Turkish Journal of Earth Sciences Turkish J Earth Sci (2013) 22: 839-863 http://journals.tubitak.gov.tr/earth/ © TÜBİTAK Research Article doi:10.3906/yer-1205-11

Messinian paleoenvironmental changes in the easternmost Mediterranean Basin: Adana Basin, southern Turkey

1 1,2 1,2 1 3 Costanza FARANDA , Elsa GLIOZZI , Paola CIPOLLARI , Francesco GROSSI , Güldemin DARBAŞ , 4 4 5 1,2, Kemal GÜRBÜZ , Atike NAZİK , Rocco GENNARI , Domenico COSENTINO * 1 Department of Geological Sciences, Faculty of Mathematical, Physical, and Natural Sciences, Roma Tre University, Rome, Italy 2 Institute of Environmental Geology and Geoengineering, IGAG-CNR, Rome, Italy 3 Department of Geological Engineering, Faculty of Engineering and Architecture, Kahramanmaraş Sütçü İmam University, Kahramanmaraş, Turkey 4 Department of Geological Engineering, Faculty of Engineering and Architecture, Çukurova University, Adana, Turkey 5 Department of Earth Science, Faculty of Mathematics, Physics, and Natural Science, University of Parma, Parma, Italy

Received: 01.06.2012 Accepted: 28.01.2013 Published Online: 26.08.2013 Printed: 25.09.2013

Abstract: We present detailed Messinian paleoenvironmental reconstructions for the Adana Basin based on a multidisciplinary approach that utilizes the fossil content of the Kuzgun and Handere Formations. To reconstruct the paleoenvironmental changes that affected the Adana Basin during the Messinian, we analyzed mollusk, ostracod, planktonic and benthonic foraminifer, and calcareous nannofossil assemblages from 2 stratigraphic sections near Kabasakal village (Adana, southern Turkey). To determine if the environmental changes recognized in the Adana Basin are local or regional, and to understand the extent to which the global changes in oceanic circulation impacted the Mediterranean sedimentary basins, we compare our results with Messinian sections from other locations in the Mediterranean region (northern Italy, southern Italy, Cyprus, Algeria, and southern Turkey). The occurrence of N. humerosa, G. bulloides, G. woodi, N. acostaensis, N. atlantica (planktonic forams), S. multiflora, T. rugosa, P. elongata, C. scitula, L. lipadusensis (ostracods), R. rotaria, A. primus, and A. delicatus (calcareous nannofossils) allows us to constrain the uppermost part of the Kuzgun Formation to the early Messinian. The ostracod assemblages indicate an enclosed marine environment characterized by sporadic local freshwater inputs that decreased the salinity of the basin. In contrast, in the late Messinian Handere Formation, the presence of Paratethyan ostracods pertaining to the Loxoconcha mülleri zone and to the Loxocorniculina djafarovi zone in the Handere Formation indicates the occurrence of the Messinian brackish water Lago-Mare event in the Adana Basin, which occurred throughout the Mediterranean between 5.60 and 5.33 Ma.

Key Words: Adana Basin, Messinian, paleontology, paleoenvironmental reconstruction, eastern Mediterranean, southern Turkey

1. Introduction in the Adana Basin occurred in the Early Miocene The Adana Basin (Figure 1), which developed during the with deposition of shallow marine clastic sediments Neogene in the easternmost part of the Mediterranean (Aquitanian-Burdigalian, Kaplankaya Formation) on top region, experienced all the main paleoceanographic of Oligocene-Lower Miocene continental sediments. At changes that affected the area during convergence of the the Middle Miocene/Late Miocene transition, the Adana African and Arabian plates with Eurasia (Şengör & Yılmaz Basin recorded a regressive event with the deposition of 1981). The local effects of these regional tectonics, coupled lower Tortonian terrestrial red beds (Kuzgun Formation), with eustatic variations of sea level in the Mediterranean, likely as a result of the uplift of the Bitlis-Zagros collision induced several transgressive/regressive cycles in the Adana zone (Okay et al. 2010) coupled with a major sea-level drop Basin that caused changes from marine to continental at the end of the Serravallian, which coincides with the deposition (Schmidt 1961; Yalçın & Görür 1983; Yetiş & Mi-5 isotope event and the deep-sea hiatus NH4 (Hilgen Demirkol 1986; Ünlügenç & Demirkol 1988; Yetiş 1988; et al. 2005). According to Cipollari et al. (2013) this hiatus Ünlügenç et al. 1991; Nazik & Gürbüz 1992; Gürbüz & could be also present in some places beneath the Başyayla Kelling 1993; Ünlügenç 1993; Williams et al. 1995; Yetiş et section (Mut-Ermenek Basin, southern Turkey; Cosentino al. 1995; Cronin et al. 2000). The first marine transgression et al. 2012b). The uplift of the Bitlis-Zagros collision zone * Correspondence: [email protected] 839 FARANDA et al. / Turkish J Earth Sci

a EUROPE Moncucco 45°N Fanantello Legnagnone Cava Serred Maccarone Black Sea Ma ella Mondragone 40°N ODP 974 Sorbas Torrente Vaccar zzo Malaga N jar ODP 975 Mar anopol Anatol a Western Med terranean Serra P rc ata Sarıalan Chel f Falconara Adana Chabet Bou Seter G bl scem 35°N Crete Tochn DSDP 375-376 Eastern Med terranean ODP 968 P ssour ODP 969 ODP 967

30°N 0 1000 km AFRICA

0°E 10°E 20°E 30°E 37° 18' 29" N 37° 18' 26" N E Black Sea E

17" İstanbul b Ankara 37" 01' STUDY AREA 35° Adana 35°28' 200 km Çatalan Medterranean Sea KarasalıAlluvum (Holocene-Recent)

Calche and Terrace (Upper Plestocene)

Avadan Fm (Lower Zanclean)

Handere Fm (Uppermost Messnan)

Kuzgun Fm wth the Tortonan Salbaş tu (Serravallan p.p.- Messnan p.p.) Güvenç Fm (Burdgalan p.p.- Serravallan p.p.) Cngöz Fm (Burdgalan p.p.) Salbaş Serravallan p.p.) Kaplankaya Fm (Burdgalan p.p.- Langhan p.p.) Karasalı Fm Seyhan (Aqutanan p.p.- dam Tortonan p.p.) E G ld rl Fm E (Aqutanan p.p.) 17" 44" Basement rocks

01' (pre-Olgocene) Fgure 2 ADANA 0 4 km 35°28' 35° 36° 59' 58" N 36° 59' 53" N Figure 1. (a) Location map of the stratigraphic sections discussed in the paper. (b) Geological map of the Adana Basin, with the location of Figure 2 [modified after Yetiş & Dermikol (1986), Unlügenç (1993), and Yetiş et al. (1995)]. cut the Mediterranean off from the Indian Ocean (Şengör A younger paleoceanographic change affected the et al. 1985; Hüsing et al. 2009; Okay et al. 2010), which Mediterranean Basin in connection with the progressive caused abrupt changes in the paleoceanography of the closure of the Gibraltar gateway, which gave rise to the Mediterranean area. Messinian Salinity Crisis (MSC) (e.g., Hsü et al. 1973; Ryan

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2009 and references therein) and the deposition of thick of the region. We compare our reconstructions of the evaporite deposits (mainly gypsum and halite) throughout Messinian paleoenvironmental changes in the Adana the Mediterranean, as far as its easternmost margins (e.g., Basin with other Messinian sections from different parts Adana Basin; Yalçın & Görür 1984). of the Mediterranean area to verify how local or regional Despite the fact that the MSC has been studied since the the environmental changes were in the Adana Basin and 1970s, its causes as well as the mechanisms that controlled to understand the extent to which the global changes in the different MSC stages are still matters of debate. oceanic circulation impacted the sedimentary basins in Cyclostratigraphy and astrochronology helped in defining the Mediterranean realm. a precise temporal evolution of the crisis, especially for its onset and for evaluating the ~90 k.y. Messinian 2. Geological setting gap (Krijgsman et al. 1999; Hilgen et al. 2007), which 2.1. Stratigraphy of the Adana Basin corresponds to the Messinian Erosional Surface (MES) The Adana Basin is located on the southeast margin of the that separates the 2 main steps of the MSC (i.e. Lower and Anatolian Peninsula and represents the onshore portion Upper Evaporites). Recently, using both cyclostratigraphy of the Adana-Cilicia Basin (Aksu et al. 2005), a subsiding and high-precision CA-TIMS U-Pb geochronology on region at the southern margin of the Central Anatolian single zircon grains, the Messinian gap was refined to at Plateau (Figure 1). According to Robertson (1998), the most 28 or 58 ± 9.6 k.y. (Cosentino et al. 2013). Adana-Cilicia Basin developed in a region of extensional Over the last decade, several models of the tectonics caused by the southward retreat of the African major paleoenvironmental changes that affected the slab. The Adana Basin developed on Tauride basement Mediterranean Basin during the MSC have been created rocks mainly in Neogene times and records the main by means of water budget variations (Meijer & Krijgsman tectonosedimentary events related to the interplay of the 2005; Blanc 2006; Topper et al. 2011). At the same time, the African plate with the Arabian and Anatolian microplates. scientific community that has been working on the MSC The base of the Adana Basin succession consists of reached a general consensus on a model for distinguishing Oligocene-Lower Miocene fluvial red beds and lacustrine the different steps of the crisis and the consequent late deposits (Karsantı intramontane basin deposits and Messinian paleoenvironmental changes (CIESM 2008). Gildirli Formation; Schmidt 1961; Görür 1979; Yetiş Some of the major depositional events connected 1988; Ünlügenç et al. 1991, 1993; Gürbüz & Kelling with the MSC in the Mediterranean Basin were recently 1993; Yetiş et al. 1995), which lie unconformably on the recognized in Messinian deposits of the Adana Basin Tauride basement rocks. The shallow marine Kaplankaya (Handere Formation) by Cosentino et al. (2010a, 2010b) Formation (Aquitanian-Burdigalian) records the first and Cipollari et al. (2012). Additional paleoenvironmental marine transgression in the Neogene Adana Basin. changes affected the easternmost Mediterranean area The coarse-grained marine deposits of the Kaplankaya during the late Miocene as a result of the uplift of the Formation are heteropic with the Gildirli red beds, the southern margin of the Central Anatolian Plateau (CAP) Karaisalı reef limestones, and the lower part of the deeper (Cosentino et al. 2012b) coupled with the effects of the marine Cingöz Formation (Gürbüz & Kelling 1993). The MSC. The uplift of the southern margin of the CAP, which Cingöz Formation (Schmidt 1961), which was deposited began in the late Messinian and likely continues to the during the late Burdigalian-early Serravallian (Nazik & present (Schildgen et al. 2012a, 2012b), greatly modified Gürbüz 1992), is a turbidite fan system (Görür 1979; Yetiş the depositional environments of the Adana Basin and & Demirkol 1986; Ünlügenc & Demirkol 1988; Yetiş 1988; induced uplift or subsidence in different parts of the basin. Ünlügenç et al. 1991; Gürbüz & Kelling 1993; Ünlügenç In this paper, we present detailed Messinian 1993; Williams et al. 1995; Yetiş et al. 1995) that developed paleoenvironmental reconstructions of the Adana Basin on the northwest margin of the Adana Basin. using a multidisciplinary approach to analyze the fossil The fine-grained deep marine basin floor deposits of content of the Kuzgun and Handere Formations. To the Güvenç Formation (Serravallian) are heteropic with reconstruct the paleoenvironmental changes that affected upper Cingöz fan turbidites and pass upsection to shallow the Adana Basin during the Messinian, we analyzed mollusk, marine outer shelf clays and marls (Ünlügenç et al. 1991; ostracod, planktonic and benthonic foraminifer, and Nazik & Gürbüz 1992; Gürbüz & Kelling 1993; Ünlügenç calcareous nannofossil assemblages from 2 stratigraphic 1993). The early Tortonian continental deposits of the sections approximately 6 km northwest of the city of Kuzgun Formation lie unconformably on the fine-grained Adana in the vicinity of Kabasakal village (Figures 1 and 2). marine deposits of the Güvenç Formation (Ünlügenç The MSC was a crucial event in the Mediterranean Basin 1993). and was characterized by paleoenvironmental changes A second transgressive event occurred in the Adana linked to important variations in the paleoceanography Basin in the middle Tortonian with the deposition of

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37° 04’ 15” N . . . 68 100 65 . a . 80

35°13 ’ 35 ” E 118

. 70 . Lake 90 . . . 65 79 100 . 130 Alluv al cover . 140 . 117 2 RLE

Kuzgun Fm . 110 3 . . 125 110 1 MES . . 110 135 . Fault 118 N E

500 m 17” 1 Sect on 35°15’ 37° 03’ 24” N

3 Adana 50 1 Sem ram s ADA 40 Explanat on 55 45 ADA 35 SEM 25 Marl SEM 24 50 SEM 23 40 ADA 30 SEM 22 Gypsum rud te 45 SEM 21 35 SEM 20 SEM 19 ADA 25 40 Calcareous marl SEM 18 30 SEM 17 35 SEM 16 25 S lt/Sand SEM 15 30 SEM 14 20 SEM 13 ADA 20 25 SEM 12 15 MES SEM 11 ADA 15 SEM 10 ADA 10 20 10 SEM 9 SEM 8 ADA 5 15 SEM 7 5 ADA 1 SEM 6 2 10 m0 Adana-1 SEM 5 MES SEM 4 ADA1 14 ADA1 15 5 SEM 2 10 ADA1 19 SEM 1 ADA1 20 m 0

5 ADA1 10 ADA1 5 m0 ADA1 1 b

Figure 2. (a) Geological map of the study area, with the location of the analyzed sections (1- Semiramis section; 2- Adana-1 section; 3- Adana section). RLE = resedimented lower evaporites; MES = Messinian Erosional Surface. (b) Stratigraphic logs of the analyzed sections. MES = Messinian Erosional Surface.

842 FARANDA et al. / Turkish J Earth Sci shallow marine sediments of the Kuzgun Formation. The Adana section is 50 m thick and consists mainly of According to the classic Late Miocene stratigraphic fine-grained deposits (marls) and several thick layers of scheme for the Adana Basin, fluvial and shallow marine resedimented evaporites (Gökkuyu Gypsum member). deposits of the Handere Formation, including gypsum The evaporites consist mainly of gypsum rudites made layers (Gökkuyu Gypsum member; Yetiş & Demirkol up of selenite fragments and include differently sized 1986; Yetiş 1988; Yetiş et al. 1995), rest conformably on gypsum clasts and large blocks of banded selenite. These the marine deposits of the Kuzgun Formation (Gürbüz & characteristics suggest debris-flow processes during the Kelling 1993; Yetiş et al. 1995; Nazik 2004; Darbaş & Nazik deposition of the lower portion of the Handere Formation. 2010), suggesting a Late Miocene-Pliocene regressive In the Mediterranean stratigraphy of the MSC (CIESM cycle. Recently, Cosentino et al. (2010a, 2010b) and 2008), the resedimented evaporites (Resedimented Lower Cipollari et al. (2012) suggested a different interpretation Evaporites, RLEs) are from the lower part of the second for the Handere Formation, especially for the Kuzgun/ step of the salinity crisis (5.60–5.55 Ma) and lie just above Handere boundary and the chronology of the Handere the MES. We collected 42 samples from the fine-grained Formation. The differences with the classic stratigraphic deposits of the Adana section for micropaleontological scheme for the Upper Miocene-Pliocene deposits of the analyses (samples ADA 1–42). The field investigations did Adana Basin (Yetiş & Demirkol 1986; Yetiş 1988; Gürbüz & not show any fossils within the fine-grained deposits of the Kelling 1993; Yetiş et al. 1995; Nazik 2004; Darbaş & Nazik Adana section. 2010) are: 1) the unconformable nature of the Kuzgun/ 2.3. The Semiramis section Handere boundary, corresponding to the MES; 2) the stratigraphical position of the Gökkuyu Gypsum member, The Semiramis section was studied by Darbaş and Nazik which is at the base of the Handere Formation, instead (2010) and is located close to both the Adana and Adana-1 of near the top as suggested by Yetiş (1988) and Yetiş et sections (Figure 2). According to Darbaş and Nazik (2010), al. (1995); 3) the unconformable nature of the boundary the Semiramis section, which is 55 m thick, encompasses between the Gökkuyu Gypsum member and the fluvial the Kuzgun/Handere transition, which was interpreted as a conglomerates and marls of the Handere Formation; conformable boundary. In the Semiramis section, as in the 4) the upper Messinian age of the Handere Formation; Adana-1 section, the Kuzgun Formation is characterized and 5) the stratigraphical transition between the fluvial by fine-grained marine deposits with intercalated sandy conglomerates and marls of the Handere Formation layers. The micropaleontological analyses performed by and the deep marine Zanclean clays that crop out in the Darbaş and Nazik (2010) on samples from the Kuzgun Avadan area (Cipollari et al. 2012). Formation (SEM 1–11, Figure 2) show a rich microfauna of mainly marine ostracods and planktonic foraminifers. In 2.2. The studied sections The stratigraphic sections that we analyzed in this study are contrast, and similar to the Adana section, the fine-grained located in the central part of the Adana Basin approximately samples collected from the Handere Formation (Gökkuyu 6 km northwest of the city of Adana near Kabasakal village Gypsum member), which begins with a 3.5-m-thick layer (Figure 1). In that area, the boundary between the Kuzgun of resedimented evaporites, are mainly barren of fossils. and Handere Formations is well exposed in several places In this paper, we compare the results of the (Figure 2). As in most of the Adana Basin, the Kuzgun/ micropaleontological analyses from the Adana and Handere boundary corresponds to the MES (Cosentino et Adana-1 sections with those from the Semiramis section al. 2010a, 2010b; Cipollari et al. 2012), which was formed to better understand the temporal progression of the Late by the lowering of the sea level in the Mediterranean during Miocene paleoenvironmental changes that affected the the MSC. Northeast of Kabasakal village, the Kuzgun easternmost Mediterranean Basin. Formation is mainly characterized by shallow marine deposits, including calcareous marl, silt, and sandy layers 3. Material and methods with mollusk-bearing horizons. We sampled a 13-m thick Twenty-two samples from the Adana-1 section and 42 section from the uppermost part of the Kuzgun Formation samples from the Adana section were investigated for (Adana-1 section; Figure 2). The Adana-1 section consists paleontological content, including analyses of planktonic mainly of fine-grained marine deposits with intercalations and benthic foraminifers, ostracods, and calcareous of 2 massive sandy layers. We collected 22 samples (ADA nannofossils. Benthic and planktonic foraminifers of the 1 1–22) from the Adana-1 section, mainly from the Adana-1 section were studied using semiquantitative fine-grained deposits. Field investigations showed the analysis on the >125 µm fraction, which was divided to occurrence of planktonic and benthic foraminifers with obtain approximately 0.1 g of dry residue. Planktonic marine mollusks (mainly gastropods). and benthic specimens were picked in 9 of 45 fields of a Near the Adana-1 section, we sampled the lowermost standard picking tray. The count was normalized to one part of the Handere Formation (Adana section; Figure 2). field to obtain relative abundance variations throughout

843 FARANDA et al. / Turkish J Earth Sci the stratigraphic column. Ostracods were handpicked Reticulofenestra spp. (including all the species smaller than from the >125 µm fraction, identified, and counted. Their 7 µm) are the most abundant in all the assemblages, but it is frequencies were normalized to 10 g of dry residue. worth noting the common occurrence of Reticulofenestra Preparation of the smear slides for light microscope rotaria and the presence of Amaurolithus primus and A. analysis of calcareous nannofossils followed standard delicatus in sample ADA-1 4 (Figure 3). techniques. The abundances of selected calcareous Planktonic foraminifers are scarce (less than 5 nannofossil taxa were determined by light microscope specimens/field) in the Adana-1 section. The assemblages (transmitted light and crossed nicols) at approximately from the sandy layers are generally small, and at least 1200× magnification. some of them could be reworked. This is suggested in The relative abundance of each species was classified as sample ADA-1 20 by the presence of Paragloborotalia follows: A = Abundant: more than 10 specimens of a single partimlabiata, which is a Serravallian marker. The species per field of view; C = Common: 1–10 specimens planktonic specimens recovered from the marls lack per field of view; F = Few: 1 specimen per 2–10 fields of any evidence of reworking from older strata. Among view; R = Rare: 1 specimen per 11–100 fields of view; V = others, Globigerina bulloides, Globigerinella obesa, Very Rare: 1 specimen per 101–1000 fields of view; and B Neogloboquadrina atlantica, Neogloboquadrina acostaensis = Barren: barren of indigenous nannofossils. sinistrally coiled, and Turborotalita quinqueloba have been The preservation of the nannofossil assemblages was identified. Benthic foraminifers are common to abundant classified as follows: G = Good preservation: little or no (10 to 40 specimens/field) in the marly layers (Figure 4), evidence of dissolution and/or secondary overgrowths of and decrease to less than 5 specimens/field in the sandy calcite, and the diagnostic features are fully preserved and layers. Overall, abundance increases from the bottom to all specimens can be identified; M = Moderate preservation: the top of the section, while species diversity remains low. dissolution and/or secondary overgrowths partially alter The most abundant species is Ammonia beccarii (up to 32 the primary morphological characteristics, but nearly all specimens/field), which is always present and dominant specimens can be identified to the species level; P = Poor in a poorly diversified assemblage. Cribroelphidium preservation: severe dissolution, fragmentation, and/ decipiens and Quinqueloculina (Q. oblunga, Q. seminulum, or secondary overgrowths have destroyed the primary and Quinqueloculina sp.) are quite common (Figure 5). features, and many specimens cannot be identified to the Other taxa, such as Florilus boueanum and Bulimina elongata, occur throughout the entire section with very species or even genera level. low abundance. Bolivina spp., Elphidium macellum, Paleoenvironmental analyses, as the physiochemical Epistomella sp., Gyroidina sp., Oridorsalis sp., Pullenia conditions (e.g., paleosalinity, paleodepth, bulloides, Sigmoilinita tenuis, Trifarina bradyi, and paleotemperatures, depositional substratum) of the Uvigerina peregrina are rare and scattered along the section. environment where the fauna lived, were carried out Marine ostracods are present in almost all the samples on foraminifers and ostracods through the community (Table 1; Figures 6 and 7) with different frequencies. structure indexes (Margalef, Shannon, evenness) and the Neomonoceratina laskarevi, Phlyctenophora farkasi, and Q-mode hierarchical cluster analysis (Morisita–Horn Xestoleberis tumida are by far the dominant species in the distance measure and the unweighted pair group method assemblages (Figure 5), along with subordinated Senesia using the arithmetic average [UPGMA]) using the software cf. S. philippi, Callistocythere quadrangula, Cytherelloidea package PAST - PAleontological STatistics (version 2.12; petrosa, Cytheridea zahorica, and Occlusacythereis occlusa. Hammer et al. 2001). Other species, such as Ionicythere reticulata, Callistocythere skeletrum, Keijella punctigibba, Loxoconcha lipadusensis, 4. Results and Loxoconcha ovulata, are rare and are scattered along 4.1. The Adana-1 section the section. Few mollusks are present in the lower portion The Adana-1 section (Kuzgun Formation) is characterized of the Adana-1 section (Table 1; Figure 8), particularly in by the presence of planktonic and benthic foraminifers, sample ADA-1 5, where 2 bivalves (Anadara turoniensis ostracods, mollusks, and calcareous nannofossils (Table and Dosinia lupinus) and 5 gastropods (Athleta rarispina, 1). Calcareous nannofossil assemblages are scarce in Hexaplex austriacus, Nassarius mutabilis, Clavatula most cases, and several samples are barren of indigenous calcarata francisci, and Clavatula jouanneti) were nannofossils; the preservation is generally moderate. Only identified. They are absent upsection from sample ADA-1 one sample, from the lower part of the section, shows 6 except for the topmost sample (ADA-1 14), where Ostrea a very abundant and well-preserved assemblage. The is abundant. relative abundances detected for each species are shown Community structure indexes calculated for the in Table 2. The long-ranging species, such as Dictyococcites benthic foraminifer and ostracod assemblages (Figure spp., Coccolithus pelagicus, Helicosphaera carteri, and 9) show relatively high frequencies in the marly layers,

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Table 1. List of the fossils collected in the Semiramis, Adana-1, and Adana sections. * = Carinocythereis carinata in Darbaş and Nazik (2010).

ADANA SECTION Globoturborotalita decoraperta (Takayanagi and Saito, 1962) Benthic foraminifers Globoturborotalita sp. Ammonia beccarii (Linnaeus, 1758) Neogloboquadrina acostaensis (Blow, 1959)sx Neogloboquadrina cf. N. acostaensis (Blow, 1959)dx Ostracods Neogloboquadrina atlanticaBerggren, 1972 Cyprideis agrigentina Decima, 1964 Orbulina universa d’Orbigny, 1839 Loxoconcha mülleri (Méhes, 1908) Turborotalita quinqueloba (Natland, 1938) Euxinocythere (Maeotocythere) praebaquana (Livental in Agalarova et al., 1940) Benthic foraminifers ADANA-1 SECTION Ammonia beccarii (Linnaeus, 1758) Calcareous nannofossils Bolivina spathulata (Williamson, 1858) Amaurolithus primus (Bukry and Percival, 1971) Bolivina sp. Gartner and Bukry, 1975 Amaurolithus delicatus Gartner and Bukry, 1975 Bulimina elongata d’Orbigny, 1826 Amaurolithus primus/delicatus intergrade Cribroelphidium decipiens (Costa, 1956) Calcidiscus macintyrei (Bukry and Bramlette, 1969) Elphidium macellum (Fichtel and Moll, 1798) Loeblich and Tappan, 1978 Calcidiscus leptoporus (Murray and Blackman, 1898) Epistomella sp. Loeblich and Tappan, 1978 Coccolithus pelagicus (Wallich, 1877) Schiller, 1930 Florilus boueanum (d’Orbigny, 1846) Dictyococcites spp. Gyroidina sp. Discoaster asymmetricus Gartner, 1969 Oridorsalis sp. Discoaster brouwerii Tan, 1927, emend. Bramlette and Riedel, 1954 Quinqueloculina oblunga (Montagu, 1803) Discoaster pentaradiatus Tan, 1927 Quinqueloculina seminulum (Linnaeus, 1758) Discoaster surculus Martini and Bramlette, 1963 Quinqueloculina sp. Discoaster variabilis Martini and Bramlette, 1963 Pullenia bulloides (d’Orbigny, 1826) 5-ray Discoaster Sigmoilinita tenuis (Czjek, 1848) Helicosphaera carteri (Wallich, 1877) Kamptner, 1954 Trifarina bradyi Cushman, 1823 Helicosphaera stalis Theodoridis, 1984 Uvigerina peregrina Cushman, 1923 Pontosphaera spp. Valvulineria bradyiana (Fornasini, 1900) Reticulofenestra pseudoumbilicus (Gartner, 1967) Gartner, 1969 Reticulofenestra rotaria Theodoridis, 1984 Mollusks Reticulofenestra spp. (<7 µm) Anadara turoniensis (Dujardin, 1837) Schyphosphaera spp. Dosinia lupinus (Linnaeus, 1758) Sphenolithus abies Deflandre in Deflandre and Fert, 1954 Athleta rarispina (Lamarck, 1811) Umbilicosphaera jafari Muller, 1974 Clavatula calcarata francisci (Toula, 1901) Clavatula jouanneti (Desmoulins, 1842) Planktonic foraminifers Nassarius mutabilis (Linnaeus, 1758) Globigerina bulloides d’Orbigny, 1826 Hexaplex austriacus (Tourneuer, 1875) Globigerina sp. Globigerinita glutinata (Egger, 1893) Ostracods Globigerinella obesaBolli, 1957 Callistocythere quadrangula Ciampo, 1984 Callistocythere skeletrum Bonaduce, Ruggieri, Globigerinoides obliquus Bolli, 1957 Russo and Bismuth, 1992 Globigerinoides trilobusReuss, 1850 Cytherelloidea petrosa (Doruk, 1976) Globorotalia sp. Cytheretta sp. Globorotalia scitula Brady, 1882 sx Cytheridea zahorica Jiriček, 1978

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Table 1. (continued).

Ionicythere reticulata (Colalongo and Pasini, 1980) Aurila sp. B Keijella punctigibba (Capeder, 1902) Bairdoppilata subdeltoidea (Muenster, 1830) Leptocythere sp. Bosquetina carinella (Reuss, 1850) Loxoconcha lipadusensis Dall’Antonia and Bossio, 2001 Callistocythere montana Doruk, 1980 Loxoconcha ovulata (Costa, 1853) Callistocythere sp. Neomomoceratina laskarevi (Krstić and Pietrzeniuk, 1972) Capsacythere sicula (Aruta, 1966) Occlusacythereis occlusa Ruggieri and Russo, 1980 Costa tricostata (Reuss, 1850) Palmoconcha agilis (Ruggieri, 1967) Cyamocytheridea dertonensis Ruggieri, 1958 Phlyctenophora farkasi (Zalanyi, 1913) Cyamocytheridea meniscus Doruk, 1978 Semicytherura sp. Cyprideis seminulum (Reuss, 1850) Senesia cf. S. philippii (Reuss, 1850) Cytherella sp. Xestoleberis tumida (Reuss, 1850) Cytherelloidea glypta (Doruk, 1977) Cytheridea acuminata (Bosquet, 1852) SEMIRAMIS SECTION Keijella punctigibba (Capeder, 1902) Planktonic foraminifers Leptocythere sp.1 Globigerinella obesa Bolli, 1957 Loxoconcha ovulata (Costa, 1853) Globigerinoides bulloideus Crescenti, 1966 Microcytherura sp. Globigerinoides sacculifer (Brady, 1877) Nonurocythereis seminulum (Seguenza, 1880) Globigerinoides trilobus Reuss, 1850 Occlusacythereis occlusa Ruggieri and Russo, 1980* Globoturborotalita woodi Jenkins, 1960 Pontocythere elongata (Brady, 1868) Neogloboquadrina acostaensis (Blow, 1959) Ruggieria tetraptera (Seguenza, 1880) Neogloboquadrina humerosa Takayanagi and Saito, 1962 Sagmatocythere cristatissima (Ruggieri, 1976) Orbulina suturalis Brönnimann, 1951 Sagmatocythere multiflora (Norman, 1865) Orbulina universa d’Orbigny, 1839 Sagmatocythere variesculpta (Ruggieri, 1962) Sagmatocythere sp. Ostracods Tegmenia rugosa (Costa, 1853) Acanthocythereis hystrix (Reuss, 1850) Xestoleberis communis Müller, 1894 Aurila albicans (Ruggieri, 1958) Xestoleberis reymenti Ruggieri, 1967 Aurila convexa (Baird, 1850) Xestoleberis ventricosa Müller, 1894 particularly in the lower portion of the section, and portion, only unspecialized species that tolerate greater very low frequencies in the sandy portion. Richness, fluctuations could inhabit the very unstable environment. expressed by the number of taxa (S) and the Margalef 4.2. The Semiramis section index, is very low along the entire section (2–23 taxa), Only planktonic foraminifers and ostracods were indicating a restricted and stressed environment. The investigated in the Semiramis section (Kuzgun Formation) Margalef and Shannon–Wiener indexes display higher (Darbaş & Nazik 2010; Table 1). The planktonic foraminifer values in the marly layers and become very low in the assemblages are poorly diversified and are represented sandy layers that record very unstable conditions. The mainly by Orbulina spp., Neogloboquadrina humerosa, evenness indexes are low (the values for samples ADA-1 Globigerinoides bulloideus, and Globoturborotalita woodi. 4, 21, and 12 are biased by the very low frequencies) and Among the most common species, Keijella punctigibba, increase slightly upsection (samples ADA-1 16 and ADA-1 Keijella procera, Callistocythere montana, Cytheridea 14). In conclusion, the trend displayed by the community acuminata, Costa tricostata, Cyamocytheridea dertonensis, structure indexes records the occurrence of generally Cyamocytheridea meniscus, and Acanthocythereis hystrix unstable environments along the entire section. In the are present, accompanied by Ruggieria tetraptera, lower portion, the fluctuation of the physicochemical Carinocythereis carinata, Sagmatocythere spp., and parameters of the environment are low, and the ecosystem Xestoleberis spp. Moreover, sponge spicules were recovered could host a more diversified fauna, while in the upper from several samples.

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Table 2. Relative abundances and quality of preservation of the calcareous nannofossils from the Adana-1 section. A = Abundant; C = Common; F = Few; R = Rare; V = Very rare; and B = Barren; G = Good preservation; M = Moderate preservation; P = Poor preservation. , <7 µm spp. samples Preservation R. pseudoumbilicus Reticulofenestra R. rotaria H. stalis H. carteri S. abies C. pelagicus C. macintyrei C. leptoporus jafari U. Pontosphaera Scyphosphaera spp. Dictyococcites spp. variabilis D. surculusD. brouweriiD. D. pentaradiatus asymmetricus D. Discoaster 5-ray

ADA-1 14 ------ADA-1 17 ------ADA-1 15 M R F - VR R R F - - F R - F ------ADA-1 16 ------ADA-1 18 M R F - VR F F F - - R - - F ------ADA-1 13 P VR VR - - VR - VR - - VR VR - R ------ADA-1 19 M VR R - - R R F VR VR R R - F - - - - - VR ADA-1 12 ------ADA-1 20 M VR R VR - R R F VR - VR - - F VR - - - - VR ADA-1 21 M VR R - - VR VR R VR VR VR VR - F ------ADA-1 22 M VR R - VR R R F - - R VR - F - - - - - ADA-1 11 ------ADA-1 10 P VR VR - - VR - R - - - VR - F ------ADA-1 9 M VR VR - - VR VR VR - - VR VR - F ------ADA-1 8 M VR R - - R - R - - - - - R ------ADA-1 7 M F C - - F F C F F R VR - C VR VR - - - - ADA-1 6 G R F - - F F C R VR F R - A ------ADA-1 5 ------ADA-1 4 G C A C - C F F VR - - R F A C C C R VR - ADA-1 3 ------ADA-1 2 ------ADA-1 1 ------

4.3. The Adana section rare to abundant brackish ostracods are present from ADA The marly levels of the Adana section (Handere 30 upsection (Cyprideis agrigentina and the Paratethyan Formation) were sampled in detail. Planktonic and species Loxoconcha mülleri, Euxinocyhere (Maeotocythere) benthic foraminifers and ostracods were analyzed (Table praebaquana, and Loxoconcha sp.) (Figure 7). An 1). The 42 studied samples are characterized by random assortment of miscellaneous broken, badly preserved, changes of fossil frequencies that range from 0 to very and mainly juvenile specimens of marine infralittoral to abundant. On the whole, planktonic foraminifers are very circalittoral species, including Neomonoceratina laskarevi, rare and sporadic along the section and are considered Cytheridea acuminata, Paracytheridea triquetra, and to be reworked. Benthic foraminifers and ostracods are Ruggeria tetraptera, are present with different frequencies more common, except in samples ADA 10 and ADA in most of the samples, indicating reworking from older 24–29, which are barren. Ammonia beccarii and Cyprideis marine levels. agrigentina were collected in the lower portion, from ADA 4.4. Cluster analysis of the studied sections 1 to ADA 23, and are sometimes accompanied by rare Darbaş and Nazik (2010) did not perform quantitative Elphidium and Cribroelphidium. Ammonia beccarii and analyses on the Semiramis fauna, and no quantitative

847 FARANDA et al. / Turkish J Earth Sci

abc

def

gh

Figure 3. Microphotographs of calcareous nannofossils from the Adana-1 section. (a) Discoaster asymmetricus Gartner, 1969; (b) Discoaster brouwerii Tan, 1927, emend. Bramlette & Riedel, 1954; (c) Discoaster pentaradiatus (Tan) Bramlette & Riedel 1954: (d) Discoaster intercalaris Bukry, 1971; (e) Discoaster surculus Martini & Bramlette, 1963; (f) Amaurolithus delicatus Gartner & Bukry, 1975; (g) Reticulofenestra rotaria Theodoridis, 1984 (crossed nicols); (h) Reticulofenestra rotaria Theodoridis, 1984 (parallel nicols); (i) Amaurolithus primus (Bukry & Percival, 1971) Gartner & Bukry, 1975.

analysis is possible on the Adana samples due to the scattered presence of autochthonous species. To make comparisons between the 3 studied sections, a simple presence/absence matrix of the ostracod species was used to perform a cluster analysis. The Q-mode dendrogram illustrated in Figure 10 shows the complete separation of 2 clusters: Cluster A, which includes samples from the Kuzgun Formation, and Cluster B, which includes samples from the Handere Formation. At a similarity level of 0.4, Cluster A divides into Clusters A1 and A2, which group samples from the Adana-1 and Semiramis sections, respectively. The very low similarity between the Adana-1 and Semiramis ostracod assemblages is due to the 1 mm presence of only 4 common species: Keijella punctigibba, Loxoconcha ovulata, Neomonoceratina laskarevi, and Figure 4. Sieved residue of sample ADA-1 5 with abundant Occlusacythereis occlusa (equivalent to Carinocythereis benthic foraminifers. carinata in Darbaş & Nazik 2010). Based on the taxonomic-

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Normal zed frequency curves Normal zed frequency curves for selected ostracod spec es for selected benth c foram n fers 2 20 1 1 5 50 50 0 0 0 00 00 00 0 0 1 2 3 40 50 0 0 0 0 0 0 0 0

ADA1 14 ADA1 17 ADA1 15 ADA1 16 ADA1 18 ADA1 13 10 ADA1 19

ADA1 12 ADA1 20 Senesia cf. S. philippi Callistocythere quadrangula Ammonia beccarii Cytherelloidea petrosa Cribroelphidium decipiens ADA1 21 Neomonoceratina laskarevi Quinqueloculina spp. Phlyctenophora farkasi Xestoleberis tumida total benth c fora m n fe rs ADA1 22 total ostracods 5 ADA1 11 ADA1 10 ADA1 9 ADA1 8 ADA1 7 ADA1 6 ADA1 5 ADA1 4 ADA1 3 ADA1 2 0 ADA1 1 Figure 5. Normalized frequencies of selected benthic foraminifer and ostracod species of the Adana-1 section. uniformitarian approach for the paleoenvironmental provide an interesting chronostratigraphic and analysis with autoecological data derived from literature paleoenvironmental framework that is useful in depicting (Table 3) (Yassini 1980; Stambolidis 1985; Lachenal 1989; the paleoenvironmental evolution of the basin during the Zangger & Malz 1989) and rare paleoecological data on latest Miocene. fossil species (Table 4; Ruggieri 1967; Russo & Bossio, 5.1. Chronological framework 1976; Doruk 1978; Szczechura & Abd-El-Shafi 1988; The ages of the 3 study sections have been inferred by Miculan 1992; Babinot & Boukli-Hacene 1998; Babinot integrating the biostratigraphical data derived from 2002; Faranda et al. 2008), it is possible that Cluster B calcareous nannofossils, planktonic foraminifers, and includes species that are typical of shallow and mesohaline ostracods. According to Darbaş and Nazik (2010), the environments (Gliozzi & Grossi 2008; Grossi et al. 2008), cooccurrence of N. humerosa, whose First Occurrence while Cluster A is characterized by true marine species. (FO) is dated to the latest Tortonian (7.81 Ma; Iaccarino The differences between Clusters A1 and A2 are linked mainly to the depths and the vegetation on the bottom; et al. 2007), G. bulloideus, and G. woodi, whose Last samples of Cluster A1, from the Adana-1 section, record Occurrence (LO) is dated to the earliest Messinian (6.83 a coastal infralittoral environment (approximately 10 m in Ma; Iaccarino et al. 2007), constrains the age of the depth) with a vegetated bottom, while samples of Cluster Semiramis section to a short time interval from 7.81 to 6.83 A2, from the Semiramis section, indicate a more open and Ma, which corresponds to the end of the Tortonian and to slightly deeper (20–40 m) marine environment with scarce the beginning of the Messinian. The collected ostracods or even absent bottom vegetation. are mainly long-ranging species, but several of them (S. multiflora, T. rugosa, P. elongata, and C. sicula) have been 5. Discussion reported as starting from the Messinian (Aruta 1966, 1983; The paleontological analyses carried out on the Kuzgun Bonaduce et al. 1988; Darbaş & Nazik 2010), thus limiting Formation in the Adana Basin (Adana-1 and Semiramis the age of the Semiramis section to the earliest Messinian sections) and the Handere Formation (Adana section) (7.226–6.83 Ma) (Figure 11).

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a b c

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Figure 6. SEM photos of ostracods from the Adana-1 section (all specimens are illustrated in lateral external view, unless otherwise specified). (a) Cytherelloidea petrosa (Doruk), female LV, sample ADA-1 3; (b) Cytherelloidea petrosa (Doruk), male RV, sample ADA-1 3; (c) Cytheridea zahorica Jiriček, female RV, sample ADA-1 5; (d) Callistocythere quadrangula Ciampo, female LV, sample ADA-1 1; (e) Callistocythere quadrangula Ciampo, male LV, sample ADA-1 7; (f) Ionicythere reticulata (Colalongo & Pasini), male LV, sample ADA-1 2; (g) Cytheridea zahorica Jiriček, female LV, sample ADA-1 5; (h) Callistocythere skeletrum Bonaduce, Russo, Ruggieri & Bismuth, female RV, sample ADA-1 9; (i) Leptocythere sp., male LV, sample ADA-1 7; (j) Neomonoceratina laskarevi (Krstić & Pietrzeniuk), female C, dorsal view, sample ADA-1 2; (k) Cytheridea zahorica Jiriček, male LV, sample ADA-1 5; (l) Cytheretta sp., female LV, sample ADA-1 5; (m) Neomonoceratina laskarevi (Krstić & Pietrzeniuk), male C, dorsal view, sample ADA-1 2; (n) Keijella punctigibba (Capeder), female LV, sample ADA-1 5; (o) Loxoconcha lipadusensis Dall’Antonia & Bossio, female RV, sample ADA-1 5; (p) Neomonoceratina laskarevi (Krstić & Pietrzeniuk), female LV, sample ADA-1 2; (q) Neomonoceratina laskarevi (Krstić & Pietrzeniuk), male LV, sample ADA-1 9; (r) Keijella punctigibba (Capeder), male RV, sample ADA-1 5; (s) Loxoconcha lipadusensis Dall’Antonia & Bossio, female LV, sample ADA-1 5; (t) Loxoconcha lipadusensis Dall’Antonia & Bossio, male LV, sample ADA-1 5; (u) Phlyctenophora farkasi (Zalanyi), female LV, sample ADA-1 2. Legend: RV = right valve; LV = left valve; C = carapace. White bar corresponds to 0.1 mm.

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f d e

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Figure 7. SEM photos of ostracods from the Adana-1 and Adana sections (all specimens are illustrated in lateral external view, unless otherwise specified). (a) Loxoconcha ovulata (Costa), female RV, sample ADA-1 5; (b) Loxoconcha ovulata (Costa), female LV, sample ADA-1 5; (c) Occlusacythereis occlusa (Ruggieri & Russo), male RV, sample ADA-1 9; (d) Occlusacythereis occlusa (Ruggieri & Russo), female LV, sample ADA-1 7; (e) Phlyctenophora farkasi (Zalanyi), C, dorsal view, sample ADA-1 4; (f) Phlyctenophora farkasi (Zalanyi), male RV, sample ADA-1 2; (g) Senesia cf. S. philippi (Reuss), female RV, sample ADA-1 5; (h) Phlyctenophora farkasi (Zalanyi), male LV, inner view, sample ADA-1 7; (i) Senesia cf. S. philippi (Reuss), female LV, sample ADA- 1 5; (j) Euxinocythere (Maeotocythere) praebaquana (Livental in Agalarova et al., 1940), juvenile LV, sample ADA 30; (k) Xestoleberis tumida (Reuss), female LV, sample ADA-1 1; (l) Senesia cf. S. philippi (Reuss), female C, dorsal view, sample ADA-1 9; (m) Xestoleberis tumida (Reuss), male RV, sample ADA-1 9; (n) Loxoconcha sp., male RV, sample ADA 23; (o) Xestoleberis tumida (Reuss), female LV, inner view, sample ADA-1 9; (p) Loxoconcha mülleri (Méhes), female LV, sample ADA 42; (q) Senesia cf. S. philippi (Reuss), male RV, sample ADA-1 5; (r) Cyprideis agrigentina, female RV, sample ADA 3. Legend: RV = right valve; LV = left valve; C = carapace. White bar corresponds to 0.1 mm.

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ab cde

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n o 1 cm Figure 8. Mollusk assemblage collected in sample ADA-1 5 (Adana-1 section – Kuzgun Fm). (a, b) Anadara turoniensis (Dujardin); (c) Ostrea sp.; (d, e) Clavatula jouanneti (Desmoulins); (f, g) Athleta rarispina (Lamarck), adult specimen; (h, i) Athleta rarispina (Lamarck), juvenile specimen; (j, k) Clavatula calcarata francisci (Toula); (l, m) Nassarius mutabilis (Linnaeus); (n, o) Hexaplex austriacus (Tourneuer).

In the Adana-1 section, both nannofloras and between 6.65 and 6.43 Ma. This is based on the common planktonic foraminifers are scarcely diversified. occurrence of N. atlantica prior to the sinistral to dextral Regardless, the common presence of Reticulofenestra coiling change of N. acostaensis in the Tripoli Formation rotaria and the occurrence of Amaurolithus primus and A. at the Falconara-Gibliscemi section (Blanc-Valleron et al. delicatus in the lower portion of the succession (Sample 2002). The presence of Loxoconcha lipadusensis, previously ADA 1–4) provide good age constraints. In particular, the recovered only from Mediterranean Messinian sediments Reticulofenestra rotaria First Common Occurrence (FCO) (Russo & Bossio 1976; Aruta 1983; Miculan 1992; is a useful nannofossil event that slightly predates the Dall’Antonia & Bossio 2001; Guernet 2005), is consistent Tortonian/Messinian boundary (Negri et al. 1999), such as with the early Messinian age of the Adana-1 section. the FOs of both A. primus and A. delicatus on a global scale The Adana section (Handere Formation) is (Raffiet al. 1995; Backman & Raffi 1997). More accurately, characterized by abundant reworked fossil remains. the A. delicatus FCO, at approximately 7.221 Ma (Hilgen Among the autochthonous forms, only ostracods are et al. 2000), seems to be the nannofossil bioevent that useful for dating the succession. The presence of C. best defines the Tortonian/Messinian boundary, as was agrigentina, L. mülleri, and E. (M.) praebaquana points to a also shown in several other stratigraphic sections in the postevaporitic Messinian age (Lago-Mare event, 5.60–5.33 Mediterranean area (Cosentino et al. 1997; Negri et al. Ma; CIESM 2008) (Gliozzi et al. 2007), spanning from 1999; Negri & Villa 2000; Sierro et al. 2001; Frydas 2004; the Loxoconcha mülleri zone in the lower portion to the Morigi et al. 2007; Mansouri et al. 2008). In summary, the beginning of the Loxocorniculina djafarovi zone (Grossi et age of the basal portion of the section is constrained to al. 2011). between approximately 7.221 Ma (A. delicatus FCO) and In summary, the sedimentary successions investigated 6.77 Ma (R. rotaria LO; Negri & Villa 2000). in this paper correspond to the early Messinian Upsection, the presence of Neogloboquadrina atlantica (preevaporitic) portion of the Kuzgun Formation and in samples ADA 1–5 and ADA 1–8 and the contemporary to the postevaporitic Messinian portion of the Handere presence of sinistrally coiled N. acostaensis indicates an age Formation. The Kuzgun and the Handere Formations in

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Normal sed frequenc es No. of taxa (S) Margalef ndex Evenness ndex (e H/S) Shannon–W ener ndex 10,000 15,000 20,000 25,000 5,000 0. 1. 2. 0. 1. 2. 0. 0 0. 0. 10 1 20 2 . 0 0 5 5 5 0 1 2 3 5 5 5 0 1 2 3 5 5 5 2 4 6 8 1

ADA1 14 ADA1 17 ADA1 15 ADA1 16 ADA1 18 ADA1 13 10 ADA1 19

ADA1 12 ADA1 20

ADA1 21

ADA1 22 5 ADA1 11 ADA1 10 ADA1 9 ADA1 8 ADA1 7 ADA1 6 ADA1 5 ADA1 4 ADA1 3 ADA1 2 0 ADA1 1 Figure 9. Community structure indexes for the benthic foraminifers and ostracods of the Adana 1 section. the study area appear to be separated by a hiatus of at least amounts of evaporites and the drawdown of sea level in 840 k.y. (MES), during which the entire Mediterranean the Mediterranean (CIESM 2008). Basin was affected by the progressive onset and acme of 5.2. Paleoenvironmental changes in the Adana Basin the Messinian Salinity Crisis, with the deposition of large during the Messinian 8 0 3 The cluster analyses performed on samples from the 14 15 8 19 22 11 2 10 6 7 1 1 9 5 3 _1 _2 _ _ _ 0 _4 3 2 1 7 4 1_ 1 1 1_ 1_ 1_ 1 1 1_ 1_ 1_ 1 1_ 1_ 1_ 1_ 8 6 1_ 5 2 4 3 42 20 22 18 14 1 1 11 8 2 1 4 40 3 6 35 3 33 31 36 30

- - -1 -1 -

A A- A- A- A- A A- A- A- A A- A- A- A- A- A- A A A A A A A A A A A A A A A A A A A A A M M M M M M M D DA DA D E D D D D D D D Kuzgun and Handere Formations (Figure 10) show a sharp AD AD AD AD AD AD AD AD A AD A AD AD AD AD AD A AD A S SE SE SE AD AD SE SE SE A AD AD AD AD A AD AD AD A A AD A A AD AD AD A 1 paleoenvironmental division. The Kuzgun Formation was deposited in true marine conditions, while the 0. 9 Handere Formation probably records short-lived brackish 0. 8 environments. According to the data from Darbaş and Nazik (2010), the slightly older Semiramis section documents 0. 7 a littoral open marine environment characterized by abundant planktonic foraminifers, which are dominated 0. 6 by warm water species of Globigerinoides and Orbulina and by infralittoral ostracods with infracircalittoral 0. 5

S m lar t y species such as Occlusacythereis occlusa, Bairdoppilata 0. 4 subdeltoidea, Costa tricostata, Bosquetina carinella, and Ruggieria tetraptera. The presence of spicules of siliceous 0. 3 sponges confirms an open external neritic environment. In contrast, the slightly younger Adana-1 section, located 0. 2 A1 A2 approximately 500 m northwest of Semiramis, records a 0. 1 very shallow coastal marine environment. This is indicated by the scarcity of nannofloras and planktonic foraminifers 0 A B and the low diversity of benthic foraminifers and Figure 10. Dendrogram resulting from cluster analysis in ostracods. The presence of Ammonia beccarii (dominant Q-mode using the UPGMA method and the Morisita–Horn among benthic foraminifers), Neomonoceratina laskarevi, distance applied to the ostracod assemblages of the Semiramis, and Phlyctenophora farkasi (dominant among ostracods), Adana-1, and Adana successions. which are typical of shallow water environments such

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Table 3. Autoecology of selected species of marine living ostracods.

Species Depths Bottom References

Acanthocythereis hystrix Around 30 m Stambolidis 1985 Circalittoral, 75 m Muddy sands Yassini 1980 >50 m Zangger & Malz 1989 Aurila (different species) Mediolittoral-infralittoral (0–40 m) Posidonia, calcareous algae Lachenal 1989 5–20 m Zangger & Malz 1989 Ubiquitarian (mediolittoral-upper On algae, Posidonia detritus, Aurila convexa Lachenal 1989 circalittoral, 0–50/60 m) sands, muds Infralittoral (0–25 m) Yassini 1980 Around 30 m Stambolidis 1985 Bosquetina carinella Around 30 m Stambolidis 1985 Between 100–200 m Silty sands, mud Yassini 1980 (maximum around 115 m) Callistocythere (different species) <20 m Stambolidis 1985 Mainly from 25 to 50 m Yassini 1980 Mediolittoral to infralittoral (4–24 m) Posidonia and algae Lachenal 1989 Infralittoral-circalittoral (30–70 m), Carinocythereis carinata Posidonia silts, Yassini 1980 maximum abundance 30 m Infralittoral-circalittoral (0–104 m), (similar to Occlusacythereis) Posidonia detritus, Posidonia Lachenal 1989 common to frequent at 2–30 m Maximum abundance around 10 m, Stambolidis 1985 but down until 30 m Costa edwardsi Circalittoral (50–100 m) Mud, silty sands Yassini 1980 Upper circalittoral (55–112 m) Silts Lachenal 1989 Cytherelloidea sordida Infralittoral and circalittoral, 0–112 m Cymodocea, algae and silts Lachenal 1989 Maximum abundance between 50 and 1 Calcareous algae, mud Yassini 1980 00 m, present at 112 m Cytheridea neapolitana 10–30 m Stambolidis 1985 Mediolittoral-upper circalittoral (0–88 m) Muds, Posidonia detritus Lachenal 1989 0–50 m Yassini 1980 Loxoconcha ovulata Low-energy, near-shore Zangger & Malz 1989 0–33 m, 15–24 °C, 34–38‰ Stambolidis 1985 Infralittoral (20–55 m) Algae, Posidonia, and silts Lachenal 1989 Infralittoral (20–28 m), infralittoral Calcareous algae, Posidonia silts Yassini 1980 (30–40 m) Phlyctenophora rara Infralittoral Posidonia, calcareous algae Lachenal 1989 Pontocythere (different species) Mediolittoral, upper infralittoral (0–2 m) Sands, Posidonia detritus Lachenal 1989 1–2 m Zangger & Malz 1989 Sagmatocythere (different Infralittoral-upper circalittoral (20–70 m) Muds, Posidonia detritus Lachenal 1989 species) Semicytherura (different species) Infralittoral Vegetated bottoms Lachenal 1989 Xestoleberis (different species) Infralittoral (10–15 m) Stambolidis 1985 Xestoleberis communis Low-energy, near-shore (dominant) Zangger & Malz 1989 Between 0-25 m Yassini 1980 Sands, silts, Posidonia, Zoostera Mediolittoral-infralittoral Lachenal 1989 Leaves and calcareous algae Xestoleberis ventricosa Upper circalittoral (55–112 m) Calcareous algae Lachenal 1989

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Table 4. Inferred autoecology for selected fossil species of marine ostracods.

Species Depths Bottom References

Cyamocytheridea (several species) Probably shallow marine Doruk 1978 Inner infralittoral Faranda et al. 2008 Keijella (several species) Probably shallow marine Doruk 1978 Kejella punctigibba Infralittoral (20–40 m) Ruggieri 1967 Infralittoral Miculan 1992 Infralittoral Russo & Bossio 1976 Neomonoceratina laskarevi From brackish to euhaline Krstic & Pietrzeniuk 1972 Infralittoral Miculan 1992 Lagoon-mediolittoral Babinot 2002 Very shallow marine Vegetated bottoms Faranda et al. 2008 Inner neritic, warm waters Szczechura & Abd-El Shafi 1988 Nonurocythereis Infralittoral Miculan 1992 Phlyctenophora farkasi Very shallow marine Vegetated bottoms Faranda et al. 2008 Tegmenia rugosa Neritic, infralittoral-circalittoral Vegetated bottoms, sandy marls Babinot & Boukli-Hacene 1998 as marshes, lagoons, and estuaries (Krstić & Pietrzeniuk foraminifers and ostracod assemblages corresponds to 1972; Murray 2006 and references therein; Faranda et al. a very unstable shallow brackish environment, which is 2008), together with Cribroelphidium decipiens, indicates characterized by high mesohaline salinity in the lower an enclosed marine environment characterized by portion (“Cyprideis-Ammonia assemblage”; Grossi et sporadic local freshwater inputs that decreased the salinity. al. 2008) and mesohaline salinity in the upper portion There is no clear evidence for oxygen depletion, although (“Cyprideis-Loxoconcha assemblage”; Grossi et al. 2008). A. beccarii can tolerate an abundant input of organic The same unstable brackish environment has already been matter (Nigam & Thiede 1983; Martins et al. 2006). The documented (Cipollari et al. 2012) in the western part of unstable environment recorded in the Adana-1 section the Adana Basin in the Avadan composite section (AVA can explain the poorly diversified assemblages recovered subsection), where Cyprideis agrigentina, Tyrrhenocythere along the succession. Regardless of this issue, well-defined, sp., and Leptocytheridae indet. were recovered. if limited, open-sea influx is documented in the lower Unpublished ostracod analyses of other outcrops of the portion of the section by the presence of abundant and Handere Formation in the Adana Basin at Kirilkaş, along well preserved nannofloras, more diversified ostracod and the Menekşe Road, and at Gökkuyu gave similar results, foraminifer assemblages (among which Quinqueloculina recording the presence of Cyprideis agrigentina and gr. is rather well represented), and euhaline gastropods. Caspiocypris juv. In the latter localities, as in the Adana In one sample from the lower part of the section, the section, reworked marine ostracods were rarely abundant, calcareous nannofossil assemblages are marked by the common presence of discoasters that are indicative of an indicating the periodic arrival of large amounts of environmental niche of open-ocean warm waters. Their siliciclastic material from the uplifting northwest margin presence clearly indicates sporadic open marine influx. to the rapidly subsiding basin. As suggested by several In contrast, the calcareous nannofossil assemblages found seismic lines and wells (Cosentino et al. 2010c; Cipollari in most of the samples from the Adana-1 section indicate et al. 2012), during the Messinian late Lago-Mare event strong reworking, and the regular presence of U. jafari, (5.45–5.33 Ma), the Adana Basin was affected by high which is considered an opportunistic species, could be subsidence rates that caused the deposition of a thick interpreted as being due to restricted, near-shore marine succession of fluvial conglomerates (>1 km; Cosentino et environments (Wade & Bown 2006). al. 2010c; Cipollari et al. 2012) intercalated with brackish- The Handere Formation was deposited unconformably to fresh-water fine-grained deposits (Handere Formation). over the Kuzgun Formation, just above the MES, after a These high sedimentation rates may also explain the very hiatus of at least 840 k.y. The subaqueous paleoenvironment rare and scattered fauna found within the fine-grained documented in the Adana section by the benthic deposits of the Handere Formation.

855 FARANDA et al. / Turkish J Earth Sci

SELECTED FOSSILS RANGE CHART

Chrono- ATNTS 2004 strat graphy adusenss p age . bullodeus . wood . elongata . rugosa zones A. delcatus Magneto Med terranean calcareous nannofoss ls b ostrat graphy N. humerosa G G C. scula T S. multora Age Polar ty Per od Epoch St Med terranean plankton c foram n fer b ostrat graphy Med terranean ostracod b ostrat graphy E. (M.) praebaquana C. agrgentna R. zancleana Sphaerodnello pss acme P R. rotara N. atlantca nux N. acostaenss s n L. l C. agrgentna L. muller MPl 4 a C2A MNN 16 4 MNN 14-15 MPl 3 Zanclean MNN 13 Lower MPl 2 c

C3 Pl ocene 5 b MPl 1 5.332 MNN 12 a L. djafarov L. muller NDZ MSC hyperhal ne Avadan secton

6 Adana secton C3A c

NEOGENE Mess n an c b MM 13 11

7 Upper

M ocene a 7.246 b

C3B Adana 1 secton MNN

b Semrams secton Torton an a

C4 MM 1 2 8 a Figure 11. Integrated Mediterranean biostratigraphic scheme of the Late Miocene-Early Pliocene, with the distribution of selected species of calcareous nannofossils, ostracods, and planktic foraminifera recovered in the sections studied in the Adana Basin. The gray bands correspond to the proposed age of the different sections. ATNTS 2004 and calcareous nannofossil biostratigraphy from Lourens et al. (2004), Di Stefano and Sturiale (2010), and Negri and Villa (2000); planktonic foraminifer biostratigraphy from Iaccarino et al. (2007); ostracod biostratigraphy from Grossi et al. (2011). NDZ: Nondistinctive zone; MSC: Messinian Salinity Crisis.

The extreme instability of the Adana Basin during the 5.3. The eastern Paleo-Mediterranean environments sedimentation of the Handere Formation, mainly due to before and during the Messinian Salinity Crisis tectonic activity, is also indicated by the occurrence of The paleoenvironmental changes that occurred during slump structures throughout the succession (Cipollari et the Messinian in the Adana Basin can be compared to the al. 2012; Lucifora et al. 2012). paleoceanographic changes that affected the entire Paleo- According to the literature, the Handere Formation was Mediterranean region before and during the greatest also deposited during the Pliocene. In contrast, Darbaş and catastrophic event to affect the Paleo-Mediterranean Nazik (2010) and Cipollari et al. (2012) demonstrated that Basin: the Messinian Salinity Crisis (Hsu et al. 1973; it was only deposited in the postevaporitic Messinian. The CIESM 2008; Ryan 2009 and references therein). earliest Pliocene sediments, which conformably overlay Deeper marine successions that are coeval with the the Handere Formation, crop out in the upper subsection marine sections studied in this paper are common in of the Avadan composite section (Cipollari et al. 2012) the western and eastern Paleo-Mediterranean region and are characterized by gray clays that are rich in marine (e.g., Fanantello in the northern Apennines, Manzi et al. fauna. These marine deposits, which were deposited 2007; Serra Pirciata, Torrente Vaccarizzo, Marianopoli, in the earliest Zanclean (MPl 1 zone p.p. and MNN 12a and Falconara-Gibliscemi in Sicily, Bellanca et al. 2001; subzone) from 5.30–5.234 Ma, have been described as a Blanc-Valleron et al. 2002; Pissouri and Tochni in Cyprus, new formation called the Avadan Formation by Cipollari Krijgsman et al. 2002; Kouwenhoven et al. 2006; Orszag- et al. (2012). Nannofloras, foraminifers, and ostracods Sperber et al. 2009). The sections are all characterized by recovered from these early Zanclean deposits record an strong cyclicity marked by the deposition of alternating epibathyal marine environment that is completely different whitish marls and black sapropelitic clays. Neritic marine from the underlying shallow brackish lagoon. successions with well-constrained ages that are related to

856 FARANDA et al. / Turkish J Earth Sci the preevaporitic Messinian in the Paleo-Mediterranean deeper facies recorded at Sarıalan and by the presence, in area are very rare. An example is the Chabet Bou Seter the lower portion of the Sarıalan section, of Heterostegina section (Algeria; Babinot & Boukli-Hacene 1998), where carbonate platform and coralgal patch reefs (Schildgen et the lower part before the FO of Turborotalita multiloba al. 2012b), which supported reefal ostracod assemblages. (6.42 Ma; Iaccarino et al. 2007) is partially coeval with the In conclusion, the differences in ostracod assemblages Semiramis and Adana-1 sections (Adana Basin) and is in the Messinian preevaporitic marine successions from similar in age to the uppermost part of the Sarıalan section the eastern Mediterranean (Semiramis, Adana-1, and (SW margin of the Central Anatolian Plateau, Deynoux et Sarıalan sections) are likely due to differences in basin al. 2005; Çiner et al. 2009; Schildgen et al. 2012b), whose depth. The absence of clear disoxic bottoms at Semiramis basal age corresponds to the disappearance of the benthic and Adana-1 could be linked to their shallower depths foraminifer Siphonina reticulata (7.17 Ma, Kouwenhoven in comparison with Sarıalan (Schildgen et al. 2012b) and et al. 1999, 2003, 2006) or slightly younger (Schildgen et the Pissouri and Tochni sections (Krijgsman et al. 2002; al. 2012b). Kouwenhoven et al. 2006; Orszag-Sperber et al. 2009). The lower portion of the Chabet Bou Seter section, Such shallow environments are subject to high-energy below the FO of T. multiloba, is composed of a cyclical wind and wave action that mixes the water column and sequence of sandy marls and/or clayey limestones prevents stratification and subsequent oxygen depletion at intercalated with laminated marls with fish remains. The the bottom. Similar inner infralittoral conditions without succession is generally characterized by the presence of “Tripoli-like” characters have also been recognized at abundant sponge spicules, abundant but low-diversity Legnagnone, a slightly younger central Mediterranean ostracod assemblages in the sandy marls (3–17 species), sedimentary succession with an age of 6.15–5.96 Ma and very poor assemblages (2–7) in the laminated marls. (unpublished data). Accompanying benthic foraminifers include Textularia, The postevaporitic Lago-Mare event of the Handere Lenticulina, Bulimina, Bolivina, and Uvigerina, which Formation has been recognized in the entire Paleo- record disoxic bottom conditions. On the whole, the Mediterranean Basin, from the westernmost areas ostracod and benthic foraminifer assemblages indicate (Malaga Basin, Nijar Basin, Sorbas Basin, Spain; Martin- an external neritic environment that gradually becomes Suarez et al. 2000; Bassetti et al. 2006; Guerra-Merchán shallower. If compared to the Semiramis section, this et al. 2010; Chelif Basin, Algeria; Rouchy et al. 2007) to slightly deeper environment agrees with the scarce the central areas (several localities in Italy, among others: presence of shared species (Acanthocythereis hystrix, Maccarone, Maiella, Mondragone, Cava Serredi, and Sagmatocythere variesculpta, Callistocythere montana, and Moncucco; Cipollari et al. 1999a, 1999b; Grossi et al. Xestoleberis communis). 2008 and references therein; Roveri et al. 2008; Violanti Based on planktonic and benthic foraminifers, et al. 2009, 2011; Riforgiato et al. 2011; Cosentino et al. Schildgen et al. (2012b) report a neritic environment for 2012a) and to the eastern Paleo-Mediterranean (Aegina the upper portion of the Sarıalan succession (Sarıalan A Island, Crete, Greece; Krstić & Stancheva 1990; Cosentino subsection) that gradually becomes shallower (from >30 et al. 2007; Cyprus; Galoukas & Danielopol 2004). In to >10 m in depth). The bottom, which was initially well addition, postevaporitic Lago-Mare deposits were drilled oxygenated, becomes disoxic upsection with the presence in several Mediterranean Ocean Drilling Program and of Uvigerina and Bolivina. In the uppermost part, sponge Deep Sea Drilling Project sites (Blanc-Valleron et al. 1998; spicules become abundant, and the deposits show a Spezzaferri et al. 1998; Iaccarino et al. 1999; Iaccarino & “Tripoli-like” character that is rich in organic matter and Bossio 1999; Orszag-Sperber 2006 and references therein; plant remains. Pierre et al. 2006) (Figure 1a). All of these locations Unpublished data on the ostracods of the Sarıalan had the same paleoenvironmental characteristics as the A subsection agree with the depths estimated based on Adana Basin (i.e. unstable brackish environments and the foraminifers (the presence of circalittoral species in the presence of Cyprideis agrigentina and Paratethyan brackish lower portion, i.e. Henrihowella asperrima, Bairdoppilata ostracods). sp., and Cytherella cf. C. russoi) associated with The wide distribution of the Lago-Mare facies infralittoral/circalittoral species such as Tenedocythere and the spreading of the Paratethyan ostracods were cruciata, Grinioneis haidingeri, Pokorniella italica, triggered by the complete closure of the Gibraltar gateway Pokorniella devians, Aurila punctata, and Loxocorniculum (Mediterranean-Atlantic connection) following the tumidum, which become dominant upsection. Ostracods drawdown of the Mediterranean base level at the end of are very scarce in the uppermost 3 samples, which agrees the first stage of the Messinian Salinity Crisis (CIESM well with possible disoxic bottom conditions. The lack 2008 and references therein). This event was coupled with of shared species between the Sarıalan A subsection and a global humid climate phase (Griffin 2002) that likely the Semiramis succession can be explained by the slightly caused the overflow of the Paratethyan waters into the

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Paleo-Mediterranean domain (McColluch & De Deckker information that are useful in reconstructing the 1989; Benson 2000; Vasiliev et al. 2010). environmental changes that occurred at that time in the The recognition of the Messinian Lago-Mare event in easternmost Mediterranean. the Adana Basin represents the easternmost record of this The occurrence of N. humerosa, G. bulloides, G. facies in the Paleo-Mediterranean. A peculiarity of the woodi, N. acostaensis, N. atlantica (planktonic forams), S. Adana Paratethyan assemblages is their low diversity. This multiflora, T. rugosa, P. elongata, C. scitula, L. lipadusensis cannot be ascribed to the general paleoclimatic conditions (ostracods), R. rotaria, A. primus, and A. delicatus of the easternmost Paleo-Mediterranean because in Cyprus (calcareous nannofossils) constrains the uppermost part (Galoukas & Danielopol 2004) and in Crete (Cosentino of the Kuzgun Formation sampled in the Semiramis and et al. 2007), a rather diversified Paratethyan fauna has Adana-1 sections to the early Messinian. The presence been recovered with several Loxonconchidae (including of Ammonia beccarii, Neomonoceratina laskarevi, and Loxocorniculina djafarovi) and Leptocytheridae. Thus, Phlyctenophora farkasi, which are typical of shallow-water the low diversity of the ostracod assemblages in the environments such as marshes, lagoons, and estuaries Adana Basin must be linked to the high siliciclastic input (Murray 2006 and references therein; Krstić & Pietrzeniuk connected with the high subsidence rate that affected the 1972; Faranda et al. 2008), with Cribroelphidium decipiens basin during the late Messinian (Cosentino et al. 2010c), indicates an enclosed marine environment characterized though diversified Paratethyan ostracod fauna, including by local sporadic freshwater inputs. Loxocorniculina djafarovi, have been found in some The presence of Paratethyan ostracods pertaining to central Mediterranean locations with high sedimentation the Loxoconcha mülleri Zone and to the Loxocorniculina rates (Cosentino et al. 2006). The high subsidence rate djafarovi Zone (Grossi et al. 2011) in the Handere of the Adana Basin is indicated by the thick deposits of Formation also points to the occurrence of the Messinian the Handere Formation, the upper portion of which is Lago-Mare event in the Adana Basin. This event, which characterized by more than 1 km of fluvial conglomerates that are interbedded with marls. The majority of the occurred throughout the Mediterranean between 5.60 to pebbles in the Handere Formation are from the Central 5.33 Ma (CIESM 2008), was characterized by unstable Tauride units, which crop out on the northwestern margin brackish environments. of the Adana Basin. The upper portion of the Handere Formation was deposited in a very short time interval Acknowledgments from 5.45 to 5.33 Ma (Cosentino et al. 2010a, 2010b; This research was funded by the Italian Ministry of Cipollari et al. 2012), indicating a large supply of detrital Instruction, University, and Research (MIUR) within grains from the southern margin of the Central Anatolian the project “High-resolution stratigraphic correlations of plateau, which has been uplifted since the latest Miocene the main palaeoceanographic and palaeoclimatic events (Cosentino et al. 2012b; Schildgen et al. 2012a, 2012b). during the Messinian salinity crisis in the Mediterranean area” (PRIN 2008, local coordinator D. Cosentino). This 6. Conclusions work is also part of the Vertical Anatolian Movements The paleontological analyses performed on the Late Project (VAMP), funded by the TOPO-EUROPE Neogene deposits of the Adana Basin (uppermost Kuzgun initiative of the European Science Foundation, including Formation and Handere Formation) provide both strong contribution by the IGAG-CNR (com. TA.P05.009, mod. chronostratigraphical constraints and paleoenvironmental TA.P05.009.003).

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