Lithostratigraphy and planktonic foraminifera of the uppermost Cretaceous – Upper Palaeocene strata of the Tavas nappe of the Lycian nappes ( SW Turkey )

The Lycian nappes lying on top of the para-autochthonous metamorphosed Menderes and unmetamorphosed Bey Dağları successions in SW Anatolia belong to the Tauride segment of the Anatolide-Tauride Block. The Tavas nappe is one of several nappe slices of the Lycian nappes and forms structurally the lowermost tectono-stratigraphic unit. The upper part of the Tavas nappe succession is represented by planktonic foraminifera-bearing uppermost Cretaceous cherty micritic limestones and calciturbidites of the Babadağ Formation and Lower Palaeogene micritic limestones and calciclastic rocks of the Faralya Formation in the study area. Lithostratigraphic characteristics and planktonic foraminiferal assemblages of the two formations in the Bozburun hill locality (S of Köyceğiz) are documented for the first time in three stratigraphic sections in this study. The uppermost part of the Babadağ Formation mainly comprises of alternating calciclastic and micritic limestones, which include diverse planktonic foraminiferal assemblages of mainly keeled morphotypes. The presence of Racemiguembelina fructicosa and Abathomphalus mayaroensis within the assemblages indicates a late Maastrichtian age for the uppermost part of the succession. Two sections of the overlying Faralya Formation comprise mainly planktonic foraminifera-bearing laminated micritic limestones, brecciated limestones and mudstones. Planktonic foraminiferal assemblages of the laminated micritic limestones are dominated by keeled Late Palaeocene morphotypes. The occurrence of Morozovella acuta and Globanomalina planoconica at the base of two sections suggests a Thanetian age for the deposits. The boundary between the Babadağ and Faralya formations is characterized by a stratigraphic gap ranging from the latest Maastrichtian to the earliest Selandian. The gap was linked with the first of the three main events, when ophiolite obduction and incorporation of the Köyceğiz Thrust Sheet into the Lycian allochthon occured. Cretaceous limestone clasts and foraminifers within the Thanetian calciclastic rocks of the Faralya Formation could be clues to that exposure and erosion. Article history: Manuscript received June 06, 2017 Revised manuscript accepted October 04, 2017 Available online October 31, 2017

Although the uppermost Cretaceous-Lower Palaeogene successions mentioned above are important as they yield valuable palaeontological data, they have been subject to a few studies, which provide some lists of foraminifera but without illustrations (e.g.ŞENEL, 1991).The aim of this study is to document the lithostratigraphic characteristics and planktonic foraminiferal assemblages of the uppermost levels of the Babadağ Fm. and the lowermost part of the Faralya Fm. in and around Bozburun hill (south of Köyceğiz town) by the means of three measured stratigraphic sections (Fig. 1).Lithostratigraphic and depositional characteristics of the carbonate dominated rocks and planktonic foraminiferal assemblages of the successions in this locality have not been previously documented.

MATERIALS AND METHODS
This study is based on three stratigraphic sections measured from the Bozburun hill locality (Fig. 1).Planktonic foraminifera were studied in thin section as the standard washed-sample methods (hydrogen peroxide and acetic acid) did not work due to hardness of the limestones of the Babadağ Fm. and the micritic and clayey limestones of the Faralya Fm.Thin section analysis as a method has been widely used in planktonic foraminifera studies especially for the Cretaceous with a high degree of confidence (see SARI, 2009SARI, , 2013 for the literature).The position of apertures and the presence of supplementary and accessory structures which were later used for generic distinctions are not identifiable in thin section (CARON, 1985).However, most of the diagnostic criteria including the size and shape of the test, thickness of the wall, size, shape, number and arrangements of chambers, form and position of the aperture, and forms of ornamentation such as ridges, spines, the position and number of peripheral thickenings or keels can be recognized in axial and subaxial sections (section passing through or parallel to the axis of coiling) (SLITER, 1989) are usable data forms.Unfortunately, there have been a limited number of attempts to study Palaeocene planktonic foraminifera from thin section (e.g.POSTUMA, 1971;van KONIJNENBURG et al., 1998;SARI, 2013;SARIGÜL et al., 2017).The resolution of thin-section zonation is nearly as precise as zonal schemes based on isolated specimens for the Cretaceous (SLITER, 1989).The Latest Cretaceous planktonic foraminiferal zonation of the classical Tethyan Gubbio section (Italy) has recently been reviewed by COCCIONI & PREMOLI SILVA (2015), and they also discuss several planktonic foraminiferal bioevents.The Late Cretaceous traditional zonations and bioevents developed and refined by many researchers (i.e.ROBASZYNSKI et al., 1984;CARON, 1985;SLITER, 1989;PREMOLI SILVA & SLITER, 1994;RO-BASZYNSKI & CARON, 1995;LI & KELLER, 1998 a, b;RO-BASZYNSKI, 1998;PREMOLI SILVA & SLITER, 1999;RO-BASZYNSKI et al., 2000;PETRIZZO, 2003;PREMOLI SILVA & VERGA, 2004;HUBER et al., 2008;PÉREZ RODRÍGUEZ et al., 2012 etc.) for almost 30 years have lately been adjusted to an updated time scale (OGG & HINNOW, 2012;ANTHONISSEN & OGG, 2012).Van KONIJNENBURG et al. (1998) showed that the subdivision of the Palaeocene part of the Gran Sasso d'Italy succession (central Appennines) by thin section is nearly as precise as with isolated specimens.Palaeocene planktonic foraminiferal identification is based on van KONIJNENBURG et al. (1998), BERGGREN et al. (1995), OLSSON et al. (1999) and OLSSON et al. (2011). Biozonation of BERGGREN et al. (1995), OLSSON et al. (1999), BERGGREN & PEARSON (2005) and OLSSON et al. (2011) adjusted to an updated timescale ( VAN-DENBERGHE et al., 2012;ANTHONISSEN & OGG, 2012) is followed herein.Because two dimensional axial views of some Palaeocene species in thin section can have a similar appearance, separation of these taxa is not always possible.Therefore, these species are grouped together such as the Morozovella angulata -Morozovella aequa group and Morozovella conicotruncana -Morozovella velascoensis group as in SARI (2013).The other keeled Late Palaeocene taxa such as Globanomalina planoco nica, Globanomalina pseudomenardii, Igorina albeari, Moro zovella acuta, Morozovella acutispira, Morozovella occlusa, Mo rozovella pasionensis and Acarinina subsphaerica can be determined in thin section as their typical characteristics are seen in axial sections.
Thin sections were studied under an Olympus BX50 microscope and photomicrographs were taken by an Olympus E330 camera attached to the microscope.All the specimens and thin sections described and illustrated in this paper are stored in the Department of Geological Engineering of Dokuz Eylül University.

The Babadağ Formation
The Babadağ Fm. named by ERAKMAN et al. (1982) rests on the Ağaçlı Fm. along a local unconformity surface and comprises a 650-1020 m thick limestone dominated succession (ŞENEL, 1997a).The unit locally includes Toarcian 'ammonitico rosso facies' at the base and is mainly represented by cherty micritic limestones and calciturbidites.The limestone succession includes local lenses of radiolarites, cherts and shales several metres thick, comprising rudist shells and fragments at the top (ŞENEL, 1997a;GÜL, 2015).Sedimentological and petrographic characteristics and controlling factors of silicification and types of cherts of the Bozburun hill locality were recently documented by GÜL (2015).
Approximately 80 m of the uppermost part of the Babadağ Fm., made up of four lithostratigraphic levels, was examined in this study (Fig. 3).The succession has well-preserved outcrops at the top of Bozburun hill and by the roadcut to the top of the hill (Fig. 1c).The succession is dominated by light grey, whitish grey, grey, locally dark grey-coloured, medium to thick, locally thinbedded planktonic foraminifera-bearing micritic limestones (Fig. 3, Pl. 1).Calciclastic (or calciturbidite) beds (calcirudites, calcarenites and calcilutites) are intercalated with the micritic limestones.The 8 m thick base of the section comprises chert bands and lenses and shows widespread bioturbation (Level-1).The overlying 22 m (Level-2) is represented by the alternation of micritic limestones and calcarenites, which include rare coarse lithoclasts and bioclasts (i.e.rudists and corals).Level-3 is made up of 15 m of distinctly-bedded micritic limestones with thin siltstone interlayers and chert lenses and bands (Pl.1a).The thickness of the chert bands and lenses ranges between 0.5 to 2.5 m, and they are 0.2 to 3-4 m long.
A few large limestone lithoclast-rich interlayers are also observed within this level (Pl.1d).Some levels comprise several limestone lithoclasts, many of which are planktonic foraminifera-bearing pelagic lithoclasts (Pl.1e).These lithoclasts have sinuous boundaries with the calciclastic facies, in which they are embedded.This indicates that the two facies (i.e.planktonic foraminifera-bearing micritic facies and calciclastic facies) were both soft and not lithified during transportation.A 1 m thick calciclastic bed (laminated calcarenites) in the middle of this level shows low-angle cross-lamination (Pl.1f).This bed is mainly made up of millimetre-to centimetre-sized intraclasts and skeletal debris consisting mainly of rudist fragments.This type of calciclastic beds are interpreted as proximal storm deposits (tempestites) in the literature (AIGNER, 1985;WRIGHT, 1986;FLÜGEL, 2004).
In thin section, the micritic limestones are represented by planktonic foraminifera-bearing wackestone depositional textures, which correspond to a background sedimentation in this type of calciturbidite deposits (Pl.2a-c) (FLÜGEL, 2004).Planktonic foraminifera and other fine clasts show parallel lamination in some beds (Pl.2b), formed as a result of transportation.Calciclastic beds are mainly represented by litho-bioclastic rudstone/ grainstone depositional textures, which are commonly associated with planktonic foraminifera (Globigerinidae)-bearing wackestones/mudstones.Carbonate lithoclasts showing various depositional textures were derived mainly from shallow water (i.e.carbonate mudstone with benthic foraminifera belonging to the family Miliolidae) and slope environments (i.e.rudstone with rudist fragments and benthic foraminifera belonging to family Orbitoidae).Planktonic foraminifera-bearing pelagic lithoclasts are also observed.Some of the lithoclasts are recrystallized.Bioclasts are mainly represented by benthic foraminifera (chiefly Orbitoidae) and rudist shell fragments (Pl.2d, e).These types of facies correspond to the allochthonous parts of the calciturbidite deposits (FLÜGEL, 2004).The irregular and sinuous nature of the boundary between the allochthonous rudstone/grainstone facies and the planktonic foraminifera-bearing wackestone facies suggests that the two facies were not lithified but were soft during transportation.Similar calciclastic deposits were documented from the upper Campanian of the eastern Pontides by SOFRACIOĞLU & KANDEMIR (2013) and SARI et al. (2014).This type of calciclastic deposits (i.e.calciturbidites) (BRAUN-STEIN, 1961) is typically deposited both on the slope and on the deeper sea floor at the base of the slope to basin transition (MEISCHNER, 1964;MCILREATH & JAMES, 1984).Silt to boulder size carbonate particles were derived from the shallowwater platform margin, where benthic organisms such as foraminifera (mainly Orbitoidae), rudists, corals and algae flourished.These deposits are transported down the slope by submarine debris-flows or other mass-transport mechanisms (MCILREATH & JAMES, 1984;PAYROS & PUJALTE, 2008).
The presence of reworked benthic organisms within the succession deposited in a deeper environment indicates that a carbonate platform persisted on a more marginal part of the late Campanian-Maastrichtian basin.

Faralya Formation
The formation is composed of various 'flysch-like' lithologies (i.e.micritic limestones, sandstones, breccia etc.) and basic volcanics and was named by ŞENEL et al. (1989).The lithostratigraphic characteristics and the lateral and vertical facies changes of the Faralya Fm. were documented in 12 stratigraphic sections by ŞENEL (1991).Eight of the sections were measured SE of Çameli (NE of Fethiye), three measured around Babadağ (SE of Fethiye) and one measured from the N of Kalkan (Fig. 1).According to the author, the unit ranges from the Late Palaeocene to Lutetian (Middle Eocene) in age, disconformably overlies the Babadağ Fm. (Fig. 2a) and is tectonically overlain by the Bodrum nappe (ŞENEL, 1991;1997a, b).The thickness of the formation reaches a maximum 290 m (ŞENEL, 1997b).The formation consists of micritic limestones and clayey limestones (or sandy limestones and calcarenites) with local chert lenses at the base in the NE and SE of Fethiye.Towards the top, the formation includes basic volcanics, limestones, breccia with chert clasts, calciturbidites, sandstones, claystones, conglomerates etc., which interfinger with each other (ŞENEL, 1991;ŞENEL, 1997a, b).Details of the lithostratigraphy of the Faralya Fm. in the Bozburun hill locality have not been previously documented.
The patchy outcrops of the Faralya Fm. are observed on the eastern slope of Bozburun hill.Lithological characteristics and planktonic foraminiferal assemblages of the formation were documented by two stratigraphic sections (Figs.1c, 4) as a composite section representing the whole formation could not be found in this locality due to the tectonically disturbed geology of the area.The succession can be divided into four different lithostratigraphic levels in Section-2 (Fig. 4).The 1.5 m thick lowermost part of the section (Level-1) is made up of grey-coloured medium to thick-bedded bioclastic/lithoclastic limestones, which includes planktonic foraminifera-bearing thin pelagic micritic limestone interbeds.Bioclastic/lithoclastic levels (i.e. the lowermost bed, where sample 15-17 was taken) comprise several limestone lithoclasts and bioclasts derived from the Upper Cretaceous.This level is overlain by 3 m of pinkish grey-coloured planktonic foraminifera-bearing laminated micritic limestones with rare chert bands (Level-2).Level-3 comprises an approximately 1 m thick sequence of reddish grey-pale red-coloured calcareous mudstones, with very rare planktonic foraminifera.The overlying Level-4 is represented by mudstone-siltstone alternations with limestone blocks.This part of the section does not yield planktonic foraminifera (Fig. 4).
Diverse lithoclasts and bioclasts are observed within the grainstone/packstone texture of the Level-1 (samples 15-17, 15-25) (Fig. 4).Many of the abundant bioclasts were derived from the uppermost Cretaceous (i.e.benthic foraminifera belonging to the family Orbitoidae and Miliolidae, algae, corals and bryozoa).Some lithoclasts include Campanian-Maastrichtian planktonic foraminifera and other litho-bioclasts are embedded within the rare Palaeocene planktonic foraminifera-bearing micrite matrix.The bed, from which sample 15-24 was taken is a thin interlayer within the litho-bioclastic limestones and comprises planktonic foraminifera-bearing wackestones, which is represented by rare but index keeled Late Palaeocene taxa.Limestones in Level-2 are dominated by planktonic foraminifera-bearing wackestone depositional textures (Fig. 4, Pl.2f), where several Late Palaeocene taxa were identified.
The second stratigraphic section (Section-3) from the Faralya Fm. was measured some 2 km east of the summit of Bozburun hill along the Bozburun hill-Dalyan roadcut (Figs.1c, 5).A 12 m thick part of the formation is observed in this locality, which is made up of an alternation of micritic limestones and brecciated limestones.Micritic limestone levels are represented by planktonic foraminifera-bearing wackestone depositional textures.Intercalating brecciated limestone beds show similar depositional textures with the base of the Section-2 (Level-1).The limestone clasts suggesting various depositional settings (i.e.platform, slope and basin) are embedded within the planktonic foraminifera (Palaeocene taxa)-bearing micritic matrix.Transported benthic organisms such as the latest Cretaceous foraminifera (Orbitoidae), rudist fragments, algae and corals are also observed within the matrix.The angular clasts are larger in Section-3 when compared to Section-2 and ranges up to 15 cm with an average of some 7-8 cm.
These data indicate that deep marine calciclastic deposition occurred during the latest Cretaceous and prevailed in the Late Palaeocene after a sedimentary break corresponding to the Early Palaeocene.

Boundary between the Babadağ and Faralya formations
The boundary between the Babadağ and Faralya formations was reported as a disconformity by ŞENEL (1991) to the NE and SE of Fethiye.The boundary between the two formations is observed in a locality, where section-2 was measured, some 800 m east of the summit of Bozburun hill (Fig. 1c).The Babadağ Fm. in this locality is represented by grey-coloured, well-bedded limestones with chert bands and angular lithoclasts.The limestones are overlain by pinkish grey-coloured friable laminated clayey limestones.The succession is cut by faults to the west and east (Fig. 6).
Cherty limestones of the Babadağ Fm. are represented by rare planktonic foraminifera-bearing wackestones with angular recrystallized intraclasts in thin section.Sample 15-16 is barren, while sample 15-15 comprises a few Campanian-Maastrichtian double-keeled globotruncanids.The assemblage includes Glo botruncana cf.bulloides, G. linneiana and G. mariei, but does not yield index taxa.In the absence of any characteristic taxa, occurrences of G. cf.bulloides and G. linneiana in the uppermost beds of the Babadağ Fm. in that section show that at least the uppermost Maastrichtian is absent in this locality as both taxa make their last occurrences within the lower part of the Abathompha lus mayaroensis Zone (Fig. 7).The overlying laminated micritic limestones are represented by wackestones with mainly globular/ semiglobular-chambered and a few keeled Palaeocene morphotypes (sample 15-18).Two such identified taxa are Morozovella occlusa and Acarinina subsphaerica suggesting that the age of the lowermost layers of the Faralya Fm. is Late Palaeocene (Selandian-Thanetian) in the Bozburun hill locality as both taxa first appear within the P4a Zone (around middle part of Selandian) (Fig 7).Therefore, the boundary is disconformable in this locality and the time gap between the two formations corresponds to the latest Maastrichtian to the earliest Selandian.

Section-1
Micritic limestones of the Babadağ Fm. comprise quite diverse planktonic foraminiferal assemblages, while calciclastic beds include limited amount of taxa (Fig. 3).The planktonic foraminiferal assemblages are mainly represented by double and single keeled globotruncanids, which are associated with rare rugoglobigerinids and multiserial heterohelicids.The following taxa were observed through Section-1; Abathomphalus mayaroensis, Con tusotruncana fornicata, C. cf.plummerae, C. walfischensis, Gansserina gansseri,Globotruncana cf. aegyptiaca,G. arca,G. arcaorientalis,G. bulloides,G. dupeublei,G. esnehensis,G. cf. falsostuarti,G. hilli,G. linneiana,G. mariei,G. neotricarinata,G. orientalis,G. ventricosa,Globotruncanella havanensis,Gl. petaloidea,Globotruncanita conica,Gt. pettersi,Gt. stuarti,Gt. stuartiformis,Gublerina sp.,Racemiguembelina fructicosa,Ra dotruncana subspinosa,Rugoglobigerina pennyi and R. rugosa (Fig. 3,Pl. 3).Many of the taxa identified above are classically observed within the Tethyan Campanian-Maastrichtian deposits (see papers in introduction part).The presence of R. fructicosa and A. mayaroensis within the assemblages is important as they are the nominated taxa of the R. fructicosa and A. mayaroensis zones of the late Maastrichtian (Figs. 3, 7) (e.g.PREMOLI SILVA & VERGA, 2004;GRADSTEIN et al., 2012;COCCIONI & PRE-MOLI SILVA, 2015).Both taxa were rarely observed in the uppermost part of the Babadağ Fm., where sample 15-06 and sam-ple 15-04 include single specimens of R. fructicosa and A. mayaroensis respectively (Fig. 3).The absence of G. bulloides and G. linneiana in sample 15-04 may indicate that the 10 m thick uppermost part of the succession corresponds to the upper part of the A. mayaroensis Zone, or may be younger as these two taxa make their last appearance within the lower part of the A. mayaroensis Zone (Figs. 3, 7).The occurrence of Ga.gansseri in sample 15-11 indicates that the age of this level and the limestones above should not be older than the latest Campanian, while the age of the lowermost part of the succession may be late Campanian.However, this part should not be older than the Gl.ha vanensis Zone as the nominated taxon of the Ra.calcarata Zone, Ra. calcarata was not observed in any samples at the base of the Babadağ succession (Figs. 3, 7).
The planktonic foraminiferal assemblages observed in two sections show that the successions are more or less time equivalent.Therefore, lithological differences between them (i.e. the absence of brecciated limestones in Section-2) could be the result of lateral facies changes within the basin.
Acarinina subsphaerica and M. occlusa are observed in the lowermost limestone beds of the Faralya Fm. (Fig. 6, sample 15-18).Both taxa make their first appearances close to the base of Zone P4a and M. occlusa disappears before the end of Zone P4b (BERGGREN et al., 1995;OLSSON et al., 1999;ANTHONIS-SEN & OGG, 2012) (Fig. 7).Therefore the age of the lowermost layers of the Faralya Fm. is Late Palaeocene (middle Selandianmiddle Thanetian) at the Bozburun hill locality (Figs. 6,7).Alternatively, taking into account the fact that the planktonic foraminiferal assemblages of both sections of the Faralya Fm. indicate a clear Thanetian age, the age of the lowermost beds of the formation is also Thanetian, but indicators of the Thanetian (i.e.M. acuta, G. planoconica etc.) were somehow not observed in the sample.In this case, the Danian and Selandian (corresponding to some 7 Ma duration of time), are missing at the Bozburun hill locality.

DISCUSSION AND CONCLUSIONS
Lithostratigraphic characteristics and planktonic foraminiferal assemblages of the upper part of the Babadağ Fm. and the lower part of the Faralya Fm. have been documented for the first time by three stratigraphic sections from the Bozburun hill locality of the Tavas nappe of the Lycian nappes.
The upper parts of the Babadağ Fm. are mainly represented by cherty micritic and calciclastic limestones.Micritic limestone beds comprise diverse planktonic foraminiferal assemblages yielding a late Campanian-Maastrichtian age.A late Maastrichtian age is obtained from the uppermost layers of the Babadağ Fm., based on the presence of R. fructicosa and A. mayaroensis.An abundance of keeled globotruncanids (K-selection) within the assemblages indicates a relatively deep pelagic environment as these large, thick-walled, complex morhotypes dominate in open oceans, mainly during the onset of high sea level stands (CARON & HOMEWOOD, 1983;ROBASZYNSI & CARON, 1995;ABRAMOVICH et al., 2010).The Faralya Fm. is studied in two sections, which have different lithological properties but similar planktonic foraminiferal assemblages and ages.Section-2 is mainly made up of planktonic foraminifera-bearing wackestones with calciclastic beds at the base and mudstones with limestone blocks at the top.Section-3 is represented by the alternation of planktonic foraminifera-bearing wackestones and brecciated limestones.Planktonic foraminiferal assemblages of the two sections are dominated by keeled Late Palaeocene morphotypes.Occurrence of M. acuta at the base of Section-2 suggests that the age of the lowermost part of the section is not older that the Thanetian.Likewise, the presence of M. cf.acuta and G. planoconica at the base and top of Section-3 respectively shows that the age of the lowermost part of the section is not older that the Thanetian as in Section-2 and the age of the upper part is late Thanetian (Zones P4c or P5).
A unique section including the disconformable boundary of the Babadağ and Faralya formations at the Bozburun hill locality shows that the latest Maastrichtian to earliest Selandian rocks are absent.A gap of similar duration between two formations was also reported to the north and east of the study area (N and E of Fethiye) by ŞENEL (1991).The latest Cretaceous-Early Palaeocene unconformity in the Tavas nappe was linked with the first of the three main tectonic events, when trench-passive margin collision caused ophiolite obduction and the Köyceğiz Thrust Sheet was incorporated into the Lycian allochthon (COLLINS & ROBERTSON, 1998).During that time interval, the upper levels of the Lycian allochthon were subaerially exposed.The presence of eroded Cretaceous carbonates and foraminifera observed within the Thanetian calciclastic rocks as lithoclasts or bioclasts could be clues to that exposure and erosion (i.e. the base of the Section-2) (Fig. 4).

Figure 1 .
Figure 1.a) The main tectonostratigraphic zones of Turkey (after GÖRÜR & TÜYSÜZ, 2001).Lycian nappes represents the westernmost part of the Anatolide-Tauride Block, b) Simplified geological map of SW Turkey, showing main tectonostratigraphic units and location of the study area (after ŞENEL, 1997a), c) Geological map of Bozburun hill and surroundings, showing the studied units of the Babadağ and Faralya formations and locations of the studied sections (simplified after ŞENEL, 1997a).

Figure 2 .
Figure 2. a) A stratigraphic column of the Tavas nappe (simplified after ŞENEL, 1997a).Studied sections correspond to the uppermost part of the Babadağ Formation and the lowermost part of the Faralya Formation (age of the Tekedere and Karadağ series is adapted from MOIX et al., 2013), b) Tectonostratigraphic positions of the nappe piles of the Lycian nappes over the relatively autochthonous units.The Tavas nappe lies at the base of these nappe packages (simplified after ŞENEL, 1997a).

Figure 4 .
Figure 4.A stratigraphic column of the Faralya Formation with the distribution of planktonic foraminifera in Section-2 (Coordinate; 35 S 0646439/4070628).See Figure 2. for explanation of symbols.

Figure 5 .
Figure 5.A stratigraphic column of the Faralya Formation with the distribution of planktonic foraminifera in Section-3 (Coordinate: 35 S 0647417/4070469).See Figure 2. for explanation of symbols.

Figure 6 .
Figure 6.Cretaceous/Palaeocene boundary section, observed as a thin sequence package between two faults (Coordinates: 35 S 0646439/4070628).The boundary includes a gap ranging from the latest Maastrichtian to the earliest Selandian.

Figure 7 .
Figure 7. Latest Cretaceous-Palaeocene planktonic foraminiferal biozones and bioevents of some selected stratigraphically important taxa (first and last appearance datums) observed in this study.Numerical ages, biozones and the first and last appearance datums of the selected taxa are adapted from OGG & HINNOW (2012) and ANTHONISSEN & OGG (2012) (for the Upper Cretaceous) and VANDENBERGHE et al. (2012) and ANTHONISSEN & OGG (2012) (for the Palaeocene).

Table 1 .
Correlation of several names attributed to the Tavas nappe.