Reconciling the stratigraphy and depositional history of the Lycian orogen-top basins, SW Anatolia

Terrestrial fossil records from the SW Anatolian basins are crucial both for regional correlations and palaeoenvironmental reconstructions. By reassessing biostratigraphic constraints and incorporating new fossil data, we calibrated and reconstructed the late Neogene and Quaternary palaeoenvironments within a regional palaeogeographical framework. The culmination of the Taurides in SW Anatolia was followed by a regional crustal extension from the late Tortonian onwards that created a broad array of NE-trending orogen-top basins with synchronic associations of alluvial fan, fluvial and lacustrine deposits. The terrestrial basins are superimposed on the upper Burdigalian marine units with a c. 7 myr of hiatus that corresponds to a shift from regional shortening to extension. The initial infill of these basins is documented by a transition from marginal alluvial fans and axial fluvial systems into central shallow-perennial lakes coinciding with a climatic shift from warm/humid to arid conditions. The basal alluvial fan deposits abound in fossil macro-mammals of an early Turolian (MN11–12; late Tortonian) age. The Pliocene epoch in the region was punctuated by subhumid/humid conditions resulting in a rise of local base levels and expansion of lakes as evidenced by marsh-swamp deposits containing diverse fossil mammal assemblages indicating late Ruscinian (late MN15; late Zanclean) age. A second pulse of extension, accompanied by regional climatic changes, prompted subsequent deepening of the lakes as manifested by thick and laterally extensive carbonate successions. These lakes, which prevailed c. 1 myr, later shrank due to renewed progradation of alluvial fans and eventually filled up and dried out, reflected by marsh-swamp deposits at the top of a complete lacustrine succession that contains diverse micro-mammal assemblages indicating a latest Villanyian (MN17; Gelasian) age. A third pulse of tectonic reorganisation and associated extension dissected the basins into their present-day configuration from the early Pleistocene onwards under warm/humid climatic conditions. The new age data provide means to correlate deposits across various basins in the region that help to place the basin development into a regional tectonic framework, which can be attributed to the consequence of the well-articulated regional phenomena of slab-tear/detachment-induced uplift followed by crustal extension and basin formation (late Tortonian), the outward extension of the Aegean arc (early Pliocene) and eventually accompanied by westward extrusion of the Anatolian Plate (early Pleistocene).

The terrestrial fossil record from these basins, developed on the Taurides in SW Anatolia, is important for the understanding of regional inter-basinal correlation as well as for deconvolving basin spatio-temporal evolution of the basins.The sedimentary architecture combined with biostratigraphic evidence constrains the timing and evolutionary history of the region.In addition, the sedimentary record in these orogen-top basins provides vital information for understanding palaeoenvironmental changes during the last stages of orogeny, which can then be corroborated by faunal changes controlled by these environmental shifts.Documenting these environmental shifts is in turn important in recognising the role of Anatolia in faunal migration routes.Some of these basins, such as the Çameli and Eşen, have been comprehensively studied, however, for others, the work is still in progress.In order to understand the tectonostratigraphic development of the basins in SW Anatolia, detailed biostratigraphic information for dating the tectonic events in the region is essential.This need stimulates progress in further explorations and discovery of new fossil mammal sites to enhance the resolution of terrestrial Neogene stratigraphy in the region.The faunas from these localities are crucial for these terrestrial basins, as they provide invaluable data for understanding the stratigraphic, palaeoenvironmental and palaeogeographic evolution of the region (Alçiçek 2001).Furthermore, because it is located at the junction of Eurasia and Africa, Anatolia is in a unique position for the study of Neogene and Quaternary ecosystems, and for understanding key developments in the biogeography of western Eurasia.This includes the environmental shifts, interregional faunal exchanges including the dispersal of Homo through this region (Alçiçek 2010, Vialet et al. 2012, Alçiçek et al. 2017, Krijgsman et al. 2018).
The primary aim of this study is to fine-tune the stratigraphic framework, and to increase the resolution of timing of geodynamic events related to the deformation history of the eastern Mediterranean.This comparative study is a contribution towards a greater understanding of the development of an array of extensional basins on top of the Lycian nappes, and provides new insights into the tectonic history of the Taurides, with analogies drawn with other branches of the Alpine orogen.

Regional geological setting
The palaeo-Mediterranean region underwent diverse geodynamical processes linked to the syn-tectonic development of both perisutural (foreland) and episutural (thrust-top, back-arc) sedimentary basins, characterized by different subsidence rates and sedimentary processes (Cipollari et al. 1999).In SW Anatolia, the compression-and extension-related basins were developed as a consequence of the Tauride Orogeny associated with the overall convergence of the African-Eurasian plates during the Neogene to Quaternary (Sözbilir 2005, Alçiçek et al. 2005, 2006, Alçiçek 2007, Alçiçek & Ten Veen 2008, Ten Veen et al. 2009).
The western Taurides in SW Anatolia constitute the eastern extension of the Alpine orogeny and correlate with the Hellenides of Greece (Poisson 1984, Özgül & Arpat 1973, Bernoulli et al. 1974).They are subdivided into three main structural units: the Beydağları autochthon, Lycian nappes, and Antalya complex (Özgül 1976, 1984;Fig.1).On a regional scale, these structural units are attributed to different stages of the Neotethyan closure that involved the genesis and emplacement of large-scale carbonate platform units and ophiolitic nappes since the late Mesozoic times (de Graciansky 1972, Collins & Robertson 1997, 1998).
The Beydağları autochthon forms a broad north-south trending anticlinorium underlying the Lycian and Antalya nappes emplaced at its western and eastern flanks respectively, and contains Liassic to middle Miocene platform carbonates (Waldron 1981, Hayward & Robertson 1982, Collins & Robertson 1999).The Lycian nappes correspond to a segment of the orogenic-belt that originated in the northern Neotethys and comprise composite allochthonous thrust sheets transported from the Late Cretaceous to the middle Miocene and emplaced onto the Beydağları platform (Hayward & Robertson 1982, Robertson et al. 2003, Collins & Robertson 2003).The Antalya complex probably originated from the southern Neotethyan domain.It was emplaced on the eastern flank of the Beydağları platform by the Late Cretaceous-Neogene, and consists of allochthonous Mesozoic and older sedimentary, igneous and metamorphic rocks (Waldron 1981, Woodcock & Robertson 1982, Poisson et al. 2003, Koç et al. 2016).
Farther to the southeast, the nappe front is eventually overlain by Serravalian shallow marine clastics (Hayward 1984).The supra-allochthonous units are considered to be deposits of a piggy-back basin, transported jointly with the nappe progradation during the middle Miocene (Alçiçek & Ten Veen 2008, Ten Veen et al. 2009).The final movement of the nappes was followed by regional uplift corresponding to a non-depositional period that lasted c. 7 Myr (Alçiçek et al. 2018).This phase took place under NE-SW directed extension and resulted in an array of graben-type depressions stretched parallel to the transport direction of the nappe front and include Çal, Baklan, Acıgöl, Burdur, Çameli, Eşen and Beyağaç basins (Ten Veen 2004, Alçiçek et al. 2005, 2006, Alçiçek 2007, Ten Veen et al. 2009, Alçiçek et al. 2013).The tectono-sedimentary development of these basins is relatively uniform in the sense that all basins comprise a tripartite basin-fill that consists of an association of alluvial-fan, fluvial and lacustrine facies.Faunal evidence from the stratigraphic record of each basin indicates coeval terrestrial deposition through the early Turolian to the Gelasian.

Comparative basin stratigraphy
The first lithostratigraphical description and subdivision of SW Anatolian terrestrial successions was made by Becker-Platen (1970), who proposed a lithostratigraphic Standard Profile for regionally correlative, discernible sedimentary units comprising Yatağan and Milet beds restricted to the Lycian hinterland.In this area sedimentation is represented by a coeval tripartite sequence ranging from alluvial-fan, fluvial and lacustrine deposits that laterally and vertically grade into each other.These units are collectively considered as 'neoautochthonous' and lithostratigraphically designated as the Çameli Formation by the Turkish Petroleum Corporation (TPAO) (Erakman et al. 1982a, b, Meşhur & Akpınar 1984, Erakman & Alkan 1986) and the Mineral Research and Exploration Directorate (MTA) (Şenel et al. 1989(Şenel et al. , Konak & Şenel 2002)).
A first attempt at incorporating faunal evidence in order to strengthen both correlations and palaeoenvironmental reconstructions of the SW Anatolian basins was undertaken by Alçiçek (2010).Although that study was largely based on Saraç (2003), a scientific report with many preliminary identifications, it did manage to produce a general framework confirming the three pulses of crustal extension caused the basin formation as earlier proposed by Alçiçek (2001), Alçiçek et al. (2005) and Alçiçek (2007).Since then, palaeontological information on the area has increased tremendously.In addition to recent biostratigraphical studies (e.g., Van den Hoek Ostende et al. 2015a, b), newly discovered localities which are currently being studied, as well as literature on the faunal evidence (e.g.Saraç 2003) that previously had gone unnoticed, have contributed to a more accurate definition of the timing of the major changes in the sedimentation mode in the region and the accompanying environmental changes.As part of the work is still in progress, we can anticipate further advances in the reconstruction of the late Neogene and Quaternary history of SW Anatolia.On the other hand, only very few palynological investigations of this region and period have been published.Reasons for this are mainly the lack of palynomorph bearing sediments (e.g.oxidised or Ca-carbonate or gypsum rich sediments) and a very limited stratigraphical value of terrestrial palynomorphs for this period.For instance the appearance of Fagus, Cedrus and Ilex defined the latest Miocene and early Pliocne pollen zone ("Yeni Eskihisar Pollen Bild") of Benda (1971), while recent palynological investigations of the Yatağan Basin documented these taxa already for the middle Miocene (Bouchal in press, in this issue).Here, we synthesise existing palaeontological, sedimentological and various chronostratigraphic data with new observations on the pre-existing and new mammal fossil locations from the Lycian orogen-top basins (such as Çameli, Eşen, Beyağaç, Yatağan, Baklan, Acıgöl, Burdur) in SW Anatolia to (re)define the stratigraphic framework and constrain the timing of broad palaeoenvironmental transitions in key Neogene basins of SW Anatolia.

The Çal Basin
The Çal Basin resides on the Lycian nappes and partly on the metamorphic Menderes Massif (Konak et al. 1986, Konak 2002).The basin succession unconformably overlies the bedrock and consists of two sequences which are separated by an angular unconformity.
These sequences comprise sediments deposited in alluvial-fan, fluvial and palustrine environments.The alluvial-fan association constitutes the basal part of the basin-fill, which thickens towards the basin boundary faults and shows a basinward fining trend.
Recently, new macro-mammal remains were discovered in marsh/swamp deposits that stratigraphically lie in between the fluvial and lacustrine deposits of the basin succession.The micro-and macro-mammal fossil content from the Sultandere locality (Fig. 1) revealed a diverse fauna implying a wide variety of habitats were present during the early/middle Pliocene (MN14/15, Ruscinian).Among the fossil mammals, the medium-sized deer Croizetoceros (Mayda et al. 2017) and the antelope Gazellospira are typical of the Plio-Pleistocene taxa, whereas the primitive gerbil genus Pseudomeriones has its latest representative in the late Pliocene (MN15) locality of Çalta, Turkey (Şen 1977, 1998, Sylvestrou & Kostopoulos 2007) (Fig. 2).A recent magnetostratigraphic study (Özkaptan et al. 2018) assigns 5.0-4.5 Ma age for the base of the lacustrine succession of the Burdur.This age determination calibrates our recent finding of MN15 biota in the Sultandere locality underlying the lacustrine succession of the Burdur basin (Table 1).
The uppermost reach of the basin succession, which consists of fluvio-deltaic deposits, yielded a Villanyian (MN17) fauna from the localities of Elmacık, Yassıgüme and Kocakır (Alçiçek et al. 2013b, Alpagut et al. 2015, Demirel & Mayda 2014, Demirel et al. 2016, 2017; Table 1,  Kocakır-2 is stratigraphically comparable but is much richer in species than Kocakır-1.The tentative results of the initial survey of Kocakır-2 showed the presence of two equids of different size (Equus cf.altidens and Equus suessenbornensis), a small rhino (Stephanorhinus cf.hundsheimensis), a giant camel (Paracamelus gigas), a panther (the size of P. gombaszoegensis), a wolf like dog (Canis arnensis), a hippo (Hippopotamus sp.) and a medium-sized bovid (Bovidae indet.)(Table 1).Overall, this fairly diverse fauna reflects an open habitat with a limited number of water bodies.The combination of Paracamelus, Equus and a medium-sized deer is typical for the middle-late Villafranchian associations of eastern Europe and western and central Asia (Alçiçek et al. 2013, Kalhke et al. 2011).
Further to the south, a locality near the village of Hasanpaşa is situated in the uppermost part of the lacustrine unit.This site yielded Mammuthus meridionalis and Gazella sp., indicating a late Pliocene-early Pleistocene age interval of 3.0-2.0Ma (MN17; middle Villanyian, Sickenberg et al. 1975, Saraç 2003).A recent magnetostratigraphic study indicates 2.5 Ma for the top of the succession (Özkaptan et al. 2018).This age determination calibrates MN17 biota from the Kocakır-1 (Alçiçek et al. 2013) and Kocakır-2 and Yassıgüme localities (Demirel & Mayda 2014) overlying the lacustrine succession of the Burdur basin (Table 1).
In the Gölcük volcanic province, c. 20 km to the NE of the basin, the basin succession interfingers with volcaniclastics of 4.77±0.25 to 4.07±0.20Ma in age (Lefevre et al. 1983).Price (1989) undertook K-Ar dating from tephra at the centrally placed Gölcük Maar, which provided an age of 4.6±0.2Ma.The volcanic intrusions and lava flows overlie Miocene deposits and interfinger with the basin-fill.The middle parts of the volcanics were assumed to be of late Pliocene age based on the tephra interlayers of that age in the adjacent Burdur graben.By using K-Ar age determination from tephra interlayers Nemec et al. (1998) showed that explosive activity of the Gölcük volcano continued until early Pleistocene time with the youngest activity in historical times at 1.50±0.18and 1.38±0.13Ka ago.

The Acıgöl Basin
The Acıgöl Basin resides on Mesozoic basement composed of allochthonous rocks of limestones and ophiolitic rocks of the Lycian Nappes, and overlying Oligocene marine to continental sediments (Konak et al. 1986, Şenel 1997, Konak & Şenel 2002, Turan 2002, Sözbilir 2005; Fig. 1).The basin strikes NE-SW and is developed within an eastward-tilted tectonic depression in which upper Miocene coarse-grained terrestrial sediments were initially deposited (Göktaş et al. 1989, Alçiçek 2009, Helvacı et al. 2013, Alçiçek et al. 2013a).From the Zanclean to Gelasian, a progressive deepening of the basin provided accommodation space for the deposition of lacustrine units, which unconformably overlie the pre-Neogene basement rocks.The only fossil mammal material from the basin was discovered by MCA in the alluvial-fan deposits of the uppermost reach of the Acıgöl basin-fill and represents a typical late Pleistocene element in the form of Equus hydruntinus (Alçiçek et al. 2013b).

The Çameli Basin
The Çameli Basin resides on the Lycian nappes and constitutes NE-trending inter connected tilt-block compartments associated with NW-dipping secondary normal faults (Fig. 1).The basin-fill was designated as the Çameli Formation by Erakman et al. (1982a, b) and Erakman & Alkan (1986), and comprises alluvial-fan, fluvial and lacustrine deposits.
Progressive angular unconformities are present within the proximal facies along the basin margins.The alluvial-fan deposits occur in the lower and upper parts of the basin-fill along the basin margin and grade laterally and vertically into the fluvial deposits.The fluvial deposits also grade laterally and vertically into lacustrine facies that are restricted to the central and upper part of the sequence.In the basin center, these tripartite deposits grade into each other and reach up to 500 m in thickness.The age of the basin-fill is determined to be Turolian to Villanyian based on mammal fauna and radiometric dating (Şenel 1997a,b,c, Saraç 2003, Alçiçek et al. 2005, Van den Hoek Ostende et al. 2015a,b, Elitez et al. 2017).The biostratigraphical studies by Van den Hoek Ostende et al. (2015a, b) have contributed to accurate definition of the exact timing of major changes in the basin's sedimentation mode.
The vertebrate fauna of coal-bearing deposits in the Elmalıyurt (Pırnaz) locality on the SE margin of the basin contains an upper dentition of a medium-sized hipparionine (Saraç 2003; Table 1).This mammal specimen was preliminarily identified by Saraç (2003) as the Vallesian species Hippotherium primigenium, and this identification was reiterated by other workers (Alçiçek 2001, Alçiçek et al. 2005).The characteristics of the H. primigenium group as defined by Bernor et al. (1996) 1; Fig. 2).
The alluvial-fan deposits grade upward into fluvial and eventually shallow lacustrine deposits.Initial lacustrine deposition is represented by marsh-swamps comprising freshwater ostracods and mollusks including Miocyprideis, Limnocythere, Candona, Pisidium, Ilyocypris, Cypridopsis, Cyprideis, Adelina, Corymbina, Paludina, Unio and Bulimus (Colin 1962, Becker-Platen 1970) and Cyprinodei remains of Onychoden, Mitraden and Tinca (Alçiçek 2007).The Corymbina gastropod species are very similar to those found in the Apolakkia Formation of SE Rhodos with middle-late Ruscinian age (MN15; lower-middle Pliocene; Van de Weerd et al. 1982).Upward the lacustrine deposits abound in mollusc, ostracod and fish assemblages representing deeper lake environment (Table 1).Later, the deep lacustrine basin eventually shrank and was filled in owing to renewed progradation of alluvial-fan and fan-deltaic deposits derived from the basin margins.

The Beyağaç (Barz) Basin
The Beyağaç basin was first described by Becker-Platen (1970; Barz Plain in there) and its geological map has recently been compiled by Akdeniz (2011a; Fig. 3).The basin contains two distinct sedimentary units; the Yatağan beds at the base, comprising alluvial-fan and fluvial deposits, and the Milet beds with lacustrine sediments at the top.
The basal Yatağan unit consists of alluvial-fan and fluvial deposits which thicken towards the basin boundary faults and show basinward thinning and fining trends.The Sazak locality, at the western basin margin, yielded fossils of Hipparion matthewi, Ceratotherium neumayri, Helladotherium duvernoyi, Protoryx carolinae, Tragoportax amalthea, Gazella deperdita and Adcrocuta eximia, indicating a middle Turolian age (MN12; Schmidt-Kittler 1976, Kaya 1993, Tuna 1999, Koufos et al. 2018).The new Kozlar locality at the eastern basin margin was discovered during this study and is still under investigation, but revealed equid (Hipparion) and rhinocero (Ceratotherium) material suggesting a middle Turolian age (MN12, Table 1; Fig. 2).Higher up in the seqeuence, the alluvial-fan deposits gradually pass upward into the fluvial facies association and are eventually overlain by the lacustrine Milet unit with a coal seam at the bottom.The basin-fill is unconformably overlain by younger alluvial-fan deposits.

Discussion
Regional crustal extension following the culmination of the Tauride orogeny gave rise to the development of several terrestrial basins in SW Anatolia (Şengör & Yılmaz 1981, Robertson & Dixon 1984, Şengör et al. 1985, Zanchi et al. 1993, Ten Veen et al. 2009).A combination of detailed bio-and lithostratigraphy of the basin fills underpins a wellconstrained model for the basin evolution that is used here as a solid time-stratigraphic framework enabling the improved timing of tectonic events along the Lycian hinterland.
The final nappe-related sedimentation in the region occurred during the early Miocene in piggy-back basins composed of terrestrial deposits, which were subsequently drowned by a Burdigalian transgression.This marine transgression was followed by regional uplift that led to local extension and formation of a NE-trending array of normal-fault bounded graben type basins.The reef unit presently stands at maximally 1846 m attributed to the gravitationally isostatic (orogenic) rebound of the nappe stack (Alçiçek & Ten Veen 2008).A 7 my period of non-deposition was followed by terrestrial sedimentation during the late Tortonian that dominated the extensional basins in the Lycian hinterland.The non-deposition period corresponded with a shift from compression to extension (Alçiçek et al. 2018).
On the Taurides in the SW Anatolia, Alçiçek (2001) attempted to obtain stratigraphic resolution that would enable an accurate definition for the duration of tectonic phases related to crustal deformation.Following that approach, Alçiçek et al. (2005) and Alçiçek ( 2007 presented here provides the means to place the basin development in the well-articulated regional tectonic framework (Ten Veen 2004, Alçiçek et al. 2006, Ten Veen et al. 2009).Late Neogene and Quaternary neotectonic developments in western Anatolia are characterized by extensional crustal deformation that resulted in the development of fault-bounded basins.This extension has strongly influenced the basin configuration, changed the sedimentation mode and given rise to several graben-type basins such as Çal, Baklan, Acıgöl, Burdur, Çameli, Eşen and Beyağaç.These basins, related to post-orogenic processes, were formerly presented as multiply pulsed orogen-top basins (Alçiçek 2001, Purvis & Robertson 2004, Alçiçek et al. 2005, Alçiçek 2007).Here, we synthesise the available data to develop a unified three phase model for basin sedimentation across the SW Anatolian region.

Phase I -Basin formation (late Tortonian)
The basal alluvial flood plain deposits of the SW Anatolian basins abound in large fossil mammal remains including the localities of Mahmutgazi in Baklan, Asarlık in Çal, Elmalıyurt (Pırnaz) in Çameli, Karamusalar in Eşen, Şerefköy in Yatağan, Sazak and Kozlar in Beyağaç, Kemer in Burdur basins (Table 1, Fig. 2).The fossils found in these localities are typical of the so-called Greco-Iranian or sub-Paratethyan province, also known as the Pikermi biome (Geraads 2017, Kaya et al. 2012, Pickford 2016) Phase II -Lacustrine period (early Pliocene) The initial basin-fill composed of alluvial-fan and fluvial deposits was subsequently drowned by extensive lakes by the early Pliocene.These initial lacustrine deposits are marked by shallow-lacustrine facies assemblages of marsh-swamp environment, which abound in fossil micro-mammals and amphibians.These conditions are most common in balanced-fill lake, characterized by the rates of sediment/water supply in balance with potential accommodation (Carroll & Bohacs 1999).The timing of the lacustrine inundation has been well established by microvertebrate remains from the locality of Ericek in the Çameli basin (Alçiçek 2001, Alçiçek et al. 2005 given, for instance, the high proportion of desmanine moles in the locality of Afşar (Table 1, Fig. 2).A similar fossil mammal reported by Saraç (2003) from the Bozarmut locality in the Yatağan basin extends the lacustrine inundation further to the west.The Mio-Pliocene boundary saw a major faunal turnover in the Mediterranean mammal faunas, which in the east marks the end of the Pikermian biome (Eronen et al. 2009).In SW Anatolia, this turnover is marked by the presence of various wood mice and a palaeobatrachid frog in the Ericek locality of the Çameli basin (Van den Hoek Ostende et al. 2015b).
Initial shallow lacustrine basins gradually deepened as marked by thick, homogeneous marly carbonate deposits.The deep lacustrine deposits are concentrated to the centres of the basins, and locally overlap the basin margins implying a lacustrine inundation following renewed basin subsidence possibly owing to renewed extension.Eventually the individual lakes were united to constitute a single mega-lake in SW Anatolia during the Pliocene (Spratt & Forbes 1847, Becker-Platen 1970, Luttig & Steffens 1976, Görür et al. 1995, 1998).Such a palaeo-lake environment was envisaged by Bering (1971) as the Pisidic Lake.Pamir (1974) has further extended this connection up the Denizli basin to the north on the basis of the presence of Cardium assemblages.

Phase III -Basin dissection (early Pleistocene)
The adjoined lake basins gradually and synchronously shrank by the early Pleistocene as During the early Pleistocene, a renewed pulse of extension prompted the deposition of coarse-grained alluvial-fan sediments derived from the basin margins interfingering with the lacustrine sediments towards the basin centre.In this stage, the lake accommodation space was eventually exhausted, as is indicated by the basin-wide expansion of alluvial to fluvial sedimentation.This stage was attributed to a change in the direction of extension that is considered to have affected the entire area of SW Anatolia (Ten Veen 2004, Alçiçek et al. 2006, Ten Veen et al. 2009).During this phase, the mega-basin became totally dissected.
Lower Pleistocene coarse clastic alluvial-fan deposits that unconformably overlie older Neogene units in SW Anatolia exemplify the renewed extension.This alluvial unit has a distinct dark-red colour with prominent pedogenic horizons in the over-bank deposits.The succeeding (i.e., Holocene) period is characterized predominantly by degradation of topographic highs through deeply incising river erosion.Newly generated faults as well as reactivated faults are thought to have been associated with subduction roll-back extension, which further enhanced the basin-and-range topography of SW Turkey (Alçiçek et al. 2005, Alçiçek 2007, Ten Veen et al. 2009).

Conclusions
The

Unit Fossil assemblages Age
Alluvial-fan
are complex pre-and post-fossette enamel plications; maintaining deeply amplified plis, and an incised hypoglyph accompanying the lingually flattened, labially rounded and more lingually placed protocone.Comparing the mean protoconal length and the plication count, the Elmalıyurt specimen differs from those of H. primigenium from Höweneg (MN9-Vallesian), and Eppelsheim (MN9-10; Vallesian) by having a moderate enamel plication (15-20 plicae) with short-narrow plis, oval, relatively small protocone (6-8 mm) free from protoloph with weak and asymmetrical double pli caballin.Instead, the medium-sized Elmalıyurt hipparion is comparable with the Turolian forms of Bulgaria and Greece, especially those from the Anatolian faunas of Sivas-Düzyayla (MN11, early Turolian, Kaya & Forsten 1999), Uşak-Kemiklitepe A-B (MN11-12, earlymiddle Turolian, Koufos & Kostopoulos 1994), Muğla-Şerefköy (MN12; early Turolian, Kaya et al. 2012) and Özlüce (MN11, early Turolian, Alpagut et al. 2014).In particular, H. mediterraneum, which is well-represented from middle Turolian (MN 12) localities from Greece (Pikermi and Perivolaki), Bulgaria (Kalimantsi and Hadjidimovo) and Turkey (Kemiklitepe A-B and Düzyayla, closely resembles the Elmalıyurt hipparion in size and morphology.In view of the existing material, we classify the Elmalıyurt specimen as Hipparion cf.mediterraneum, noting that it certainly does not represent H. primigenium, but rather resembles Turolian forms, especially H. mediterraneum.Consequently, the Elmalıyurt locality in the lowermost part of the Çameli basin succession is considered to be Turolian in age.The lacustrine unit in the basin is confined by coal-bearing marsh-swamp deposits at the bottom and top.At the base, the Ericek locality contains murines (Apodemus cf.dominans, Rhagapodemus cf.primaevus, Orientalomys cf.similis), arvicoline (Mimomys occitanus), cricetine (Cricetulus), glirid (Muscardinus), and shrew (Asoriculus sp.), which were assigned to late MN15, i.e., late Ruscinian (Van den Hoek Ostende et al. 2015a, Table1; Fig.2).Higher in the section, the unit grades from a shallow to deep lake environment.The mollusc content, with Paludina,Lymnaea, Radix, Lithoglyphus, Pyrgula (Becker-Platen 1970), Melanopsis, Pseudamnicola(Alçiçek et al. 2005) and ostracods of Cyprideis pannonica, Candona parallela pannonica, Heterocypris salina, Ilyocypris sp., Eucypris sp.(Darbaş 2017), marks the transition from shallow to deeper lake environments.The uppermost part of the succession grades again into coal-bearing marsh-swamp deposits abounding in mammal remains including cricetines, arvicolines and murines, similar to the locality of Bıçakçı (MN17, late Villanyian;Alçiçek et al. 2005, Van den Hoek Ostende et al. 2015b; Table ) described terrestrial orogen-top basins such as Çameli and Eşen and distinguished three distinct pulses of crustal extension that occurred in the late Miocene, middle Pliocene and early Pleistocene times, respectively.Spatial and temporal correlation of the facies associations in each individual basin indicate that they are correlative and deposited coevally with typical tripartite facies associations; alluvial-fan facies at the margin, fluvial and lacustrine facies in the centre.The post-orogenic terrestrial basins collectively provide sedimentary and stratigraphic data describing synchronicity of the individual basin development and related sedimentation as well as describing interconnections between the tectonic provinces.The new age control . This assemblage is suggestive of open forested landscapes ranging from sclerophylous evergreen to mixed conifer and deciduous woodlands to open xerophyic terrains forming a mosaic of different plant associations (Jiménez-Moreno et al. 2007, Biltekin et al. 2015) and indicating relatively humid climatic conditions in the late Tortonian.Around 5.9 Ma (late Turolian), an onset of drastic climatic change with greater aridity and continentality and cooler climate occurred in the eastern Mediterranean in combination with the continued convergence between Africa and Europe.This led to easier and more rapid faunal exchanges between the two continents.However, only a sparse record of large grazing mammals, living in open areas, is found in the late Turolian.These taxa adapted to more dry and open environments.Climate became more arid at the end of the late Miocene, resulting in more open vegetation and more rare forest vegetation (Biltekin et al. 2015).All of the fossil localities observed in the lowermost stratigraphy of each basin have a similar age range of early-middle Turolian (MN11-12).Therefore, it appears that the SW Anatolian post-orogenic basins subsided synchronously and initially filled with alluvial-fan deposits in a high-energy setting.During the basin subsidence, the marginal alluvial-fans from the basin-bounded escarpments supplied rivers running along the basin axis and accompanied by ephemeral lakes in the basin center.The basins were underfilled, represented by the rate of potential accommodation exceeding rate of sediment/water supply, gradually filling with a fining-upward fluvial sequence in which braided streams predominated, punctuated by sheetfloods and graded into meandering systems(Caroll & Boharcs 1999).Eventually these fluvial systems were gradually drowned by shallow-lacustrine marsh-swamp environments.
,Van den Hoek Ostende et al. 2015a).At the lowermost part of the lacustrine succession, cypriniform fish assemblages were reported byRutte & Becker-Platen (1980) in the Baklan basin andAlçiçek (2007) found similar cypriniform assemblages in the Eşen basin.New fossil mammals yielded from the Sultandere locality of Burdur and the Afşar locality of Sandıklı are of Ruscinian age, supporting the lacustrine inundation throughout SW Anatolia and also implying humid climatic conditions at that time, indicated by a gradual transition of homogeneous lacustrine marls into shallow lacustrine marsh-swamp deposits.The shallow lacustrine environments abound in fossil micro-and macro-mammal assemblages across the entirety of SW Anatolia.Locations include the Bıçakçı locality in Çameli, Kırmızıtepe locality in Çal, Gelinören locality in Baklan, Yelalan locality in Acıgöl and Kocakır, Elmacık, Yassıgüme and Ardıçtekke localities in Burdur basins (Alçiçek 2001, Alçiçek et al. 2005, Wesseling & Alçiçek 2010, Alçiçek et al. 2012, 2013a, Demirel & Mayda 2014, Van den Hoek Ostende et al. 2015a, b, Alçiçek et al. 2017).The more open vegetation conditions are well-reflected in the Bıçakçı fauna at the demise of the lacustrine period with subhumid climatic conditions.That fauna is dominated by hamsters (cricitines), and shows in addition a large variety of voles (microtines).Murids, which were dominant in the preceding period, now play a far more modest role (Van den Hoek Ostende et al. 2015a, Alçiçek et al. 2017).
sedimentary architecture of SW Anatolian terrestrial basins has been linked to multiple pulses of extension that are reflected in palaeoenvironmental changes.Strongly concerted environmental changes in the basins are based on their integrated faunal-and depositional assemblages.Stratigraphy and sedimentation patterns of the mammal bearing strata in this Lycian orogen-top domain allows us to present a regional inter-basinal correlation and palaeobiogeographical reconstruction over the Anatolian gateway, which is uniquely located along the migration route critical to the fauna of the Old World.Biostratigraphic constraints in these basins have been reassesed with the support of new fossil finds to calibrate and ageconstrain the palaeoenvironments within a regional palaeogeographic framework.The fossil associations have been combined with the sedimentation pattern to refine the post-orogenic basin development and regional palaeobiogeography throughout the Lycian Taurides.Our studies have reaffirmed the triparte nature of the sedimentation in the various basins, which is synchronous and represents a late Miocene, Pliocene and early Pleistocene phase, each with its own particular environments.Terrestrial sedimentation on the Lycian hinterland had commenced by the late Tortonian (early Turolian) following c. 7 my of non-deposition following the latest marine transgression in the region.In the early stage, the basins subsided to form a transition from coarse-clastic alluvial-fans and axial fluvial systems.These alluvial flood-plain deposits abound in large mammal taxa of the Pikermi biome, implying an open, seasonal palaeoenvironment with grass-dominated steppe ecosystem.The terrestrial fossil assemblages correlate with those of adjacent basins indicating palaeobigeographical connections.By the early Pliocene (late Ruscinian), gradual transition from an alluvial-fan environment into a fluvial system was initiated by regional climatic variations changing into warm and more humid conditions with savannah-type open habitats, resulting in base-level rise, lake expansion, ascending river gradient and increased flow-capacity.The humidity was sustained until the late Pliocene, when shallow-palustrine lacustrine environments comparable with the modern SW Anatolian lacustrine basins appeared.The fossil associations underlying and overlying the Pliocene lacustrine deposits indicate the duration of the lake phase of at least 1 ma.By the early Pleistocene (latest Villanyian), the basin was dissected by newly generated faults and the the basin configuration was re-arranged.The base-level changes resulted in coarse-clastic alluvial-fan to fluvial material unconformably overlying the earlier deposits in the basins.This unit contains large mammal taxa representing an open steppe ecosystem under more temparate (i.e.semiarid) climatic conditions.

Fig. 1 .
Fig.1.(A) Tectonic map of the Aegean and western Turkey showing the major tectonic structures (Bozkurt 2003); (B) Overview of the prominent extensional basins of western Anatolia surrounding the Çameli Basin (based onKonak 2002, Konak & Şenel 2002, Şenel 2002, Turan 2002).The fossil localities subjected in this study are indicated.See Fig.2 and 3for the stratigraphic position of the fossil sites and Table1for their contents.
Table 1 for their contents.