in its Finally, even if the presence of the genus Calcidiscus in the lower part, whereas its uppermost portion, just below the
830 CIPOLLARI et al. / Turkish J Earth Sci first occurrence of shallow-water limestones of the Mut of H. stalis. Even if its abundance is not very high due to Formation in our local section, is included within the late the scarcity of the assemblages (in particular of the genus Serravallian. Helicosphaera), we can presume that the Başyayla section 4.2. The Başyayla section is above the FCO of H. stalis. This position is supported In the Başyayla section, the calcareous nannofossils are by the virtual absence of H. walbersdorfensis (Fornaciari rare and moderately preserved. All the assemblages are et al. 1996). Finally, the abundance of U. jafari, which dominated by small specimens ranging from 3 µm to generally prefers near-shore marine environments and 5 µm and by the presence of U. jafari. Furthermore, in high salinity waters, is consistent with paleoenvironmental the Başyayla section, the genus Discoaster is essentially conditions that prevented the diffusion of discoasterids in absent. These peculiar assemblages were interpreted as the a shallow-water marine environment. The results of the result of environmental filtering (Cosentino et al. 2012). semiquantitative analysis are shown in Table 2, whereas Nevertheless, it is important to note the continuous presence some representative species are shown in Figure 4.
Table 2. Results of the semiquantitative analysis of the calcareous nannofossils assemblages from the Başyayla section. A: abundant (>10 specimens per field of view), C: common (1–10 specimens per field of view), F: frequent (1 specimen per field of view), R: rare (<1 specimen per field of view), VR: very rare (<<1 specimen per field of view). Samples H. carteri H. intermedia H. stalis S. abies R. pseudoumbilicus spp. Reticulofenestra jafari U. C. pelagicus Dictyococcites spp. spp.Pontosphaera
BAS 1 ------BAS 2 R - VR R R A C VR A VR BAS 3 R - R R VR C F R C VR BAS 4 - - R VR R A C VR A VR BAS 5 ------BAS 6 F VR R VR VR C C VR C R BAS 7 R - R - R A F - C - BAS 8 F - R F R C F F C - BAS 9 R VR R R R C F VR C VR BAS 10 R VR - VR VR F F F C R BAS 11 R - VR - VR C C R C - BAS 12 F R C - F C C F C - BAS 13 R - VR R F C F VR C - BAS 14 VR - VR - VR R F - C - BAS 15 VR - R - R F C - C - BAS 16 R VR F R F C F - C VR BAS 17 ------BAS 18 ------BAS 19 - - - VR VR R F - F - BAS 20 VR - R VR R F F VR C - BAS 21 R VR R R R C F - C - BAS 22 VR - R - VR F F - C VR BAS 23 VR - R R R F C R C - BAS 24 - - R - R F R - C -
831 CIPOLLARI et al. / Turkish J Earth Sci
Following the calcareous nannofossil assemblages cycles) (Figure 6). In the Mut-Ermenek Basin, at least in found in the Başyayla section, the study section should the Olukpınar slope-to-basin depositional environment, be placed no earlier than within subzone MNN8b (early this second-order cycle ended in the late Serravallian with Tortonian). The total absence of discoasterids due to the progradation of shallow-water limestones, including unfavorable paleoenvironmental conditions prevents foramol/bryomol and rhodalgal/coralgal limestones application of calcareous nannofossil zonation for more (Mut Formation), onto deeper marine marly deposits, precisely constraining the age of the study section. Looking containing mainly planktonic foraminifera and sponge at the planktonic foraminifera assemblages, the occurrence spicules (Köselerli Formation) (Figure 2B). of both Catapsidrax parvulus and Globigerinoides extremus A similar change in the Middle Miocene depositional allowed Cosentino et al. (2012) to limit the upper part environments of the Mediterranean Basin happened of the Başyayla section to the late Tortonian (MMi 12a in the central Apennine foreland domain (western biozone, 8.35–7.81 Ma). Mediterranean) close to the MNN5/MNN6 transition. In that area, foramol/bryomol and rhodalgal limestones 5. Discussion (Calcari a Briozoi e Litotamni Formation) prograded 5.1. Interpretation of cyclicity in the Mut-Ermenek Basin extensively onto slope-to-basin marls rich in planktonic The marine sediments onlapping the basement rocks of foraminifera and sponge spicules (Spongolitic Unit), the Central Taurides were deposited in the postorogenic also containing debris flows and slumpings (Cosentino phase of the Tauride orogeny, during a quiescent tectonic et al. in press). This paleoenvironmental change, which period. As a result, any transgressive–regressive cycles happened at the same time both in southern Turkey and in in the stratigraphy of the Mut-Ermenek Basin should central Italy, points to a late Serravallian regressive event mainly correspond to relative sea-level changes induced throughout the Mediterranean Basin. by eustatic cycles and sediment supply (Bassant et al. 2005; Considering the age of the lower boundary of the Janson et al. 2010). MNN5a subzone (~15.6 Ma) and that of the upper In this framework, the marine succession of the Mut- boundary of the MNN6b subzone (~11.9 Ma), the Ermenek Basin (Mut and Köselerli formations) was at least biochronological constraints from the Olukpınar section in part deposited in an overall late Burdigalian-Serravallian point to a maximum time span of 3.7 Myr (Figure 5). transgressive–regressive cycle (TB2 supercycle, second- Compared to the Neogene global sea level curve and order cycle, Haq et al. 1988), characterized by high- coastal onlaps of Snedden and Liu (2010) (Figure 6), this frequency sea-level and coastal-onlap changes (third-order time interval contains 2 complete third-order cycles (TB2.4 S
Y SEQUENCE COASTAL ONLAPS ON TERMINOLOGY AGE CHRONOSTRATIGRAPHY Landward Basinward SEA-LEVEL CHANGE
(Ma) STUD Haq et al. Hardenbol et al. ECTI
S (1988) (1998) 0.5 0.0 100 0 -100m 5.33 5.55 TB3.3 Me1 Present day Messinian Başyayla sea-level 7.25 section 7.16 TB3.2 TB3.2 Tor2 9.32 10 Tortonian TB3.1 Tor1 11.61 11.79 Olukpınar Ser3 section TB2.6 12.76 Serravallian TB2.5 TB2.5 Ser2 13.82 13.65 TB2.4 TB2.4 Lan2/Ser1 Langhian 14.78 15.97 TB2.3 TB2.3 Bur5/Lan1 Major relative 16.38 Bur4 sea-level TB2.2 change 17.25 Bur3 Burdigalian 18.49 TB2.1 Bur2 Minor relative Long-term sea-level 19.19 trend 20 Bur1 change 20.43 20.43
Figure 6. Diagram showing the position of the study sections within a global scheme for Neogene sequences, coastal onlaps, and sea-level changes. Coastal onlaps and sea-level changes are from Snedden and Liu (2010). The magnitudes of sea-level change follow the estimation of Hardenbol et al. (1998). The sequence boundary have been recalibrated by Snedden and Liu (2010) following the geological time scale from Gradstein et al. (2008).
832 CIPOLLARI et al. / Turkish J Earth Sci and TB2.5) and part of the TB2.3 and TB2.6 cycles, at the The upper Tortonian marine deposits of the Başyayla base and the top of the Olukpınar section, respectively. section, which at ~8 Ma recorded a progradational event of However, taking into account the occurrence of the debris shallow water foramol/bryomol and rhodalgal limestones flows, which we interpret as related to falling stage system onto offshore or intraplatform marls, containing tracts (FSSTs), and the Köselerli/Mut transition within the mollusks, bryozoans, ostracods, benthonic and planktonic Olukpınar section, which we relate to a transgressive-to- foraminifera, and calcareous nannofossils (Cosentino highstand transition, only 2 boundaries of the third-order et al. 2012), are the upper part of a younger third-order sequence are recorded in the study section: TB2.3/TB2.4 cycle (TB3.2, Haq et al. 1988; Figure 6). In particular, the and TB2.4/TB2.5 (Figure 6). According to Snedden and Başyayla section corresponds to the TST/HST transition Liu (2010), the TB2.3/TB2.4 sequence boundary (14.78 of the TB3.2 sequence. The TB3 supercycle started in the Ma) corresponds to a major relative sea-level drop, whereas earliest Tortonian (Figure 6), just after a major sea-level the younger TB2.4/TB2.5 sequence boundary (13.65 Ma) drop at the end of the Serravallian (TB2.6/TB3.1 transition, corresponds to a minor relative sea-level change. 11.79 Ma; Snedden & Liu 2010). The glacioeustatic sea- Interestingly, the debris flows at the base of the level lowstand at the base of cycle TB3.1, which marks TB2.4 and TB2.5 sequences in the Olukpınar section the Serravallian/Tortonian transition, coincides with the show different thicknesses likely related to the different Mi-5 isotope event and the deep-sea hiatus NH4 (Hilgen amounts of sea level drop responsible for the genesis of et al. 2005). This hiatus should also be present in the Mut- those sequence boundaries (Figure 7). The MNN5/MNN6 transition at 13.6 Ma, which occurs at ~67 m of depth Ermenek Basin somewhere between the Olukpınar and within the uppermost debris flow of the Olukpınar section Başyayla sections. (Figure 7), supports the notion of a debris flow triggered Unfortunately, in the marine sections sampled in the by the sea-level drop that occurred globally at 13.65 Mut-Ermenek Basin, we missed the Serravallian/Tortonian Ma (TB2.4/TB2.5 sequence boundary, Figure 6). In the transition (11.61 Ma), which, according to Snedden and Mut-Ermenek Basin, 2 similar debris flow and slumping Liu (2010), happened very close to one of the major global deposits were reported by Bassant et al. (2005) within the ocean sea-level drops (~70 m) that occurred during the upper Burdigalian marine deposits of the Mut succession Miocene. This major sea-level drop, which occurred in (MNN4 calcareous nannofossil biozone). However, the latest Serravallian (11.79 Ma), corresponds to the although according to the authors those debris flows were TB2/TB3 transition of the supercycles of Haq et al. (1988) triggered by 2 Burdigalian sea level falls, they were related (Figure 6). Although we did not recognize any exposure to the late highstands of 2 different sequences, instead of surface or forced regression facies corresponding to the their relative falling stages. TB2/TB3 transition in the Mut-Ermenek Basin (possibly Although mass gravity flows and related deposits due to bad exposure of the corresponding stratigraphical could be triggered by different processes (e.g., margin interval or unsuitable facies), in the Adana Basin, a well- oversteepening during sea-level highstands, seismic developed erosional surface due to a relative sea-level drop activity, or erosion during sea level lowstands), the most characterizes the top of the Serravallian Güvenç Formation. common process for triggering mass gravity flow on the Along the erosional surface, the early Tortonian terrestrial slope is a relative sea-level fall with erosion of the basin red beds of the Kuzgun Formation rest unconformably on margins (Handford & Loucks 1993; Scheibner et al. 2000, the outer shelf clays and marls of the Güvenç Formation 2003; Drzewiecki & Simó 2002 and references therein; (Ünlügenç 1993). This erosional surface could be linked, Warrlich et al. 2002; Bosence & Wilson 2003). Debris flows at least in part, to the sea-level drop that happened during related to sea-level falls have been identified from different the latest Serravallian at the TB2/TB3 transition (Snedden basins, from the Cambrian up to the Miocene (Drzewiecki & Liu 2010). & Simó 2002 and references therein). Scheibner et al. (2000, 2003), working on slope sediments of a Paleocene 5.2. The Olukpınar and Başyayla sections in the Middle- ramp-to-basin transition in NE Egypt, reported Late Miocene platform-basin system of the Mut-Ermenek depositional facies quite similar to the facies recognized at Basin the Olukpınar section, with hemipelagic marls and debris Both of the sections that we sampled in the Mut-Ermenek flow deposits that were related to transgressive/highstand Basin pertain to a complex platform-basin system. In and lowstand phases, respectively. According to our age particular, according to the age model provided in this model for the Olukpınar section, derived from an updated paper for the Olukpınar section, the analyzed deeper biostratigraphical scheme for nannofossils (Fornaciari marine sediments of the Köselerli Formation, which point et al. 1996), and the global/regional cyclicity of sea-level to a basin-to-slope environment, are temporally equivalent changes, the debris flows recognized at the Olukpınar to the shallow-water limestones of the Ermenek Platform section may be related to different phases of sea level fall. (Janson et al. 2010) (Figure 7). These Langhian-Serravallian
833 CIPOLLARI et al. / Turkish J Earth Sci
13.6 Ma 15.6 Ma NN6 NN5 NN4 rm fo at n et al., 2010) so an Ermenek Pl (J 0 50 300 250 200 150 100
<15.6 Ma 13.1 Ma 13.6 Ma 14.4 Ma
MNN6b MNN6a MNN5b MNN5a
T FSS T HS FSST T HS T TS T LS ST TT n LS
SB SB B2.5 T TB2.4 sectio per) (this pa Olukpınar 0
30 20 10 60 40 70 50 80 90
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a yl tino et al şya B T Ba 0 osen 50 40 30 20 10
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& igra Okada at CN7 CN4
CN9 CN2 CN8 CN3 us nannofossils
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NN5 NN4 NN9 NN8 NN7 NN3
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C5A ty ri la Po
a) (M e TNTS 2004 Ag A 8 9 11 17 12 10 13 14 19 15 16 18 2010). PLT: 2010). PLT: al. et (Janson platform the Ermenek section for the composite sections) and Olukpınar sections and (Başyayla the study among panel 7. Correlation Figure tract, TST: systems lowstand LST: boundary, sequence SB: deeper deposits, slope-to-basin marine STB: deeperdeposits, marine intraplatform INT: platform; carbonate tract. systems highstand tract, HST: systems transgressive
834 CIPOLLARI et al. / Turkish J Earth Sci deeper marine marls of the Köselerli Formation extensively In the carbonate succession of the Ermenek platform, crop out to the south and to the west of Ermenek in the which was the shallow-water counterpart of the Olukpınar Olukpınar and Başyayla areas, respectively. Thus, the deeper water marine succession, based on the depositional extent of the Miocene carbonate platform in those areas, as geometries and the vertical and lateral facies variation, suggested by many authors (Gedik et al. 1979; Şenel 2002; Janson et al. (2010) distinguished 2 large-scale sequences Ulu 2002; Bassant et al. 2005; Janson et al. 2010; Pomar et that may be correlated with the large-scale cycles that we al. 2012), should be greatly revised for this time interval, suggest for the Olukpınar section (Figure 7). since those maps mainly depict the area of the deeper 5.3. Age constraints from the Mut-Ermenek Basin for marine marls as within the younger Serravallian carbonate the uplift of the CAP southern margin platform. The calcareous nannofossil biochronology of the Mut- The long-term transgressive–regressive cycle of the Ermenek Basin presented here confirms the Langhian- Olukpınar section, which corresponds to the middle- upper part of the TB2 supercycle of Haq et al. (1988) Serravallian age (MNN5-MNN6 biozone) for the majority (Figure 6), can be subdivided into at least 2 cycles of of the marine sediments onlapping the southern margin 106-year scale based on the occurrence of 2 thick debris of the CAP, already provided from previous work on flow deposits (debris flows 2 and 4), containing shallow different sections of the same area (Janson et al. 2010). In water components derived from the edge of a carbonate this paper, adopting an updated biostratigraphical scheme platform. At that time, a composite platform system was for reference (Fornaciari et al. 1996), we were also able to developing to the north of the Olukpınar area (Ermenek identify the calcareous nannofossil subzone within the platform, Janson et al. 2010). The N-S channel axes of these MNN5-MMN6 interval (MNN5a, MNN5b, MNN6a, and remobilized carbonate sediments imply that shallow-water MNN6b), allowing us to better constrain the age of the carbonate debris flowed from north, which is consistent Olukpınar section and to improve the possible correlations with the facies distribution of the platform-basin system among other Middle Miocene deeper marine sections in of the Middle Miocene Mut-Ermenek Basin (Janson et al. the Mediterranean Basin. 2010). In the Mut-Ermenek Basin, a younger sedimentary The debris flow deposits intercalated within the deeper cycle showing a transgressive–regressive trend was marine marls of the Köselerli Formation are interpreted as recognized at the top of the marine succession cropping strictly linked to the sea-level drops that happened during out in the vicinity of the town of Başyayla (Cosentino the middle Langhian (14.78 Ma) and the early Serravallian et al. 2012). In the Başyayla section, the presence of (13.65 Ma) (Figure 6). As stated before, according to the Helicosphaera stalis throughout the analyzed succession age model presented in this paper, these 2 cycles of 106- implies that the youngest marine deposits capping the year scale (third-order cycles) correspond to the TB2.4 Tauride basement rocks at the southern margin of the and TB2.5 cycles of Haq et al. (1988). In each 106-year- CAP are at least as young as early Tortonian (MNN8b). scale cycle recognized in the Olukpınar section, the debris According to Cosentino et al. (2012), planktonic flow deposits (FSSTs) together with the less distinguishable foraminifera and magnetostratigraphy tightly constrain sediments of the lowstand systems tract (LST) pass the upper part of the section to the interval of 8.35–8.108 upwards into marls with planktonic foraminifera and Ma (late Tortonian), constraining the uplift of the CAP sponge spicules, which could be generally related to a long southern margin at a post-8 Ma age. period of sea-level rise, containing both the transgressive The youngest portion of the late Tortonian sedimentary systems tract (TST) and the highstand systems tract cycle recognized in the Başyayla section was recently (HST). A hiatus could be interpreted at the TB2.4/TB2.5 found in the Beyşehir area (Sarıalan section, Deynoux et transition, due to the erosional character of the bottom al. 2005; Flecker et al. 2005; Schildgen et al. 2012b), where of the debris flow deposits and the removal of some HST above upper Tortonian deeper marine sediments lower deposits of the TB2.4 cycle. The HST of the younger third- Messinian shallow-water marine deposits constrain the order cycle (TB2.5) contains shallow-water limestones, onset of surface uplift in a period younger than 6.7 Ma such as coral boundstones and red algae bindstones, (early Messinian) (Schildgen et al. 2012b). very similar to the Serravallian shallow-water limestones at the top of the Ermenek platform (Janson et al. 2010). 5.4. Middle-Late Miocene paleogeography of the Eastern The occurrence of shallow water limestones on top of the Mediterranean Basin in southern Turkey Serravallian deeper water marls of the Köselerli Formation In southern Turkey, following the earlier uplift phase document an infra-Serravallian sea-level highstand, which linked to the central Tauride orogeny, continental induced reduction of the accommodation space and sedimentary basins mainly connected with postorogenic consequent progradation, with forestepping geometries, extensional tectonics developed throughout the southern of the shallow-water sediments toward the slope-to-basin margin of the central Taurides with the deposition of depositional environment. fluvial conglomerates and fine-grained lacustrine deposits
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(Yenimahalle and Fakırca formations in the Mut-Ermenek help to better understand the evolution of the marine Basin, and Karsantı and Gildirli formations in the Adana succession of the Mut-Ermenek Basin onlapping the CAP Basin). Subsequently, during a quiescent tectonic period, southern margin. The Olukpınar section shows calcareous 2 long-term transgressive–regressive cycles (second-order nannofossil assemblages associated with the biozones cycles) were responsible for changing the paleogeography between MNN5a and MNN6b, corresponding to a time of the marginal area of the Eastern Mediterranean Basin. interval between ~15.6 Ma and ~12.5 Ma (late Langhian- The first transgression phase, happening early within the late Serravallian). The section includes deep marine marls TB2 supercycle, started in the late Burdigalian with the and remobilized sediments (debris flow deposits) coming deposition of marine deposits related to the evolution of from the shelf edge of the Middle Miocene Ermenek platform-basin systems in both the Mut-Ermenek Basin platform. (Mut and Köselerli formations; Tanar & Gökçen 1990; The Başyayla section (late Tortonian, ~8 Ma) Şafak et al. 2005) and in the Adana Basin (Karaisalı and corresponds to the youngest sedimentary cycle within the Kaplankaya formations; Gürbüz 1993; Gürbüz & Kelling marine succession onlapping the CAP southern margin. It 1993; Cronin et al. 2000). defines the maximum age in the Mut-Ermenek Basin for The innermost and highest evidence for coastal onlap starting the uplift of the plateau margin. on the basement rocks of the Taurides, indicating a major The marine succession capping the southern margin transgression event, are related to marine deposits pertaining of the CAP was deposited during a quiescent tectonic to the TB3 supercycle (Figure 7). In particular, in the Başyayla period. In this framework, facies changes, forestepping area, the onlap surface of the youngest marine deposits of this geometries, and backstepping geometries are mainly transgressive cycle (late Tortonian, ~8 Ma; Cosentino et al. related to glacioeustatic sea-level changes. The Olukpınar 2012) reaches an elevation of 2 km. Additionally, the upper section correlates with the TB2.4 and TB2.5 cycles, whereas Tortonian-lower Messinian marine succession, recently found the Başyayla section correlates with the TB3.2 cycle. in the Beyşehir area (Sarıalan section, Deynoux et al. 2005; The major transgressive event at the southern margin Flecker et al. 2005; Schildgen et al. 2012b), showing upper of the CAP, which happened within the TB3.2 cycle (late Tortonian shallow-water deposits unconformably overlying Tortonian), brought the coastal onlap of the Mediterranean highly deformed Triassic limestones, indicates a late Miocene Sea toward the interior of the Anatolian Peninsula, almost (late Tortonian) transgression of the Eastern Mediterranean 100 km from the present Eastern Mediterranean coast line. Sea onto the interior of the Anatolian Peninsula, reaching at least the Başyayla and Beyşehir areas. Acknowledgments At that time, before the uplift of the CAP southern This work is part of the Vertical Anatolian Movements margin, the paleogeography of southern Turkey was very Project (VAMP), funded by the TOPO-EUROPE close to the reconstruction at 7 Ma suggested by Schildgen initiative of the European Science Foundation, including et al. (2012b) showing the coastal area of the Mediterranean contribution by the IGAG-CNR (com. TA.P05.009, mod. Sea in the interior of the Anatolian Peninsula, more than TA.P05.009.003) and by the APVV (Agentúra na podporu 100 km inland from its present position. výskumu a vývoja; Slovak Research and Development Agency) (EC–009-07). The manuscript benefited from 6. Conclusions helpful reviews by Taylor Schildgen. We greatly appreciate The stratigraphy and the nannofossil biochronology of the the useful comments and suggestions of Xavier Janson and Olukpınar and the Başyayla sections of southern Turkey 2 anonymous reviewers, which improved the paper.
References
Akay, E. & Uysal, Ş. 1988. Post-Eocene tectonics of the central Taurus Bosence, D.W.J. & Wilson, R.C.L. 2003. Sequence stratigraphy Mountains. Mineral Res. Expl. Bull. 108, 23–34. of carbonate depositional systems. In: Coe, A.L. (ed), The Sedimentary Record of Sea-Level Change. The Open University, Akay, E., Uysal, S., Poisson, A., Cravatte, J. & Müller, C. 1985. Cambridge, 234–256. Stratigraphy of the Antalya Neogene Basin. Bull. Geol. Soc. Turkey 28, 105–119. Bozkaya, Ö. & Yalçin, H. 2000. Very low grade metamorphism of upper Paleozoic-lower Mesozoic sedimentary rocks related to Aksu, A.E., Calon, T.J., Piper, D.J.W., Turgut, S. & Izdar, E. 1992. burial and thrusting in the central Taurus Belt, Konya, Turkey. Architecture of late orogenic Quaternary basins in northeastern International Geology Review 42, 353–367. Mediterranean Sea. Tectonophysics 210, 191–213. Cosentino, D., Miccadei, E., Barberi, R., Basilici, G., Cipollari, P., Bassant, P., Van Buchem, F.S.P., Strasser, A. & Görür, N. 2005. The Parotto, M. & Piacentini, T. In press. Explanatory Notes of the stratigraphic architecture and evolution of the Burdigalian Geological Map of Italy, Scale 1:50,000, Sheet 357-Cittaducale carbonate-siliciclastic sedimentary systems of the Mut Basin, (in Italian). Available at http://www.isprambiente.gov.it/ Turkey. Sedimentary Geology 173, 187–232. Media/carg/note_illustrative/357_Cittaducale.pdf.
836 CIPOLLARI et al. / Turkish J Earth Sci
Cosentino, D., Schildgen, T.F., Cipollari, P., Faranda, C., Gliozzi, Gürbüz, K. & Kelling, G. 1993. Provenance of Miocene submarine E., Hudáčková, N., Lucifora, S. & Strecker, M.R. 2012. Late fans in the northern Adana Basin, southern Turkey: a test of Miocene surface uplift of the southern margin of the Central discriminant function analysis. Geological Journal 28, 277–293. Anatolian plateau, Central Taurides, Turkey. Geological Society Handford, C.R. & Loucks, R.G. 1993. Carbonate depositional of America Bulletin 124, 133–145. sequences and systems tracts—responses of carbonate Cronin, B.T., Gürbüz, K., Hurst, A. & Satur, N. 2000. Vertical and platforms to relative sea-level change. In: Loucks, R.G. & Sarg, lateral organization of a carbonate deep-water slope marginal R. (eds), Carbonate Sequence Stratigraphy; Recent Advances to a submarine fan system, Miocene, southern Turkey. and Applications. American Association of Petroleum Geologists Sedimentology 47, 801–824. Memoir 57, 3–41. Deynoux, M., Çiner, A., Monod, O., Karabıyıkoğlu, M., Manatschal, Haq, B.U., Hardenbol, J. & Vail, P.R. 1988. Mesozoic and Cenozoic G. & Tuzcu, S. 2005. Facies architecture and depositional chronostratigraphy and cycles of sea level change. In: Wilgus, evolution of alluvial fan to fan-delta complexes in the C.K., Hastings, B.S., Kendall, C.G.St.C., Posamentier, H.W., tectonically active Miocene Köprüçay Basin, Isparta Angle, Ross, C.A. & Van Wagoner, J.C. (eds), Sea-Level Changes: An Turkey. Sedimentary Geology 173, 315–343. Integrated Approach. SEPM Spec. Publ. 42, 109–124. Dixon, J.E. & Robertson, A.H.F. 1984. The geological evolution of Hilgen, H., Aziz, H.A., Bice, D., Iaccarino, S., Krijgsman, W., Kuiper, the eastern Mediterranean. Geol. Soc., London, Spec. Publ. 17. K., Montanari, A., Raffi, I., Turco, E. & Zachariasse, W.J. 2005. Drzewiecki, P.A. & Simó, J.A. 2002. Depositional processes, triggering The Global boundary Stratotype Section and Point (GSSP) of mechanisms and sediment composition of carbonate gravity the Tortonian Stage (Upper Miocene) at Monte Dei Corvi. flow deposits: examples from the Late Cretaceous of the south- Episodes 28, 6–17. central Pyrenees, Spain. Sedimentary Geology 146, 155–189 Iaccarino, S.M., Premoli Silva., I., Biolz, M., Foresi, L.M., Lirer, F., Eris, K.K., Bassant, P. & Ülgen, U.B. 2005. Tectono-stratigraphic Urco, E. & Petrizzo, M.R. 2007. Practical manual of Neogene evolution of an Early Miocene incised valley-fill (Derinçay Planktonic foraminifera. International School on Planktonic Formation) in the Mut Basin, Southern Turkey. Sedimentary Foraminifera. VI course: Neogene. Perugia (Italy), 19–23 Geology 173, 151–185. February 2007, 1–181. Faranda, C., Gliozzi, E., Cipollari, P., Grossi, F., Darbaş, G., Gürbüz, Janson, X., van Buchem, F.S.P., Dromart, G., Eichenseer, H.T., K., Nazik, A., Gennari, R. & Cosentino, D. 2013. Messinian Dellamonica, X., Boichard, R., Bonnaffe, F. & Eberli, G. paleoenvironmental changes in the easternmost Mediterranean 2010. Architecture and facies differentiation within a Middle Basin (Adana Basin, Southern Turkey). Turkish Journal of Miocene carbonate platform, Ermenek, Mut Basin, southern Earth Sciences doi:10.3906/yer-1205-11. Turkey. Geological Society, London, Special Publications 329, 265–290. Flecker, R., Poisson, A. & Robertson, A.H.F. 2005. Facies and palaeogeographic evidence for the Miocene evolution of the Jarvis, A., Reuter, H.I., Nelson, A. & Guevara, E. 2008. Hole-Filled Isparta Angle in its regional eastern Mediterranean context. Seamless SRTM Data V4. International Centre for Tropical Sedimentary Geology 173, 277–314. Agriculture (CIAT). Available at http://srtm.csi.cgiar.org (last accessed May 2008). Fornaciari, E., Backman, J. & Rio, D. 1993. Quantitative distribution patterns of selected lower to middle Miocene calcareous Jolivet, L. & Faccenna, C., 2000. Mediterranean extension and the nannofossils from the Ontong Java Plateau. In: Berger, W.H., Africa-Eurasia collision. Tectonics 19, 1095–1106. Kroenke, L.W., Mayer, L.A. (eds), Proceedings of the Ocean Kempler, D. & Ben-Avraham, Z., 1987. The tectonic evolution of the Drilling Program, Scientific Results 130. ODP, College Station, Cyprean arc. Annales Tectonicae 1, 58–71. TX, USA, 245–256. Lourens, L., Hilgen, F., Shackleton, N.J., Laskar, J. & Wilson, J. 2004. Fornaciari, E., Di Stefano, A., Rio, D. & Negri, A. 1996. Middle Appendix 2. Orbital tuning calibrations and conversions for Miocene quantitative calcareous nannofossil biostratigraphy the Neogene Period. In: Gradstein, F.M., Ogg, J.G., & Smith, in the Mediterranean region. Micropaleontology 42, 37–63. A.G. (eds), A Geologic Time Scale 2004. Cambridge University Gedik, A., Birgili, S., Yilmaz, H. & Yoldas, R. 1979. Geology of the Press, Cambridge, 469–471. Mut-Ermenek-Silifke (Konya, Mersin) area and petroleum Martini, E. & Müller, C. 1986. Current Tertiary and Quaternary possibilities. B. Geol. Soc. Turkey 22, 7–26. calcareous nannoplankton stratigraphy and correlations. Görür, N. 1992. A tectonically controlled alluvial fan which developed Newsl. Stratigr. 16, 99–112. into a marine fan-delta at a complex triple junction: Miocene Okada, H. & Bukry, D. 1981. Supplementary modification and Gildirli Formation of the Adana Basin, Turkey. Sedimentary introduction of code numbers to the low-latitude coccolith Geology 81, 245–252. biostratigraphic zonation (Bukry, 1973; 1975). Marine Gradstein, F.M., Ogg, J.G. & Smith, A.G. (eds) A Geologic Time Scale Micropaleontology 5, 321–325. 2004. Cambridge University Press, Cambridge, 469–471. Özgül, N. 1997. Stratigraphy of tectonostratigraphic units in the Gürbüz, K. 1993. Identification and Evolution of Miocene Submarine Bozkir-Hadim-Taskent around northern part of Central Fans, in the Adana Basin, Turkey. PhD, University of Keele. Taurus. Bull. Mineral Res. Explorat. 119, 113–174.
837 CIPOLLARI et al. / Turkish J Earth Sci
Pomar, L., Bassant, P., Brandano, M., Ruchonnet, C. & Janson, X. 2012. Schildgen, T.F., Cosentino, D., Caruso, A., Buchwaldt, R., Yildirim, Impact of carbonate producing biota on platform architecture: C., Bowring, S.A., Rojay, B., Echtler, H. & Strecker, M.R. 2012b. insights from Miocene examples of the Mediterranean region. Surface expression of Eastern Mediterranean slab dynamics: Earth-Science Reviews 113, 186–211. Neogene topographic and structural evolution of the SW margin of the Central Anatolian Plateau, Turkey. Tectonics 31, Raffi, I., Rio, D., d’Atri, A. Fornaciari, E. & Rocchetti, S. 1995. TC2005. Quantitative distribution patterns and biomagnetostratigraphy of Middle and Late Miocene calcareous nannofossils from Şenel, M. 2002. Geological Map of Turkey, Konya (No. 14). Scale Equatorial Indian and Pacific Oceans (Legs 115, 130, and 138). 1:500,000, 1 sheet. Ankara, Turkey, Maden Tetkik ve Arama In: Pisias, N.G., Mayer, L.A., Janecek, T.R., Palmer-Julson, Genel Müdürlüğü (MTA). A. & van Andel, T.H. (eds), Proceedings of the Ocean Drilling Şengör, A.M.C. & Yilmaz, Y. 1981. Tethyan evolution of Turkey: a Program, Scientific Results 138. ODP, College Station, TX, plate tectonic approach. Tectonophysics 75, 181–241. USA, 479–502. Snedden, J.W. & Liu, C. 2010. A compilation of Phanerozoic sea- Robertson, A.H.F. 1998. Tectonic significance of the Eratosthenes level change, coastal onlaps, and recommended sequence Seamount: a continental fragment in the process of collision designations. AAPG, Search and Discovery Article with a subduction zone in the eastern Mediterranean (Ocean #40594. Available at http://www.searchanddiscovery.com/ Drilling Program Leg 160). Tectonophysics 298, 63–82. documents/2010/40594snedden/ndx_snedden.pdf. Robertson, A.H.F. 2000. Tectonic evolution of Cyprus in its Tanar, Ü. & Gökçen, N. 1990. Mut-Ermenek Tersiyer istifinin easternmost Mediterranean setting. In: Panayides, I., stratigrafisi ve mikropaleontolojisi. MTA Dergisi 110, 175–180 Xenophontos, C. & Malpas, J. (eds), Proceedings of the Third (in Turkish). International Conference on the Geology of the Eastern Mediterranean, Geological Survey Department, Republic of Ulu, Ü. 2002. Geological Map of Turkey, Adana (No. 15). Scale Cyprus, 11–44. 1:500,000, 1 sheet. Ankara, Turkey, Maden Tetkik ve Arama Genel Müdürlüğü (MTA). Robertson, A.H.F. & Grasso, M. 1995. Overview of the Late Tertiary- recent tectonic and paleoenvironmental development of the Ünlügenç, U.C. 1993. Controls on Cenozoic Sedimentation, Adana Mediterranean region. Terra Nova 7, 114–127. Basin, Southern Turkey. PhD, University of Keele. Şafak, Ü., Kelling, G., Gökçen, N.S. & Gürbüz, K. 2005. The mid- Warrlich, G.M.D., Waltham, D.A. & Bosence, D.W.J. 2002. Cenozoic succession and evolution of the Mut basin, southern Quantifying the sequence stratigraphy and drowning Turkey, and its regional significance. Sedimentary Geology 173, mechanisms of atolls using a new 3-D forward stratigraphic 121–150. modelling program (CARBONATE 3D). Basin Research 14, 379–400. Scheibner, C., Kuss, J. & Marzouk, A.M. 2000. Slope sediments of a Paleocene ramp-to-basin transition in NE Egypt. International Williams, G.D. & Ünlügenç, U.C. 1992. Structural controls on Journal of Earth Sciences 88, 708–724. stratigraphic evolution of the Neogene Çukurova basin complex. International Workshop on Work in Progress on Scheibner, C., Reijmer, J.J.G., Marzouk, A.M., Speijer, R.P. & Kuss, Geology of Turkey, Abstracts, Keele University England, 79–80. J. 2003. From platform to basin: the evolution of a Paleocene carbonate margin (Eastern Desert, Egypt). International Journal of Earth Sciences 92, 624–640. Schildgen, T.F., Cosentino, D., Bookhagen, B., Niedermann, S., Yildirim, C., Echtler, H.P. & Strecker, M.R. 2012a. Multi-phased uplift of the southern margin of the Central Anatolian plateau, Turkey: a record of tectonic and upper mantle processes. Earth and Planetary Science Letters 317–318, 85–95.
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