Planktonic foraminiferal biostratigraphy of the Coniacian-Maastrichtian sequences of the Bey Dağları Autochthon, western Taurides, Turkey: thin-section zonation

Cretaceous Research 30 (2009) 1103–1132

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Planktonic foraminiferal biostratigraphy of the Coniacian-Maastrichtian sequences of the Bey Dag˘ları Autochthon, western Taurides, Turkey: thin-section zonation Bilal Sarı _ ¨ niversitesi, Mu ¨l U ¨ hendislik Faku ¨ ltesi, Jeoloji Mu ¨ hendisliqi Bo ¨lu ¨ mu ¨ , Tınaztepe Yerles¸ kesi, 35160 Buca-Izmir, Dokuz Eylu Turkey

a r t i c l e i n f o

a b s t r a c t

Article history: Received 13 February 2007 Accepted in revised form 29 March 2009 Available online 7 April 2009

Planktonic foraminifer distributions in seventeen stratigraphic sections of Upper Cretaceous hemipelagic and pelagic sequences of northern Bey Dag˘ları Autochthon (western Taurides) yield six biozones such as, Dicarinella concavata Interval Zone, Dicarinella asymetrica Range Zone, Radotruncana calcarata Range Zone, Globotruncana falsostuarti Partial Range Zone, Gansserina gansseri Interval Zone, and Abathomphalus mayaroensis Concurrent Range Zone. Two of the zones, Dicarinella concavata Zone and Dicarinella asymetrica Zone, are identified in the massive hemipelagic limestones of the Bey Dag˘ları Formation, of Coniacian-Santonian age. They are characterized by scarce planktonic foraminifera and abundant calcisphaerulids. The other four biozones are determined from the cherty pelagic limestones of the Akdag˘ Formation and indicate a late Campanian-late Maastrichtian time interval. The planktonic foraminifera observed in these four biozones are diverse, complex morphotypes (K-selection), suggesting open oceans. The assemblage of the Abathomphalus mayaroensis Zone shows that the latest Maastrichtian record is absent throughout the northern part of the autochthon. Two main sedimentary hiatuses are recognized within the Upper Cretaceous pelagic sequence. Early to middle Campanian and latest Maastrichtian-middle Paleocene planktonic foraminifera are absent in all measured stratigraphic sections. Hiatus durations differ between sections as a result of diachronism of onset of the hemipelagic and pelagic deposition and the post-Santonian and post-Maastrichtian erosional phases. Drowning event and the early-middle Campanian and latest Maastrichtian-middle Paleocene hiatuses in the pelagic sequence are attributed to regional tectonics during the Late Cretaceous. Ó 2009 Elsevier Ltd. All rights reserved.

Keywords: Planktonic foraminifera Biostratigraphy Thin-Section Zonation Upper Cretaceous Bey Dag˘ları Autochthon Western Taurides

1. Introduction The distribution of planktonic foraminifera yields information on the time of onset and age of pelagic deposits and the duration of stratigraphic hiatuses. This is important because pelagic deposits are key to palaeogeographic reconstructions and recognition of geodynamic events (such as timing of tectonic events, platform drowning, fluctuations in sea level and erosional events) in the Mesozoic Tethys (Farinacci and Yeniay, 1986; Okay et al., 2001). The study of planktonic foraminifera using thin-sections of indurated carbonate rocks has a long history (e.g., de Lapparent, 1918; Renz, 1936; Vogler, 1941; Bolli, 1945; Postuma, 1971). More recent papers demonstrating such methodology include Wonders (1979), Fleury (1980), Weidich (1987), Sliter (1989), Sliter and Leckie (1993), Premoli Silva and Sliter (1994), Simmons et al. (1996), Sliter (1999), Robaszynski et al. (2000), Premoli Silva and Verga

E-mail address: [email protected] 0195-6671/$ – see front matter Ó 2009 Elsevier Ltd. All rights reserved. doi:10.1016/j.cretres.2009.03.007

¨ zkan (1985), Farinacci (2004). Papers specific to Turkey include O ¨ zkan and Ko¨ylu¨og˘lu (1988), O ¨ zkan-Altıner and and Yeniay (1986), O ¨ zcan (1999), Yakar (1993), Sarı (1999, 2006a,b), Sarı and O ¨ zer O (2002) and Okay and Altıner (2007), which contain thin-section illustrations of planktonic foraminifera. The various Upper Cretaceous biostratigraphic zonations were revised and reconciled by the European Working Group on Cretaceous Planktonic Foraminifera (Robaszynski and Caron (coordinators), 1979 and Robaszynski et al., 1984) and by Caron (1985) to reduce the complexity caused by the multitude of previously established taxa. Premoli Silva and Sliter (1994), Robaszynski and Caron (1995) and Robaszynski (1998) have calibrated the planktonic foraminiferal biozones according to the time scale of Gradstein et al. (1994). The resolution of thin-section zonation is nearly as precise as zonal schemes based on isolated specimens (Sliter, 1989). Nearly four decades of study has been devoted to the clarification of the stratigraphy and tectonics of the Bey Dag˘ları Autochthon (Poisson, 1977; Gutnic et al., 1979; Farinacci and Ko¨ylu¨og˘lu, 1982;

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Fig. 1. a, Main tectonic units of Turkey (after Go¨ru¨r and Tu¨ysu¨z, 2001); b, Geological map of the western Taurides (simplified from S¸enel, 1997) showing location of the measured stratigraphic sections.

B. Sarı / Cretaceous Research 30 (2009) 1103–1132 Table 1 Table showing the stratigraphic sections studied in this study and in a previous paper (Sarı, 2006a) Figure No

Section No

Stratigraphic Sections (from northeast to southwest)

11 6 10 14 20 19 12 21 22 17 4 7 18 23 15 16 13

S-1 S-2 S-3 S-4 S-5 S-6 S-7 S-8 S-9 S-10 S-11 S-12 S-13 S-14 S-15 S-16 S-17

¨ ZET TAS¸I GO ALADG˘ KOCABOG˘AZ DERE ALA TEPE _ KOCAALILER _ I_ DERE DEMIRC KIRAÇ TEPE _ IBURNU _ ENIKL YAG˘CA CANAVAR BOG˘AZI ¨Y KARGALIKO _ DERE FEDIL _ IG _ ˘ I_ SAVRAN EKINL BOZCALAR DERE YUMRUÇALI TEPE ¨ LU ¨ KDAG˘ TEPE BO ¨Y TEKKEKO

Sections already studied in Sarı (2006a)

as Section-1

as Section-4

¨ zgu¨l, 1984; Waldron, 1984a,b; Poisson, 1984; Poisson et al., 1984; O ¨ zkan and Ko¨ylu¨og˘lu, 1988; Naz et al., Farinacci and Yeniay, 1986; O ¨ zer, 2001, 2002, 2009; 1992; Sarı, 1999, 2006a,b; Sarı and O Robertson et al., 2003; Poisson et al., 2003; Sarı et al., 2004, 2009). Although Upper Cretaceous pelagic limestones are widely exposed in the Bey Dag˘ları Autochthon, there few studies which address the planktonic foraminiferal biostratigraphy of these limestones ¨ zkan and Ko¨ylu¨og˘lu, 1988; Sarı, 1999; Sarı and (Poisson, 1977; O ¨ zer, 2002; Sarı, 2006a,b). These studies have shown that the O Upper Cretaceous pelagic sequence is characterized by important sedimentary gaps. The first detailed study covering the taxonomy and biostratigraphy of the Upper Cretaceous planktonic foraminifera was carried out in the Korkuteli area by Sarı (1999), and further developed by Sarı (2006a,b). Late Cretaceous evolution of the Bey Dag˘ları carbonate platform between Susuzdag˘ and Çamlıdere has been examined using data from foraminifera and rudist biostratigraphy and Sr-C-isotope stratigraphy (Sarı, 2006b). The purpose of this paper is to present the Upper Cretaceous (Coniacian-Maastrichtian) planktonic foraminiferal distribution and biozonation of the hemipelagic and pelagic limestones of seventeen stratigraphic sections measured from the northern part of the Bey Dag˘ları Autochthon between Susuzdag˘ and Çamlıdere (Fig. 1). As the hemipelagic and pelagic limestones are hard, planktonic foraminifera were studied in thin-section. This paper represents a continuation of research described in a previous paper (Sarı, 2006a), which focussed on the Upper Cretaceous planktonic foraminiferal biostratigraphy of the Korkuteli area. Current research examines the stratigraphic distribution of planktonic foraminifera from an additional fifteen stratigraphic sections measured to the north and south of the Korkuteli area (Fig. 1). As the primary or nominate species and secondary, stratigraphically important species were decribed in the previous paper (Sarı, 2006a), they are not repeated in this study.

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1982; Naz et al., 1992; Robertson, 1993) (Fig. 1). During the Mesozoic, the autochthonous unit was part of a larger crustal fragment of the African palaeomargin which can be traced in the Taurides and Zagrides to the east, and the Hellenides, Dinarides and Apennines to the west (S¸engo¨r and Yılmaz, 1981; Farinacci and Ko¨ylu¨og˘lu, ¨ zgu¨l, 1984; Farinacci and Yeniay, 1986; 1982; Poisson et al., 1984; O Robertson, 1993; Robertson et al., 2003). The Bey Dag˘ları Autochthon corresponds to the westernmost part of the Geyik Dag˘ı Unit of ¨ zgu¨l (1976, 1984). O The initial works dealing with the Bey Dag˘ları Autochthon and neighbouring areas introduced information on geology, tectonostratigraphy and biostratigraphy of the autochthonous and allochthonous units (Altınlı, 1944, 1945; Colin, 1962; Brunn et al., ¨ zgu¨l and Arpat, 1973; O ¨ zgu¨l, 1970, 1971; Dumont et al., 1972; O 1976). These works produced important data about the place of the Bey Dag˘ları in the regional context and contributed to the present knowledge of the highly complex geology of the area. The first detailed biostratigraphic data including planktonic foraminifera content of the Upper Cretaceous hemipelagic and pelagic limestones were presented by Poisson (1977) and Gutnic et al. (1979). Many studies since the early 1980s have been carried out to understand the Late Cretaceous palaeogeographic and palaeotectonic evolution of the region (S¸engo¨r and Yılmaz, 1981; Poisson, ¨ zgu¨l, 1984; Waldron, 1984a,b; Rob1984; Poisson et al., 1984; O ertson, 1993, 1998; Robertson et al., 2003; Okay et al., 2001; Poisson et al., 2003). These studies show that the Late Cretaceous was a time of widespread intense tectonic events especially in the

2. Geological setting The Bey Dag˘ları Autochthon represents a segment of Mesozoic Tethyan platform on which carbonate accumulation persisted from the Triassic to the early Miocene. This segment was overthrusted by the Antalya nappes in the east and by the Lycian nappes in the ¨ zgu¨l, 1976; Poisson, 1977; Farinacci and Ko¨ylu¨og˘lu, northwest (O

Fig. 2. Generalized stratigraphic columnar section of the northern part of the Bey Dag˘ları Autochthon. (See Fig. 5 for explanations).

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Fig. 3. Lithostratigraphic column of the Upper Cretaceous sequence of the northern part of the Bey Dag˘ları Autochthon. The planktonic foraminiferal biozones identified from the hemipelagic limestones of the Bey Dag˘ları Formation and the pelagic limestones of the Akdag˘ Formation have been correlated with the recent biozonations offered for the Upper Cretaceous sequences. The identified planktonic foraminiferal biozones indicate the presence of two stratigraphic hiatuses corresponding to the early-middle Campanian and the latest Maastrichtian. Time table was adapted from Gradstein et al. (1994). The explanation of the numbers in the subzone column of Robaszynski et al. (2000) are as follows; 1: D. concavata rare, 2: D. imbricata, 3: D. concavata abundant, 4: D. asymetrica, 5: S. carpatica, 6: G. stuartiformis, 7: G. elevata, 8: S. rugocostata, 9: G. arca, 10: G. ventricosa abundant, 11: G. calcarata, 12: G. falsostuarti, 13: G. wiedenmayeri, 14: A. kefiana?, 15: G. stuarti, 16: C. contusa, 17: G. linneiana, 18: A. mayaroensis, 19: P. reicheli.

Table 2 Table showing the thickness (m) of the identified planktonic foraminiferal biozones in each stratigraphic section Stratigraphic Sections

Planktonic Foraminiferal Biozones

Figure No

Section No

Sections (from northeast to southwest)

D. concavata Interval Zone

D. asymetrica Range Zone

R. calcarata Range Zone

G. falsostuarti Partial Range Zone

G. gansseri Interval Zone

A. mayaroensis Concurrent Range Zone

11 6 10 14 20 19 12 21 22 17 4 7 18 23 15 16 13

S-1 S-2 S-3 S-4 S-5 S-6 S-7 S-8 S-9 S-10 S-11 S-12 S-13 S-14 S-15 S-16 S-17

¨ ZET TAIS¸I GO ALADG˘ KOCABOG˘AZ DERE ALA TEPE _ KOCAALILER _ I_ DERE DEMIRC KIRAÇ TEPE _ IBURNU _ ENIKL YAG˘CA CANAVAR BOG˘AZI ¨Y KARGALIKO _ DERE FEDIL _ IG _ ˘ I_ SAVRAN EKINL

– 3þ –

14þ 3.5 23þ

3 18 – 27 – – – – – – – – – – – – 7

6þ 5.5 – 21 – – – – – – 2.5 – – – 10 10þ 3

– 10 0.5þ 46 5.5 1.5 – 9.5þ 4 7þ 5.5 1.5þ 6.5 22 48þ 10

– 2 – 2þ – – – – – – – – 0.5 6.5 32þ – –

BOZCALAR DERE YUMRUÇALI TEPE ¨ LU ¨ KDAG˘ TEPE BO ¨Y TEKKEKO

18 – –

– – 4

– – – 5.5 – – – – – –

– – – 9 6 – – – – –

Fig. 4. Stratigraphic distribution of the planktonic foraminifera in the Kargalıko¨y section. (See Fig. 5 for explanations and Fig. 1 for location of the section).

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neritic and pelagic carbonates (Poisson, 1977; Gutnic et al., 1979; ¨ zkan Farinacci and Ko¨ylu¨og˘lu, 1982; Farinacci and Yeniay, 1986; O ¨ zer, and Ko¨ylu¨og˘lu, 1988; Naz et al., 1992; Sarı, 1999; Sarı and O 2001, 2002; Sarı et al., 2004; Sarı, 2006a,b). 3. Material and methods

Fig. 5. Lithology, fossil and sedimentary structure explanation for all measured stratigraphic sections.

eastern Mediterranean region. The tectonics changed from extensional to compressional during this critical period as a result of plate re-organisation (Robertson, 1993, 1998), which led to the emplacement of the ophiolite nappes over the carbonate platforms. Details of the Late Cretaceous reconstruction of the area (i.e., the number and size of carbonate platforms and troughs separating the carbonate platforms and the origin of the nappe piles) are still under discussion because of complex palaeotectonic history (Robertson, 1993; Poisson et al., 2003). The Bey Dag˘ları carbonate platform (BDCP) was one of the many Mesozoic Tethyan carbonate platforms initiated as a result of flooding of blocks, which had rifted from the northern margin of Gondwana during Mid-Late Triassic (following Late Permian-Early Triassic rifting) throughout the southern part of the Eastern Mediterranean region (S¸engo¨r and Yılmaz, 1981; Robertson, 2002). The BDCP passed through the entire predicted geodynamic spectrum of the Wilson cycle: rifting, drifting, transtension, transpression, and collision (Bosellini, 1989). The BDCP is reconstructed as an isolated carbonate platform, which was the southernmost representative of the girdle of intraoceanic platforms extending from the western Mediterranean to the eastern Mediterranean Neotethys during the late Cenomanian (Dercourt et al., 2000). The time of onset of pelagic deposition, age of the pelagic deposits and the determination of the stratigraphic hiatuses are important, because pelagic deposition always has been regarded as key to palaeogeographic reconstructions and recognition of geodynamic events in the Mesozoic Tethys (Farinacci and Yeniay, 1986; Okay et al., 2001). The Bey Dag˘ları Autochthon was under the influence of different tectonic regimes during the Late Cretaceous, a time of intense tectonic movements in this critical area of eastern Mediterranean. Late Cretaceous tectonic activities are thought to be responsible for the drowning of carbonate platforms, the opening of small oceanic basins and the collision of different tectonic units. Many studies have shown that the Upper Cretaceous sequences are characterized by breaks in deposition and important facies variations in both

Closely-spaced 873 samples were collected from pelagic and hemipelagic limestones in nineteen measured stratigraphic sections located in the northern part of the Bey Dag˘ları Autochthon. Four stratigraphic sections were previously presented in Sarı (2006a). The fifteen stratigraphic sections and two of the previously published stratigraphic sections (i.e., Kargalıko¨y and Bozcalar Dere sections) are presented in this study to construct the biostratigraphic framework and to present correlation of the Upper Cretaceous sequences (Fig. 1, Table 1). The samples were collected systematically throughout the sections as closely spaced as possible. The samples were taken from the massive hemipelagic limestones of the Bey Dag˘ları Formation and thin- to mediumbedded pelagic limestones of the Akdag˘ Formation. As the hemipelagic and pelagic limestones are hard and indurated, it was not possible to disaggregate the limestones and process normal washed-sample method; therefore thin-sections were prepared to analyse the planktonic foraminifera. A large number of specimens was observed in the thin-sections, but most of them were partial or oblique cuts through the tests and of no use for identification purposes. Only axially oriented forms were picked to identify most taxa with a high degree of confidence, as most of the diagnostic criteria can be recognized in such axial and/or subaxial sections. Atlases of European Working Group on Cretaceous Planktonic Foraminifera by Robaszynski and Caron (coordinators, 1979) and Robaszynski et al. (1984), Caron (1985) and Premoli Silva and Sliter (1994) are the basis for the identifications in this study. In addition, ¨ zkan and Postuma (1971), Wonders (1979), Fleury (1980), O Ko¨ylu¨og˘lu (1988), Sliter (1989), Robaszynski et al. (2000) and Premoli Silva and Verga (2004) are useful references, as they include thin-section illustrations of planktonic foraminifera. 4. Lithostratigraphy The Upper Cretaceous sequence of the Bey Dag˘ları Autochthon comprises two formations. The Bey Dag˘ları Formation in the northern part of the autochthon can be divided into two parts. The approximately 700-m-thick middle Cenomanian-Coniacian inner platform-peritidal carbonates form the basal part and are capped with the 26-m-thick Coniacian-Santonian hemipelagic limestones that form the upper part. The 100-m-thick upper Campanian-upper Maastrichtian Akdag˘ Formation comprises planktonic foraminifera-bearing pelagic limestones and disconformably overlies the different stratigraphic levels of the Bey Dag˘ları Formation along a prominent hardground or erosional surface. The Paleogene pelagic marls disconformably rest over the different stratigraphic levels of the Upper Cretaceous sequence (Fig. 2). The neritic part of the Bey Dag˘ları Formation is generally made up of grey-cream coloured limestone. It is locally bituminous, mainly medium- to thickly (30–100 cm) bedded, but locally thinly or massively bedded limestone. The neritic limestones mainly accumulated in a platform interior environment without any terrestrial sediment input. Microscopic studies have indicated peritidal (tidal flat, ponds and channels), subtidal, shelf (restricted circulation), shelf lagoon (open circulation), winnowed edge, organic build up and foreslope environments (Sarı, 2006b). The lower part of the platform limestones (middle-upper Cenomanian) is represented by rich benthonic foraminiferal

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Fig. 6. Stratigraphic distribution of the planktonic foraminifera in the Aladag˘ section. (See Fig. 5 for explanations and Fig. 1 for location of the section).

assemblages, while the upper part (Turonian-Coniacian) contains poor assemblages with nondiagnostic species. These data correlate well with the other Mediterranean successions. Appearance of Moncharmontia apenninica-compressa and Pseudocyclammina sphaeroidea in the upper part of the platform limestones indicate late Turonian and Coniacian respectively (Sarı et al., 2009). The uppermost part of the neritic succession in the northern part of the autochthon is also characterized by the abundance of rudist bivalve Vaccinites praegiganteus (Toucas) (hippuritid lithosome). The lithosome can be traced patchily throughout the northernmost part of ¨ zer, 2009). the autochthon as a key marker level (Sarı and O Geochemical analysis of well-preserved low-Mg calcite of shells of Vaccinites praegiganteus (Toucas), measuring for 87Sr/86Sr values,

has yielded a late Turonian age (mean numerical age: 89.1– 90.1 Ma) (Sarı et al., 2004). The data mentioned above and the C-isotope stratigraphy of the Cenomanian-Turonian neritic limestones from the Korkuteli area show that the neritic accumulation persisted from middle Cenomanian to the Coniacian in the Bey Dag˘ları carbonate platform without any pelagic incursion (Sarı et al., 2005). The massive hemipelagic limestones cap the neritic limestones and form the upper part of the formation. These hemipelagic limestones are massive, cream-coloured and fractured, and contain sparse planktonic foraminifera and abundant calcisphaerulids. The neritic and hemipelagic limestones are similar in appearance (i.e., textures on broken, fresh surface are the same) and therefore

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Fig. 6. (continued).

cannot be differentiated from each other in the field. The maximum thickness of the hemipelagic level is 26 m measured from the Kocabog˘az Dere section. The limestones, in which the planktonic foraminifera first appear, are arguably considered to be the transitional zone between the neritic and hemipelagic facies. Rudist fragments, echinoids, bryozoans, rare inoceramid fragments and abundant calcisphaerulids accompany the foraminiferal assemblage in the lowermost part of the level. The poor planktonic foraminiferal assemblage indicates a late Turonian-Santonian age according to the zonal scheme of Robaszynski and Caron (1995). As the hemipelagic limestones overlie the late Turonian-Coniacian rudistid neritic limestones, the oldest age assignable to the hemipelagic limestones is Coniacian. (Fig. 3). The upper Campanian-upper Maastrichtian Akdag˘ Formation disconformably overlies different stratigraphic levels of the Bey Dag˘ları Formation along a prominent surface (hardground or erosional surface). The surface is characterized by Fe-Mn oxidation, silicification and bioturbation, indicative of a later period of

sediment starvation (Rosales et al., 1994). The Akdag˘ Formation is mainly composed of thin- to medium-bedded (8–10 cm), locally thick-bedded (30–100 cm), planktonic foraminifera-bearing, greycream-coloured, cherty limestones. The pelagic limestones in some sections have fine pebble and sand-size intraclasts derived from the different stratigraphic levels of the underlying pelagic, hemipelagic and neritic limestones. The formation thickness varies laterally attaining a maximum thickness of 100 m. These limestones are generally distinctly bedded and contain abundant brown and greycoloured chert nodules and interlayers throughout. The limestones of the Akdag˘ Formation are a planktonic foraminifera-bearing biomicrite. Examination of the planktonic foraminiferal assemblages of the pelagic limestones of the Akdag˘ Formation yields a late Campanian-late Maastrichtian age (Fig. 3). Paleogene pelagic marls form the base of the Tertiary sequence. They begin, locally with a thin pelagic conglomerate and disconformably overlie different stratigraphic levels of the Upper Cretaceous sequence (Fig. 3).

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Fig. 7. Stratigraphic distribution of the planktonic foraminifera in the Fedil Dere section. (See Fig. 5 for explanations and Fig. 1 for location of the section).

5. Planktonic foraminiferal biostratigraphy: thin-section zonation The position of apertures and the presence of supplementary and accessory structures often used for generic distinctions are not identifiable in thin-section (Caron, 1985). Most of the diagnostic criteria, however, can be recognized in axial and subaxial sections. These criteria include the size and shape of the test (e.g., degree of convexity and symmetry of two sides; spiral and umbilical), the degree of peripheral angle (acute, right or obtuse), presence or absence of adumbilical ridges, thickness of the wall, size, shape, number and arrangements of chambers, and forms of ornamentations such as ridges, spines, position and number of peripheral thickenings or keels (Sliter, 1989). Some important characteristics such as position of apertures and the presence of supplementary and accessory structures cannot be observed in two dimentional, axial views of some species, they have similar features and therefore can not be separated from each other in thin-section. These species are grouped as four groups such as Globotruncanita conica (White) - Globotruncanita atlantica (Caron) group, Marginotruncana marginata (Reuss) - Globotruncana bulloides Vogler group, Marginotruncana pseudolinneiana Pessagno - Globotruncana linneiana (d’ Orbigny) group and Radotruncana subspinosa (Pessagno) - Radotruncana calcarata (Cushman) group. Fifty species belonging to twelve genera are identified from examination of thin-sections. The stratigraphic distribution of the taxa allows for the designation of six planktonic foraminiferal biozones. These are, in ascending order: Dicarinella concavata Interval Zone, Dicarinella asymetrica Range Zone, Radotruncana calcarata Range Zone, Globotruncana falsostuarti Partial Range Zone, Gansserina gansseri Interval Zone and Abathomphalus mayaroensis Concurrent Range Zone from the Coniacian-upper Maastrichtian

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succession of the Bey Dag˘ları Autochthon (Fig. 3). The first two biozones are observed in the hemipelagic limestones of the Bey Dag˘ları Formation, and following four biozones are identified from the pelagic limestones of the Akdag˘ Formation. Two of the zones are interval zones between the first occurrence (FO) and the last occurrence (LO) of the selected taxon (Dicarinella concavata Zone and Gansserina gansseri Zone). Two zones are range zones identified by the first and the last occurrences (range) of the nominal taxon (Dicarinella asymetrica Zone and Radotruncana calcarata Zone). Range zones used in this study are local range zones as the occurrences of the species are limited by disconformity surfaces (i.e., the last occurrence of D. asymetrica and the first occurrence of R. calcarata). One is a partial range zone identified by stratigraphical interval with Globotruncana falsostuarti Sigal between the LO of R. calcarata and the FO of Gansserina gansseri (Bolli) (Globotruncana falsostuarti Zone). Range of the nominal taxon (G. falsostuarti) usually exceeds the lower and upper limits of the biozone. The other zone is a concurrent range zone identified by the first occurrence of A. mayaroensis and the last occurrence Globotruncanita stuarti together with all the Cretaceous taxa (Abathomphalus mayaroensis Zone). Planktonic foraminifera observed in the hemipelagic limestones of the Bey Dag˘ları Formation (Dicarinella concavata Zone and Dicarinella asymetrica Zone) are generally scarce and of low diversity. By contrast, the planktonic foraminiferal assemblages from the Akdag˘ Formation (Radotruncana calcarata, Globotruncana falsostuarti, Gansserina gansseri Zone and Abathomphalus mayaroensis Zone) are diverse, large, thick-walled and are complex morphotypes (K-selection), which dominate in open oceans, mainly during the onset of highstands of sea level (Robaszynski and Caron, 1995). The six planktonic foraminiferal biozones identified in this study are briefly described from old to young (Fig. 3). Stratigraphic distributions of planktonic foraminifera are plotted in seventeen stratigraphic sections. 5.1. Dicarinella concavata Interval Zone (part) The Dicarinella concavata Interval Zone corresponding to the Coniacian-early Santonian age, has been described by many authors including Robaszynski et al. (1984), Caron (1985), Sliter (1989), Premoli Silva and Sliter (1994, 1999), Robaszynski and Caron ¨ zkan-Altıner and O ¨ zcan (1999), (1995), Robaszynski (1998), O Robaszynski et al. (2000) and Premoli Silva and Verga (2004) and the zone is defined as the interval from the first appearance datum (FAD) of Dicarinella concavata (Brotzen) to the FAD of Dicarinella asymetrica (Sigal) (interval zone). 5.1.1. Diagnosis In this study, occurrence of the Globotruncanids together with D. concavata in the transition zone between the neritic and hemipelagic limestones, is accepted as the beginning of the zone in local sense (Fig. 4). The lower limit of this zone may correspond to the lower part of the Coniacian, as the hemipelagic limestones grade into the Upper Turonian-Coniacian rudistid neritic limestones towards the base (Figs. 2, 4). The upper limit of the zone is marked by the FO of D. asymetrica (Fig. 4). 5.1.2. Remarks The planktonic foraminifera assemblage accompanying D. concavata is rather low in diversity and contains Marginotruncana coronata (Bolli), gr. M. pseudolinneiana - G. linneiana, gr. M. marginata - G. bulloides and Hedbergella sp.. Besides abundant calcisphaerulids, a few benthonic foraminifera (Rotalina? sp. and Goupillaudina sp.), and bivalves (inoceramid fragments) are also encountered. Stratigraphic distributions of planktonic foraminifera

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Fig. 8. Thin-section photomicrographs of the planktonic foraminifera observed in the Coniacian-Maastrichtian sequence of the Bey Dag˘ları Autochthon. 1, Abathomphalus mayaroensis Bolli, Loeblich & Tapan; axial section; sample 03-292; A. mayaroensis Zone, Ala Tepe section. 2, Abathomphalus mayaroensis Bolli, Loeblich & Tapan; axial section; sample 04-158; A. mayaroensis Zone, Yumruçalı Tepe section. 3, Abathomphalus mayaroensis Bolli, Loeblich & Tapan; subaxial (nearly axial) section; sample 97-110; A. mayaroensis Zone, Sarp Dere locality. 4, Contusotruncana contusa (Cushman); axial section; sample 01-106; G. gansseri Zone, Aladag˘ section. 5, Contusotruncana contusa (Cushman); axial section; sample 97-5; G. gansseri Zone, Sarp Dere-2 section. 6, Contusotruncana contusa (Cushman); subaxial section; sample 03-579; G. gansseri Zone, Enikliburnu section. 7, Contusotruncana fornicata (Plummer); axial section; sample 04-110; G. gansseri Zone, Bo¨lu¨kdag˘ Tepe section. 8, Contusotruncana fornicata (Plummer); axial section; sample 03-448; G. falsostuarti Zone, Kıraç Tepe section. 9, Contusotruncana fornicata (Plummer); axial section; sample 04-141; G. falsostuarti Zone, Yumruçalı Tepe section. 10, Contusotruncana patelliformis (Gandolfi); subaxial (nearly axial)section; sample 01-35; R. calcarata Zone, Aladag˘ section. 11, Contusotruncana patelliformis (Gandolfi); axial section; sample 03-434; G. falsostuarti Zone, Kıraç Tepe section. 12, Contusotruncana patelliformis (Gandolfi); axial section; sample 03-217; R. calcarata Zone., Ala Tepe section. 13, Contusotruncana plicata (White); subaxial section; sample 01-102; G. falsostuarti Zone, Aladag˘ section. 14, Contusotruncana cf. plicata (White); oblique axial section; sample 03-270B; G. gansseri Zone, Ala Tepe section. 15, Contusotruncana walfischensis (Todd); axial section; sample 03-285; G. gansseri Zone, Ala Tepe section. 16, Contusotruncana walfischensis (Todd); axial section; sample 01-137; G. gansseri Zone, Aladag˘ section. 17, Contusotruncana walfischensis (Todd); axial section; sample 01-93; G. falsostuarti Zone, Aladag˘ section. 18, Dicarinella canaliculata (Reuss); axial section; sample 98-93; D. asymetrica Zone, Çakmak Kertig˘i-2 section. 19, Dicarinella asymetrica (Sigal); axial section; sample 98-80; D. asymetrica Zone, Çakmak Kertig˘i-1 section. 20, Dicarinella asymetrica (Sigal); subaxial section; sample 03-461; D. asymetrica Zone, Bademag˘acı section. 21, Dicarinella concavata (Brotzen); subaxial section; sample 97-434; D. asymetrica Zone, Kargalıko¨y-2 section. 22, Dicarinella concavata (Brotzen); axial section; sample 98-86; D. asymetrica Zone, Çakmak Kertig˘i-1 section. 23, Gansserina gansseri (Bolli); subaxial section; sample 04-171; A. mayaroensis Zone, Yumruçalı Tepe section. 24, Gansserina gansseri (Bolli); axial section; sample 01-146A; A. mayaroensis Zone, Aladag˘ section. 25, Gansserina cf. gansseri; axial section; sample 01-90; G. falsostuarti Zone, Aladag˘ section. 26, Gansserina wiedenmayeri (Gandolfi); axial section; sample 98-238; G. gansseri Zone, Bozcalar Dere section. 27, Gansserina wiedenmayeri (Gandolfi); axial section; sample 01-143; A. mayaroensis Zone, Aladag˘ section. 28, Globotruncana aegyptiaca Nakkady; axial section; sample 01-423; G. gansseri Zone, Kocaaliler section. 29, Globotruncana aegyptiaca Nakkady; axial section; sample 04-103; G. gansseri Zone, Bo¨lu¨kdag˘ Tepe section. 30, Globotruncana aegyptiaca Nakkady; axial section; sample 01-410; G. gansseri Zone, Kocaaliler section. 31, Globotruncana cf. aegyptiaca Nakkady; axial section; sample 03-231; R. calcarata Zone, Ala Tepe section. 32, Globotruncana arca (Cushman); axial section; sample 01-48; R. calcarata Zone, Aladag˘ section. 33, Globotruncana cf. arca (Cushman); axial section; sample 03-583; G. gansseri Zone, Enikliburnu section. 34, Globotruncana bulloides Vogler; axial section; sample 04-194; R. calcarata Zone, Tekkeko¨y

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observed in Dicarinella concavata Zone are documented in Figs. 4 and 6. 5.1.3. Occurrence Dicarinella concavata Interval Zone is the oldest zone identified in the present study and corresponds to the lower part of the hemipelagic limestones of the Bey Dag˘ları Formation. The biozone was determined in two stratigraphic sections (Table 2). The maximum thickness of the biozone is 5.5 metres in the Kargalıko¨y section (Fig. 4) and it is more than 3 metres in the Aladag˘ section (Table 2; Fig. 6). The absence of the biozone in some sections is probably related to the diachronism of the onset of the hemipelagic deposition. 5.2. Dicarinella asymetrica Range Zone This biozone is characterized by the FAD and the last appearance datum (LAD) of the nominal taxon (as a total range zone) and corresponds to the middle-late Santonian (Robaszynski et al., 1984; Caron, 1985; Sliter, 1989; Robaszynski and Caron, 1995; Robaszynski, 1998; Premoli Silva and Sliter, 1994, 1999; Robaszynski et al., 2000; Premoli Silva and Verga, 2004) (Fig. 3). 5.2.1. Diagnosis In this study, the Dicarinella asymetrica Zone is identified by the FO and the LO of D. asymetrica (as a range zone) and corresponds to the middle-late Santonian. The biozone is cut by a disconformity surface throughout the autochthon. 5.2.2. Remarks The foraminiferal assemblage observed in the Dicarinella concavata Interval Zone is also encountered in the Dicarinella asymetrica Range Zone. Many forms including nominal taxon, D. asymetrica, Contusotruncana fornicata, Marginotruncana cf. schneegansi (Sigal), Marginotruncana cf. sigali (Reichel), Marginotruncana sinuosa, Marginotruncana tarfayaensis (Lehmann), Marginotruncana undulata (Lehmann) and Archaeoglobigerina sp./Rugoglobigerina sp. make their first occurrence in the Dicarinella asymetrica Zone (Figs. 7–9). Abundant calcisphaerulids, rare inoceram fragments and benthonic foraminifera (Rotaliidae, Rotalina? sp. and Goupillaudina sp.) accompany the foraminiferal assemblage. All the ConiacianSantonian planktonic foraminifera together with the nominal taxon D. asymetrica became extinct at the end of this biozone. Archaeoglobigerina sp./Rugoglobigerina sp.-like forms having globular chambers, biserial heterohelicids and C. fornicata cross the Santonian-Campanian boundary. Stratigraphic distributions of planktonic foraminifera observed in Dicarinella asymetrica Zone are documented in Figs. 4, 6, 7, 10, and 11. 5.2.3. Occurrence The Dicarinella asymetrica Zone is the last biozone of the hemipelagic limestones of the Bey Dag˘ları Formation and was identified

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from 5 stratigraphic sections (Table 2; Figs. 4, 6, 7, 10, 11). The maximum thickness of the biozone, more than 23 metres, is observed in the Kocabog˘az Dere section (Fig. 10). The thickness of the biozone varies between stratigraphic sections because of the diachronism and the post-Santonian erosion (Table 2; Figs. 4, 6, 7, 11, 12). The approximately 2-m-thick hemipelagic interval beneath the erosional surface in the Kıraç Tepe section is represented by the presence of an assemblage, which is similar to the assemblage of D. asymetrica Zone (Fig. 12). However, because there is a single occurrence of D. asymetrica in this section, D. asymetrica Zone is not proposed for this level. 5.3. Radotruncana calcarata Range Zone The Radotruncana calcarata Zone is defined as the interval from the FAD to the LAD of the nominal taxon (as a total range zone) and corresponds to the early late Campanian (Robaszynski, 1998; Premoli Silva and Sliter, 1994, 1999; Robaszynski et al., 2000; Premoli Silva and Verga, 2004) (Fig. 3). 5.3.1. Diagnosis In this study, Radotruncana calcarata Zone is identified as an interval from the FO to the LO of the nominal taxon (as a range zone) and corresponds to the early late Campanian. 5.3.2. Remarks In the Bey Dag˘ları successions, the beginning of the Campanian is marked by a distinct faunal turnover of the planktonic foraminifera. Many Coniacian-Santonian species became extinct at the boundary and many new single and double-keeled species appeared by the beginning of the Campanian. However some species such as C. fornicata cross the Santonian-Campanian boundary. The predominant species of the zone are Archaeoglobigerina blowi Pessagno, Archaeoglobigerina cretacea (d’Orbigny), C. fornicata, C. patelliformis, Contusotruncana plicata (White), Contusotruncana plummerae (Gandolfi), Contusotruncana walfischensis (Todd), Gansserina wiedenmayeri (Gandolfi), Globotruncana aegyptiaca Nakkady, Globotruncana arca (Cushman), Globotruncana arca-orientalis, G. bulloides, Globotruncana dupeublei Caron et al., Globotruncana esnehensis Nakkady, Globotruncana falsostuarti Sigal, Globotruncana (?) insignis Gandolfi, G. linneiana, Globotruncana mariei Banner and Blow, Globotruncana orientalis El Naggar, Globotruncana rosetta (Carsey), Globotruncana pseudoconica Solakius, Globotruncana ventricosa White, Globotruncanella havanensis (Voorwijk), gr. G. conica - G. atlantica, Globotruncanita elevata (Brotzen), Globotruncanita pettersi (Gandolfi), Globotruncanita stuarti (de Lapparent), Globotruncanita stuartiformis (Dalbiez), R. calcarata, gr. R. subspinosa - R. calcarata and intermediate forms between Archaeoglobigerina and Gansserina (Figs. 8, 9). All of the assemblage with the exception of C. fornicata, make their first occurrence in this zone. Besides these, some long-ranging groups such as Rugoglobigerina sp./Archaeoglobigerina sp. and biserial

section. 35, Globotruncana bulloides Vogler; axial section; sample 98-11; G. gansseri Zone, Kargalıko¨y section. 36, Globotruncana bulloides Vogler; axial section; sample 01-408; G. gansseri Zone, Kocaaliler section. 37, Globotruncana esnehensis Nakkady; axial section; sample 03-438; G. falsostuarti Zone, Kıraç Tepe section. 38, Globotruncana esnehensis Nakkady; axial section; sample 04-148; G. gansseri Zone, Yumruçalı Tepe section. 39, Globotruncana esnehensis Nakkady; subaxial (nearly axial) section; sample 01-413; G. gansseri Zone, Kocaaliler section. 40, Globotruncana arca (Cushman); axial section; sample 03-247; G. falsostuarti Zone, Ala Tepe section. 41, Globotruncana falsostuarti Sigal; axial section; sample 01-423; G. gansseri Zone, Kocaaliler section. 42, Globotruncana (?) insignis Gandolfi; axial section; sample 01-410; G. gansseri Zone, Kocaaliler section. 43, Globotruncana (?) insignis Gandolfi; axial section; sample 01-416; G. gansseri Zone, Kocaaliler section. 44, Globotruncana (?) insignis Gandolfi; axial section; sample 01-76; R. calcarata Zone, Aladag˘ section. 45, Globotruncana linneiana (d’Orbigny); axial section; sample 03-590; G. gansseri Zone, Enikliburnu section. 46, Globotruncana linneiana (d’Orbigny); axial section; sample 04-194; R. calcarata Zone, Tekkeko¨y section. 47, Globotruncana linneiana (d’Orbigny); axial section; sample 01-73; R. calcarata Zone, Aladag˘ section. 48, Globotruncana cf. mariei Banner & Blow; subaxial section; sample 03-441; G. falsostuarti Zone, Kıraç Tepe section. 49, Globotruncana orientalis El Naggar; axial section; sample 01-421; G. gansseri Zone, Kocaaliler section. 50, Intermediate forms between Globotruncana arca (Cushman) and Globotruncana orientalis El Naggar; axial section; sample 97-637; G. gansseri Zone, Canavar Bog˘azı section. 51, Globotruncana orientalis El Naggar; axial section; sample 03-434; G. falsostuarti Zone, Kıraç Tepe section. 52, Globotruncana rosetta (Carsey); axial section; sample 01-60; R. calcarata Zone, Aladag˘ section.

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Fig. 9. Thin-section photomicrographs of the planktonic foraminifera observed in the Coniacian-Maastrichtian sequence of the Bey Dag˘ları Autochthon.1, Globotruncana ventricosa White; axial section; sample 01-84; R. calcarata Zone, Aladag˘ section. 2, Globotruncana ventricosa White; axial section; sample 04-113; G. gansseri Zone, Bo¨lu¨kdag˘ Tepe section. 3, Globotruncana ventricosa White; subaxial (nearly axial) section; sample 98-187; A. mayaroensis Zone, Savran Ekinlig˘i section. 4, Globotruncanita angulata (Tilev); axial section; sample 04-170; A. mayaroensis Zone, Yumruçalı Tepe section. 5, Globotruncanita angulata (Tilev); axial section; sample 97-638; G. gansseri Zone, Canavar Bog˘azı section. 6, Globotruncanita angulata (Tilev); axial section; sample 01-97; G. falsostuarti Zone, Aladag˘ section. 7, gr. Globotruncanita conica (White) - Globotruncanita atlantica (Caron); axial section; sample 03-211; R. calcarata Zone, Ala Tepe section. 8, cf. gr. Globotruncanita conica (White) - Globotruncanita atlantica (Caron); oblique axial section; sample 98-236; G. gansseri Zone, Bozcalar Dere section. 9, gr. Globotruncanita conica (White) - Globotruncanita atlantica (Caron); axial section; sample 98-233; G. gansseri Zone, Bozcalar Dere section. 10, Globotruncanita elevata (Brotzen); axial section; sample 03-511; R. calcarata Zone, Go¨zet Tas¸ı section. 11, Globotruncanita elevata (Brotzen); axial section; sample 98-111a; R. calcarata Zone, Çakmak Kertig˘i-2 section. 12, Globotruncanita elevata (Brotzen); subaxial (nearly axial) section; sample 98-117; R. calcarata Zone, Çakmak Kertig˘i-2 section. 13, Globotruncanita pettersi (Gandolfi); axial section; sample 01-69; R. calcarata Zone, Aladag˘ section. 14, Globotruncanita pettersi (Gandolfi); axial section; sample 01-426; G. gansseri Zone, Kocaaliler section. 15, Globotruncanita pettersi (Gandolfi); axial section; sample 01-57; R. calcarata Zone, Aladag˘ section. 16, Globotruncanita stuarti (de Lapparent); axial section; sample 98241; A. mayaroensis Zone, Bozcalar Dere section. 17, Globotruncanita stuarti (de Lapparent); slightly oblique axial section; sample 03-444; G. falsostuarti Zone, Kıraç Tepe section. 18, Globotruncanita stuarti (de Lapparent); axial section; sample 97-4; G. gansseri Zone, Sarp Dere-2 section. 19, Globotruncanita stuartiformis (Dalbiez); subaxial (nearly axial) section; sample 03-211; R. calcarata Zone, Ala Tepe section. 20, Globotruncanita stuartiformis (Dalbiez); axial section; sample 04-156; G. gansseri Zone, Yumruçalı Tepe section. 21, Globotruncanita stuartiformis (Dalbiez); axial section; sample 04-113; G. gansseri Zone, Bo¨lu¨kdag˘ Tepe section. 22, Radotruncana calcarata (Cushman); axial section; sample 01-75; R.

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heterohelicids also cross the Santonian-Campanian boundary and therefore accompany the late Campanian assemblage. The last occurrence of the nominal taxon R. calcarata marks the upper limit of the Radotruncana calcarata Range Zone. Stratigraphic distributions of planktonic foraminifera observed in Radotruncana calcarata Zone are documented in Figs. 6, 11, 13, and 14. The extinction of R. calcarata had long been used to draw the Campanian-Maastrichtian boundary (Robaszynski et al., 1984; Caron, 1985; Almogi-Labin et al., 1986; Sliter, 1989). Robaszynski and Caron (1995), however, noted that an accurate calibration had not been published. They also stated that R. calcarata disappeared before the base of the Nostoceras (Nostoceras) hyatti Zone (ammonite zone dating the uppermost Campanian) and thus the Radotruncana calcarata Zone might be a little older. As noted by Premoli Silva and Sliter (1994) the Campanian-Maastrichtian boundary was equated to the chron 32N/chron 31R boundary and shifted to 71.3 Ma by Lommerzheim and Hambach (1992) and Gradstein et al. (1994). Thus the Radotruncana calcarata Zone no longer corresponds to the uppermost part of the Campanian, moreover Globotruncanella havanensis and Globotruncana aegyptiaca zones (or corresponding Globotruncana falsostuarti Zone) and even the lower part of the Gansserina gansseri Zone are all of late Campanian age. This placement was accepted by the following biostratigraphic studies (Premoli Silva and Sliter, 1994, 1999; Robaszynski et al., 2000; Premoli Silva and Verga, 2004). This is the first zone of the Campanian in the study area where the lower and middle Campanian were not deposited or eroded. Globotruncanita elevata and Globotruncana ventricosa zones are absent in all measured stratigraphic sections except for the Tekkeko¨y section in the southern part of the autochthon (Fig. 13), where the level lacking any index taxa but lying below the Radotruncana calcarata Zone may belong to the Globotruncana ventricosa Zone. The other alternative is that this level also belongs to the Radotruncana calcarata Zone, but the nominal species could not be observed because of the rareness of the species or difficulties in determining the species in thin-section. The Aladag˘ and Ala Tepe sections are important as they are rich in well-preserved forms of R. calcarata. The lowermost parts of the two stratigraphic sections yield numerous identical sections showing tubulospines. The floods of the species were encountered in some levels of the two sections (i.e., Aladag˘ section, Fig. 6, samples 01-83, 01-84, 01-86; Ala Tepe section, Fig. 14, samples 03227, 03-231). See Fig. 8 for identical photomicrographs of the species.

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5.3.3. Occurrence The Radotruncana calcarata Range Zone corresponds to the base of the Akdag˘ Formation and was identified in 4 stratigraphic sections (Table 2; Figs. 6, 11, 13, 14). The Çakmak Kertig˘i section in the Korkuteli area presents the thickest interval belonging to the biozone, 40-m-thick (See Section-2 in Sarı, 2006a). However this stratigraphic section does not present identical sections of the nominal species. As the onset of the pelagic limestones is diachronous, the thickness of the biozone ranges from 18 metres in the Aladag˘ section (Fig. 6) to 27 metres in the Ala Tepe section (Fig. 14). The biozone is absent in some stratigraphic sections (Table 2).

5.4. Globotruncana falsostuarti Partial Range Zone The Globotruncana falsostuarti Partial Range Zone represents the stratigraphical interval with G. falsostuarti between the LAD of R. calcarata and the FAD of G. gansseri and corresponds to the middle late Campanian (Robaszynski, 1998). Robaszynski et al. (1984, 2000), Chacon et al. (2004) and Sarı (2006a) used this zone, whereas Caron (1985), Sliter (1989), Robaszynski and Caron (1995), Robaszynski (1998), Premoli Silva and Sliter (1994, 1999) and Premoli Silva and Verga (2004) used Globotruncanella havanensis and Globotruncana aegyptiaca zones instead. 5.4.1. Diagnosis The Globotruncana falsostuarti Zone is identified as an interval with G. falsostuarti from the LO of R. calcarata to the FO of G. gansseri (as a partial range zone) and corresponds to the middle late Campanian. 5.4.2. Remarks Although G. aegyptiaca is widely recorded from the Maastrichtian deposits, Almogi-Labin et al. (1986) reported that the species occurred in the uppermost Campanian of Israel (associated with R. calcarata and important microfossils). Recently Robaszynski et al. (2000) and Chacon et al. (2004) documented the co-occurrence of G. aegyptiaca and R. calcarata in central Tunisia and SE Spain respectively. The present study supports the findings of these researchers as the co-occurrence of the two species is also the case for the Bey Dag˘ları Autochthon. The Radotruncana calcarata Zone is represented by numerous identical sections (showing tubulospines) in two stratigraphic sections in the northern part of the autochthon (i.e., the Aladag˘ and Ala Tepe sections; Figs. 6, 14). Some

calcarata Zone, Aladag˘ section. 23, Radotruncana calcarata (Cushman); axial section; sample 01-83; R. calcarata Zone, Aladag˘ section. 24, Radotruncana calcarata (Cushman); subaxial section; sample 03-235; R. calcarata Zone, Ala Tepe section. 25, Radotruncana calcarata (Cushman); axial section; sample 04-194; R. calcarata Zone, Tekkeko¨y section. 26, gr. Radotruncana subspinosa (Pessagno) - Radotruncana calcarata (Cushman); slightly oblique axial section; sample 98-224; G. gansseri Zone, Bozcalar Dere section. 27, gr. Radotruncana subspinosa (Pessagno) - Radotruncana calcarata (Cushman); subaxial (nearly axial) section; sample 01-67; R. calcarata Zone, Aladag˘ section. 28, gr. Radotruncana subspinosa (Pessagno) - Radotruncana calcarata (Cushman); slightly oblique axial section; sample 01-412; G. gansseri Zone, Kocaaliler section. 29, Marginotruncana coronata (Bolli); axial section; sample 98-164; D. concavata Zone, Fedil Dere section. 30, Marginotruncana coronata (Bolli); axial section; sample 98-97; D. asymetrica Zone, Çakmak Kertig˘i-2 section. 31, cf. gr. Marginotruncana marginata (Reuss) - Globotruncana bulloides Vogler; axial section; sample 97-434; D. asymetrica Zone, Kargalıko¨y section. 32, gr. Marginotruncana marginata (Reuss) - Globotruncana bulloides Vogler; subaxial section; sample 03-461; D. asymetrica Zone, Kıraç Tepe section. 33, Marginotruncana paraconcavata Porthault; axial section; sample 03-195; D. concavata Zone or D. asymetrica Zone, Ala Tepe section. 34, gr. Marginotruncana pseudolinneiana Pessagno - Globotruncana linneiana (d’Orbigny); axial section; sample 98-83; D. asymetrica Zone, Çakmak Kertig˘i-1 section. 35, gr. Marginotruncana pseudolinneiana Pessagno - Globotruncana linneiana (d’Orbigny); axial section; sample 98-80; D. asymetrica Zone, Çakmak Kertig˘i-1 section. 36, Marginotruncana cf. schneegansi (Sigal); subaxial (nearly axial) section; sample 03-641; from the hemipelagic infillings of the neptunian dykes within the neritic limestones of the Karain section. 37, Marginotruncana cf. schneegansi (Sigal); subaxial (nearly axial) section; sample 03-640; from the hemipelagic infillings of the neptunian dykes within the neritic limestones of the Karain section. 38, Marginotruncana sigali (Reichel); axial section; sample 03-461; D. asymetrica Zone, Kıraç Tepe section. 39, Marginotruncana sinuosa Porthault; subaxial section; sample 98-86; D. asymetrica Zone, Çakmak Kertig˘i-1 section. 40, Marginotruncana cf. undulata (Lehmann); axial section; sample 03-137; D. asymetrica Zone, Kocabog˘az Dere section. 41, Archaeoglobigerina cf. blowi Pessagno; axial section; sample 98-45; G. gansseri Zone, Çakmak Kertig˘i-2 section. 42, Archaeoglobigerina cf. blowi Pessagno; axial section; sample 98-140; R. calcarata Zone, Çakmak Kertig˘i-2 section. 43, Archaeoglobigerina cf. blowi Pessagno; axial section; sample 03-284; A. mayaroensis Zone, Ala Tepe section. 44, Rugoglobigerina milamensis Smith; axial section; sample 04-110; G. gansseri Zone, Bo¨lu¨kdag˘ Tepe section. 45, Rugoglobigerina pennyi Bro¨nnimann; axial section; sample 04-170; A. mayaroensis Zone, Yumruçalı Tepe section. 46, Globotruncanella havanensis (Voorwijk); axial section; sample 04-103; G. gansseri Zone, Bo¨lu¨kdag˘ Tepe section. 47, Planoglobulina sp.; sample 03-277; G. gansseri Zone, Ala Tepe section. 48, Biserial heterohelicid; sample 97-434; D. asymetrica Zone, Kargalıko¨y section. 49, Rotaliidae (Rotalina? sp.); sample 04-208;?G. ventricosa Zone, Tekkeko¨y section. 50, Goupillaudina sp.; sample 98-24; D. asymetrica Zone, Kargalıko¨y section. See Sarı (2006a) for the Çakmak Kertig˘i-2 and Sarp Dere-2 stratigraphic sections (Section-2 and Section-3, respectively) and Sarı (2006b) for the Çakmak Kertig˘i-1 and Karain stratigraphic sections.

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Fig. 10. Stratigraphic distribution of the planktonic foraminifera in the Kocabog˘az Dere section. (See Fig. 5 for explanations and Fig. 1 for location of the section).

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Fig. 11. Stratigraphic distribution of the planktonic foraminifera in the Go¨zet Tas¸ı section. (See Fig. 5 for explanations and Fig. 1 for location of the section).

sections of G. aegyptiaca were also identified within the Radotruncana calcarata Zone (Figs. 6, 8, 14). The occurrence of G. aegyptiaca within the Radotruncana calcarata Zone shows that Globotruncanella havanensis and Globotruncana aegyptiaca zones can not be used for the middle part of the late Campanian in the Bey Dag˘ları Autochthon. Therefore Globotruncana falsostuarti Partial Range Zone is used in this study. The planktonic foraminiferal assemblage of the biozone is similar to that of the Radotruncana calcarata Zone except for R. calcarata, which became extinct at the end of the Radotruncana calcarata Zone. G. elevata is represented by a few specimens at the lower part of the biozone and became extinct within this biozone (i.e., Kıraç Tepe section, Fig. 12). Globotruncanita angulata (Tilev) first appears in the middle of the biozone in the Aladag˘ section and is very rare throughout the biozone (Fig. 6). Stratigraphic distributions of planktonic foraminifera observed in Globotruncana falsostuarti Zone are documented in Figs. 3, 4, 6, 11, 12, and 14–16. 5.4.3. Occurrence Globotruncana falsostuarti Zone corresponds to the middle part of the Akdag˘ Formation and was identified in 8 stratigraphic sections (Table 2; Figs. 4, 6, 11, 13–16). The thickness of the biozone

is maximum in the Ala Tepe section, 21 metres (Fig. 14). It is 2.5 metres thick in the Kargalıko¨y section (Fig. 4). 5.5. Gansserina gansseri Interval Zone The Gansserina gansseri Interval Zone has been defined by many authors (Robaszynski et al., 1984; Caron, 1985; Sliter, 1989; Premoli Silva and Sliter, 1994, 1999; Robaszynski and Caron, 1995; Robaszynski, 1998; Robaszynski et al., 2000; Premoli Silva and Verga, 2004) as an interval between the FAD of the nominal species and the FAD of Abathomphalus mayaroensis Bolli, Loeblich and Tapan. 5.5.1. Diagnosis The Gansserina gansseri Zone is identified as an interval from the FO of G. gansseri to the FO of A. mayaroensis (as an interval zone) and corresponds to the latest Campanian-early Maastrichtian. 5.5.2. Remarks The planktonic foraminiferal assemblage is similar with the Globotruncana falsostuarti Zone. All the species encountered within the Globotruncana falsostuarti Partial Range Zone cross the lower boundary of the Gansserina gansseri Zone. The most remarkable

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Fig. 12. Stratigraphic distribution of the planktonic foraminifera in the Kıraç Tepe section. (See Fig. 5 for explanations and Fig. 1 for location of the section).

bioevent of the biozone is the abundance of the nominal taxon in some levels of some sections (i.e., Yumruçalı Tepe, Bo¨lu¨kdag˘ Tepe, Canavar Bog˘azı and Savran Ekinlig˘i sections; Fig. 15, samples 04-165–04-171; Fig. 16, sample 04-102; Fig. 17, samples 97-638, 97-639; Fig. 18, samples 98-184–98-186). Besides this taxon, G. angulata and G. pettersi occur abundantly. Contusotruncana contusa (Cushman) and multiserial heterohelicids (Planoglobulina sp.) first appear in this zone. Biserial heterohelicids dominate in some levels of some sections (i.e., Canavar Bog˘azı section; Fig. 17, samples 97-636). Stratigraphic distributions of planktonic foraminifera

observed in Gansserina gansseri Zone are documented in Figs. 4, 6, 10, and 13–22. Some forms in the Radotruncana calcarata Zone and Globotruncana falsostuarti Zone share similar characteristics with Gansserina. They have more or less flat or slightly convex spiral side and strongly convex umbilical side with hemispherical chambers. They do not have a clear single keel, hovewer, especially on the early chambers of the last whorl (i.e., Aladag˘ and Ala Tepe sections, Figs. 6, 14). These are probably the transitional forms between Gansserina and its ancestor Archaeoglobigerina.

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Fig. 13. Stratigraphic distribution of the planktonic foraminifera in the Tekkeko¨y section. (See Fig. 5 for explanations and Fig. 1 for location of the section).

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Fig. 14. Stratigraphic distribution of the planktonic foraminifera in the Ala Tepe section. (See Fig. 5 for explanations and Fig. 1 for location of the section).

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Fig. 14. (continued).

5.5.3. Occurrence The Gansserina gansseri Interval Zone was identified in 14 stratigraphic sections (Table 2; Figs. 4, 6, 10, 13–23). The biozone is thickest in the Bo¨lu¨kdag˘ Tepe section reaching more than 48 metres (Fig. 16). Thickness of the biozone is only 5.5 metres in the Kargalıko¨y section (Fig. 4). 5.6. Abathomphalus mayaroensis Concurrent Range Zone (part) The Abathomphalus mayaroensis Zone is the last biozone of the Late Cretaceous. The biozone has been widely defined by many researchers as Abathomphalus mayaroensis Zone between the FAD and the LAD of the nominal taxon (as a total range zone) to determine the uppermost part of the Maastrichtian (Robaszynski et al., 1984; Caron, 1985; Sliter, 1989; Premoli Silva and Sliter, 1994, 1999; Robaszynski and Caron, 1995; Robaszynski, 1998; Robaszynski et al., 2000; Premoli Silva and Verga, 2004; Chacon et al., 2004). 5.6.1. Diagnosis The scarcity of the nominal taxon in this study, requires that the interval be identified as a concurrent range zone. The lower boundary of the Abathomphalus mayaroensis Zone is represented by the FO of the nominal taxon. The upper limit is characterized by the LO of G. stuarti together with all the Late Cretaceous

planktonic foraminifera near the middle of the late Maastrichtian (Fig. 3). 5.6.2. Remarks The foraminiferal assemblage of the biozone is similar to the assemblage observed in the Gansserina gansseri Zone with the exception of C. plummerae, which disappears towards the top of the Gansserina gansseri Zone. The occurrence of C. fornicata, C. patelliformis, C. plicata, G. wiedenmayeri, G. bulloides, G. (?) insignis, G. linneiana, G. mariei, G. orientalis, G. ventricosa gr. R. subspinosa - R. calcarata within the Abathomphalus mayaroensis Zone indicates that the latest Maastrichtian is absent in the Bey Dag˘ları Autochthon probably because of the truncation of the pelagic sequence. Stratigraphic distributions of planktonic foraminifera observed in Abathomphalus mayaroensis Zone are documented in Figs. 6, 14, 15, and 23. The lower-middle Paleocene is also absent in all measured stratigraphic sections except for the Çamlıdere area, from where we lack enough biostratigraphic data concerning the CretaceousPaleogene boundary. Poisson (1977) suggested, however, that latest Maastrichtian and Danian exist in some parts of the Bey Dag˘ları Autochthon (e.g., Bozcalar Dere and Çamlıdere areas). 5.6.3. Occurrence A. mayaroensis is quite rare in the Bey Dag˘ları Autochthon. Although numerous closely-spaced samples were collected from

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Fig. 15. Stratigraphic distribution of the planktonic foraminifera in the Yumruçalı Tepe section. (See Fig. 5 for explanations and Fig. 1 for location of the section).

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Fig. 16. Stratigraphic distribution of the planktonic foraminifera in the Bo¨lu¨kdag˘ Tepe section. (See Fig. 5 for explanations and Fig. 1 for location of the section).

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Fig. 17. Stratigraphic distribution of the planktonic foraminifera in the Canavar Bog˘azı section. (See Fig. 5 for explanations and Fig. 1 for location of the section).

the pelagic limestones of the Akdag˘ Formation, only 10 specimens of A. mayaroensis were determined from the uppermost parts of the 7 stratigraphic sections (Table 2; Figs. 6, 14, 15, 18–20, 23). The thickness of the biozone is generally reduced and varies from 0.5 metre to 6.5 metres in 5 stratigraphic sections. The maximum thickness was measured from the Yumruçalı Tepe section and is about 32 metres (Fig. 15). 6. Hiatuses in the pelagic sequence and Late Cretaceous evolution of the BDCP: evidences from the planktonic foraminiferal biostratigraphy The Bey Dag˘ları carbonate platform is reconstructed as an isolated carbonate platform without any terrestrial input. Foraminifera and rudist biostratigraphy indicate that the platform conditions persisted from middle Cenomanian to the Coniacian in the

northern part of the autochthon (Sarı et al., 2004, 2005, 2009; Sarı, ¨ zer, 2009). Diachronous subsidence of the plat2006b; Sarı and O form after the late Turonian (Coniacian and Santonian) resulted in a hemipelagic environment that would persist until the end of the Santonian. Two planktonic foraminiferal biozones, Dicarinella concavata Zone and Dicarinella asymetrica Zone, suggest a ConiacianSantonian age for the massive hemipelagic limestones, which are overlain by the upper Campanian - upper Maastrichtian, thinbedded pelagic limestones of the Akdag˘ Formation along a prominent discontinuity surface. The surface shows the characteristic features of a hardground such as Fe-Mn oxidation crust, silicification and bioturbation, which is indicative of a period of low rate of sedimentation or non-deposition within the marine environment due to relative starvation caused by deepening (Schlager, 1981; Rosales et al., 1994). This drowning event corresponds to the ‘starved drowning’ of Bosellini (1989). The nondeposition in basinal

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Fig. 18. Stratigraphic distribution of the planktonic foraminifera in the Savran Ekinlig˘i section. (See Fig. 5 for explanations and Fig. 1 for location of the section).

condition occurred during the early-middle Campanian as evidenced by the planktonic foraminiferal biozones. Radotruncana calcarata Zone is the oldest zone determined in the pelagic limestones and corresponds to the lowermost part of the upper Campanian. The early-middle Campanian was also the time of submarine erosion, during which hemipelagic limestones and the upper part of the neritic limestones were eroded (Fig. 24). Diachronous drowning of the northern part of the platform after the Santonian (beginning within the late Campanian) resulted in a pelagic environment, which is supported by complex morphotypes (K-selection) of planktonic foraminifera dominant in open oceans (Robaszynski and Caron, 1995). Planktonic foraminifera observed in the pelagic limestones of the Akdag˘ Formation indicate four biozones which suggest a late Campanian-late Maastrichtian age. Occurrence of pebble and sand size intraclasts of neritic, hemipelagic and pelagic limestones within the late Campanian-late Maastrichtian pelagic limestones indicate that different stratigraphic levels of the platform succession were eroded during the deposition of the pelagic limestones (Fig. 24). The examination of the planktonic foraminifera reveals two main sedimentary gaps within the Upper Cretaceous pelagic sequence. Lower to middle Campanian and uppermost Maastrichtian-middle Paleocene are absent in all measured stratigraphic sections with the exception of the Çamlıdere area, from where we lack sufficient data (Fig. 24). Blocks, pebbles and sand-size particles of the different stratigraphic levels of the Upper Cretaceous sequence are observed at the base of the Paleogene in some sections (Fig. 24). The Paleogene disconformably overlies the pelagic limestones, hemipelagic limestones or neritic limestones (Fig. 24). It is likely that the drowning events after the Turonian were linked to the regional crustal extention, which may have been the driving force of subsidence of the carbonate platforms after Cenomanian times as a result of the extensional collapse caused by ‘roll-back’ of down going, north dipping Late Triassic-Jurassic oceanic crust located in the south of the platform (Poisson, 1984;

Robertson, 1993; Robertson et al., 2003). An extensional normal faulting could be the mechanism responsible for the platform drowning, evidenced by the presence of local breccia levels within the deeper water carbonates (Robertson, 1998; Poisson et al., 2003). The Coniacian is also considered the peak of tectono-eustatic transgressions initiated during the late Turonian in Northern Africa (Reyment and Dingle, 1987). The change of depositional environment from the Santonian to the late Campanian may have been related to an important tectonic phase, perhaps associated with the Campanian-Maastrichtian highstand of sea-level (Haq et al., 1987). In the Apulian domain and neighbouring areas, CampanianMaastrichtian interval was the time of maximum extent of pelagic facies on the flooded carbonate platforms (e.g., Friuli, Karst, Parnassos and Bey Dag˘ları) (Poisson, 1977) related to extensional tectonic movements on faulted platform margins (Philip et al., 1993). During the Campanian-Maastrichtian period, the converging Mediterranean was a narrowing space controlled by subduction and collision (Camoin et al., 1993). It was also the time of initial records of emplacement-related sedimentation and tectonics. The lower-middle Campanian and uppermost Maastrichtianmiddle Paleocene hiatuses in the pelagic sequence can readily be ascribed to the regional tectonics because the easternmost Mediterranean area was subjected to the important tectonic events mentioned previously during the Late Cretaceous. The second hiatus may have been related to the compressional tectonics as the Maastrichtian was the closure time for the Arabo-African and Eurasiatic plates and the initial stages of emplacement time of the Antalya nappes in this particularly critical area of Tethys. The Pamphylian basin in the Isparta Angle closed, and the preserved Antalya allochthon was initially emplaced onto the adjacent peripheral carbonate platform units (e.g., Tekedag˘) in Maastrichtian time, but was not finally emplaced over the main carbonate platforms (e.g., Bey Dag˘ları) until the Paleocene (Robertson et al., 2003; Poisson et al., 2003). The nappes did not reach the central part of the Bey Dag˘ları carbonate platform (Poisson et al., 2003). Eustatic

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Fig. 19. Stratigraphic distribution of the planktonic foraminifera in the Demirci Dere section. (See Fig. 5 for explanations and Fig. 1 for location of the section).

sea level changes may have had a secondary effect on the Upper Cretaceous carbonate successions of the Bey Dag˘ları Autochthon. 7. Conclusions Detailed investigations of the planktonic foraminiferal biostratigraphy within the seventeen stratigraphic sections measured from the Upper Cretaceous hemipelagic and pelagic sequences of the northern part of the Bey Dag˘ları Autochthon (western Taurides) yields following conclusions: (1) The planktonic foraminiferal species identified enable determination of six biozones, from old to young, Dicarinella concavata Interval Zone, Dicarinella asymetrica Range Zone,

Radotruncana calcarata Range Zone, Globotruncana falsostuarti Partial Range Zone, Gansserina gansseri Interval Zone and Abathomphalus mayaroensis Concurrent Range Zone. (2) Dicarinella concavata Zone and Dicarinella asymetrica Zone are identified from the Coniacian-Santonian massive hemipelagic limestones of the Bey Dag˘ları Formation, which are represented by rare planktonic foraminifera and abundant calcisphaerulids content. (3) The last four biozones are identified from the cherty pelagic limestones of the Akdag˘ Formation and indicate a late Campanian-late Maastrichtian time interval. The planktonic foraminifera observed in the last four biozones are diverse, complex morphotypes, which dominate in open oceans, mainly during onset of highstands of sea level.

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Fig. 20. Stratigraphic distribution of the planktonic foraminifera in the Kocaaliler section. (See Fig. 5 for explanations and Fig. 1 for location of the section).

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Fig. 21. Stratigraphic distribution of the planktonic foraminifera in the Enikliburnu section. (See Fig. 5 for explanations and Fig. 1 for location of the section).

(4) The planktonic foraminiferal assemblages of the Abathomphalus mayaroensis Zone show that the latest Maastrichtian is absent throughout the northern part of the autochthon. (5) The examination of the planktonic foraminifera indicates two main sedimentary gaps within the Upper Cretaceous pelagic sequence. Lower to middle Campanian and uppermost Maastrichtian-middle Paleocene are absent in all measured stratigraphic sections except for the Çamlıdere area, from where we lack sufficient data. Hiatus durations differ between most stratigraphic sections, as a result of the diachronistic onset of the hemipelagic and pelagic deposition and the post-Santonian and post-Maastrichtian erosional phases. (6) The incipient drowning of the northern part of the platform after the late Turonian as a result of inferred extensional normal faulting, resulted in a hemipelagic environment that would persist until the end of the Santonian. The platform was drowned after the Santonian and the pelagic sediments were deposited on the northern part of the platform. It is plausible to

postulate that the drowning events were linked to the regional crustal extension, a possible driving force for the subsidence of the carbonate platforms after Cenomanian times resulting from the extensional collapse caused by ‘roll-back’ of down going, north-dipping Late Triassic-Jurassic oceanic crust located in the south of the platform. (7) The lower-middle Campanian and uppermost Maastrichtianmiddle Paleocene hiatuses in the pelagic sequence are ascribed to regional tectonics as the easternmost Mediterranean area was subjected to the important tectonic events during the Late Cretaceous. The second hiatus may have been related to compressional tectonics as the Maastrichtian was the closure time for the Arabo-African and Eurasiatic plates and the initial stages of emplacement of the Antalya complex in this particularly critical area of Tethys. Eustatic sea level changes may have had a secondary effect on the Upper Cretaceous carbonate succession of the Bey Dag˘ları Autochthon.

Fig. 22. Stratigraphic distribution of the planktonic foraminifera in the Yag˘ca section. (See Fig. 5 for explanations and Fig. 1 for location of the section).

Fig. 23. Stratigraphic distribution of the planktonic foraminifera in the Bozcalar Dere section. (See Fig. 5 for explanations and Fig. 1 for location of the section).

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Fig. 24. Chart showing the correlation of the Upper Cretaceous stratigraphic sections measured from the nerthern part of the Bey Dag˘ları Autochthon. The numbers in circles in the hemipelagic and pelagic limestones stand for the thickness of the planktonic foraminiferal zones. Note the two hiatuses corresponding to the early-middle Campanian and latest Maastrichtian-middle Paleocene. Hiatus durations differ between most stratigraphic sections, as a result of the diachronistic onset of the hemipelagic and pelagic deposition and the post-Santonian and post-Maastrichtian erosional phases (See Fig. 1 for location of the sections).

Acknowledgements This work was financially supported by a TUBITAK project, no. 102Y062, which is gratefully acknowledged. I appreciate guidance ¨ zer who was supervisor of my PhD studies. I would like to of Sacit O thank Guy Tronchetti for verifying the planktonic foraminifera

determinations. I also would like to thank three anonymous reviewers for their constructive and helpful reviews. Demir Altıner ¨ zkan-Altıner are thanked for invaluable discussions on and Sevinç O planktonic foraminiferal biozonation. I also appreciate the helps of _ ¨ zkar-O ¨ ngen who identified the early Paleogene planktonic Izver O foraminifera. A special thank must go to Andre Poisson who guided

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me for the important section locations and critical outcrops during one-day excursion throughout the northern part of the autochthon. ¨ zer, Akif Sarı, U ¨ mit Kasım, Evren Yu¨cel and The help of Sacit O Go¨rkem Oskay who took part in the field works are also appreciated. I would like to thank Ann M. Molineux and William C. Ward for their grammatical suggestions on the latest version of the manuscript. Bayram Karabacak and Enver Yıldız, who are the former staff members of the thin-section laboratory, are thanked for preparation of numerous thin-sections. References Almogi-Labin, A., Reiss, Z., Caron, M., 1986. Senonian Globotruncanidae from Israel. Eclogae Geologicae Helvetiae 79, 849–895. Altınlı, E., 1944. Etude stratigraphique de la re´gion d’ Antalya. Revue de la Faculte´ des Sciences de l’ Universite´ d’ Istanbul, B 9, 227–238. Altınlı, E., 1945. Etude tectonique de la re´gion d’ Antalya. Revue de la Faculte´ des Sciences de l’ Universite´ d’ Istanbul B 10, 60–67. 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