A Key Unit for Understanding Late Cretaceous Evolution of the Pontides, N Turkey

PALAEO-07329; No of Pages 17 Palaeogeography, Palaeoclimatology, Palaeoecology xxx (2015) xxx–xxx

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Palaeogeography, Palaeoclimatology, Palaeoecology

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The Kapanboğazı formation: A key unit for understanding Late Cretaceous evolution of the Pontides, N Turkey

Okan Tüysüz a,⁎, Mihaela C. Melinte-Dobrinescu b, İsmail Ömer Yılmaz c, Sabri Kirici d, Lilian Švabenická e,PetrSkupienf a Istanbul Technical University, Eurasia Institute of Earth Sciences, 34469 Maslak, Istanbul, Turkey b National Institute of Marine Geology and Geo-ecology (GEOECOMAR), Bucharest, 23–25 Dimitrie Onciul Street, RO 024053, Romania c Middle East Technical University, Faculty of Engineering, Dept. of Geology, ODTÜ, Ankara, Turkey d Turkish Petroleum Co, Söğütözü Mahallesi 2180. Cad. 86, 06520 Çankaya, Ankara, Turkey e Czech Geological Survey, Klárov 131/3, 118 21 Praha 1, Czech Republic f VSB, Technical University Ostrava, Faculty of Mining and Geology, Institute of Geological Engineering, 17, Listopadu 15, Ostrava, Poruba, Czech Republic article info abstract

Article history: The Pontides forming the south-western continental margin of the Black Sea consist of two tectonic units, the Received 20 January 2015 Istanbul Zone in the west, and the Sakarya Zone in the central and eastern parts. The Sinop Basin in the Sakarya Received in revised form 19 June 2015 Zone is filled, from base to top, by Hauterivian to Albian turbidites, Cenomanian–Turonian red pelagic sediments, Accepted 24 June 2015 Turonian–Campanian magmatic-arc and related deposits, and by the uppermost Campanian to middle Eocene Available online xxxx post-magmatic units developed on the southern passive margin of the Black Sea. Based on nannofossil, dinofla- ğ ı – Keywords: gellate, Foraminifera and Radiolaria data we describe the Kapanbo az Formation, a Cenomanian Turonian unit Central Pontides in the Sinop Basin, represented by red calcareous/siliceous pelagic shales, limestones and cherts passing gradu- Sinop Basin ally from the Albian black shales. These sediments possibly represent deepest depositional conditions of the Albian–Turonian interval basin during the Cenomanian–Turonian interval and also reflect the transition from an anoxic to an oxic Litho- and biostratigraphy palaeoenvironmental setting. The Istanbul Zone to the west was emerged during the deposition of the Tectonics Kapanboğazı Formation in the Sakarya Zone. Palaeoenvironment In the Pontides, red pelagic sediments were deposited at different times during the Cenomanian–Maastrichtian interval. Because the Kapanboğazı Formation was deposited only in the Sakarya Zone and because it is present in limited outcrops due to structural reorganization and thick overlying volcanoclastic pile, most previous authors assumed Cenomanian–Turonian hiatus. Herein we describe detailed palaeontological data from this unit and discuss their importance to the interpretation of depositional history and tectonics of the Black Sea region, as well as climatic and eustatic implications. © 2015 Elsevier B.V. All rights reserved.

1. Introduction Zonguldak and Ulus basins in the Istanbul Zone, and the Hauterivian up to Cenomanian sediments of the Sinop Basin in the Sakarya Zone The western part of the Pontides (Ketin, 1966; Şengör and Yılmaz, (Figs. 1band2), reflect opening and deepening periods of these basins 1981; Okay and Tüysüz, 1999), forming the southern continental mar- (Tüysüz, 1999). gin of the Black Sea, consists of two tectonic units: the Istanbul Zone Different opinions on the stratigraphic evolution of these basins in the west and the Sakarya Zone in the east (Fig. 1a; Okay, 1989; have been presented in the literature. According to Okay et al. (2006, Okay and Tüysüz, 1999). These two tectonic units are also known, geo- 2013), and an earlier opinion of Şengör and Yılmaz (1981), the Istanbul graphically, as the Western and Central Pontides, respectively. The Zon- and Sakarya zones juxtaposed before the Late Jurassic, and Lower Creta- guldak and Ulus basins in the Istanbul Zone, and the Sinop Basin in the ceous sediments filling these basins were fed by a common source to the Sakarya Zone (Fig. 1b) were mainly filled by Lower Cretaceous sedi- north. Okay et al. (2006, 2013) assumed that the Pontides had collided ments and by Upper Cretaceous volcanic/volcanosedimentary rocks with a continental Domuzdağ fragment to the south during the Albian (Fig. 2). The Upper Barremian up to Albian sediments of both the stage, and this collision caused the development of a regional metamorphism along the southern periphery, and the uplifting and emergence of the Western and Central Pontides. ⁎ Corresponding author. Based on calcareous nannoplankton biostratigraphy, Hippolyte et al. E-mail addresses: [email protected] (O. Tüysüz), [email protected] (M.C. Melinte-Dobrinescu), [email protected] (İ.Ö. Yılmaz), [email protected] (2010) showed that sedimentation was continuous in the Zonguldak (S. Kirici), [email protected] (L. Švabenická), [email protected] (P. Skupien). Basin from the Late Barremian to Late Albian in a deepening upward

Fig. 1. a: Tectonic units of Turkey; b: simpliﬁed geological map of the Pontides. Red dashed line indicates boundary between Istanbul and Sakarya Zones (Intra-Pontide Suture, after Tüysüz et al., 2012). (For interpretation of the references to colour in this ﬁgure legend, the reader is referred to the web version of this article.) O. Tüysüz et al. / Palaeogeography, Palaeoclimatology, Palaeoecology xxx (2015) xxx–xxx 3

Fig. 2. Stratigraphic chart of the Cretaceous of the Istanbul and Sakarya zones. Lower Cretaceous sediments of the Zonguldak basin are represented by marginal marine sediments at the base. These consists of the Çengelli, İncigez, Kilimli and Velibey formations (shallow marine siliciclastics) and Kapuz formation (platform carbonate) at the base and the Sapça and Tasmaca formations at the top (deepening-upward glauconitic sandstones and bluish marls, respectively). The Ulus and Çağlayan formations are represented by siliciclastic turbidites with debris- flow horizons. See the text for the other formations (partly modified after Tüysüz et al., 2004). environment, in contrast to the Albian uplift hypothesis of Okay et al. that the Dereköy Formation forms the first common cover of the Istan- (2013). The Zonguldak Basin was uplifted and eroded during the bul and Sakarya zones, and postdates the juxtaposition of these zones Cenomanian as previously indicated by Tüysüz (1999). Except for the during the Cenomanian, just prior to the start of the Pontide arc suspicious ammonite finding by Tokay (1952) no other fossil data indi- magmatism. cate a depositional interval in the Istanbul Zone during the Cenomanian The Dereköy Formation is unconformably overlain by the Upper stage. Santonian pelagic limestones of the Unaz Formation and volcanic/ The Hauterivian to Albian sediments of the Sinop Basin in the volcanosedimentary rocks of the Campanian Cambu Formation (Fig. 2). Sakarya Zone are also represented by deepening-upward siliciclastic Following the report of Ketin and Gümüş (1963),subsequentstudies sediments. In contrast to the Istanbul Zone, the Cenomanian–Turonian by Görür et al. (1993), Okay et al. (2006) and Hippolyte et al. (2010) interval in this basin was the deposition time of deep marine sediments, erroneously used the name “Kapanboğazı Formation” for all Upper namely the Kapanboğazı Formation (Fig. 2). This formation was Cretaceous red pelagic sediments occurring in the Western and Central originally described by Ketin and Gümüş (1963) as being composed of Pontides, without reference to their age and stratigraphic position. red pelagic micritic limestone and shale. In the original description, Recently, Tüysüz et al. (2012) separated and described one of these sed- these authors determined the age of the formation as Upper imentary horizons, the Unaz Formation, and discussed its importance Cenomanian–Turonian based on the planktic foraminifera Ticinella for the geological evolution of the Black Sea region. roberti, Globigerinella aequilateralis, Globotruncana delrioensis turbinata, The aim of this paper is to present the newly acquired data on the Globotruncana renzi, Globotruncana imbricata, Globotruncana lapparenti lithostratigraphy and biostratigraphy of the Kapanboğazı Formation inflata, Globotruncana lapparenti lapparenti, Globotruncana lapparenti that was deposited at the beginning of the Late Cretaceous times only coronata, Globotruncana lapparenti bulloides,andGlobotruncana in the Sakarya Zone. Observed modifications in the overall geological lapparenti tricarinata. context are linked herein to tectonic and eustatic changes. According to Tüysüz (1999) the Istanbul and the Sakarya zones were separated by the Intra-Pontide Ocean until the Cenomanian. A thick vol- 2. Geological setting canic/volcanosedimentary succession, the Dereköy Formation, forms the first common cover of both tectonic units (Fig. 2). The lower part The Pontide magmatic arc extends from the Srednagorie region in of the succession, reaching up to 800 m in thickness, starts with a Bulgaria up to the Caucasus in Georgia, including both the Istanbul thick basal conglomerate grading upward into an alternation of calc- and the Sakarya zones. First products of the Pontide magmatic arc alter- alkaline and acidic to intermediate lavas and pyroclastics, with pelagic nate with the Middle Turonian sediments (Tüysüz et al., 2012). This micritic limestones and turbiditic clastics. The foraminiferal assem- magmatic activity lasted until the end of the Campanian and locally blages found in the oldest pelagic limestone beds and in the matrix of until the Maastrichtian. There is a general agreement that this arc was debris flow horizons in the middle part of the formation indicate the established in response to northward subduction of the northern Middle Turonian age (Tüysüz et al., 2012). Tüysüz (1999) advocated Tethys, namely the İzmir–Ankara–Erzincan Ocean (Çoğulu, 1975;

Akın, 1978; Moore et al., 1980; Akıncı, 1984; Ohta et al., 1988; Aykol and micropalaeontological studies that include non-calcareous dinoflagel- Tokel, 1991; Berza et al., 1998; von Quadt et al., 2005; Karacıkand lates, foraminifers, radiolarians, and calcareous nannofossils. Tüysüz, 2010). Fifty thin sections of samples for planktic foraminifera were Tüysüz (1999) and Tüysüz et al. (2012) divided this magmatic activ- prepared and investigated using the Olympus transmitting light micro- ity into two depositional intervals, separated by a regional unconformi- scope at Turkish Petroleum Co. Research Department, Ankara, Turkey. ty, which is overlain by the Upper Santonian Unaz Formation composed Biostratigraphic data were interpreted applying biostratigraphy of mainly of pelagic limestones (Fig. 2). The lower volcanic succession, the Postuma (1971), Robaszynski and Caron (1979), Caron (1985),and Dereköy Formation, was formed between the Middle Turonian and Premoli Silva and Verga (2004). Early Santonian, while the upper volcanic succession, the Cambu For- Samples for non-calcareous dinoflagellate cysts were processed by mation, during the Campanian. Geochemical characteristics of these standard palynological technique. After washing and drying, the stan- two magmatic periods are also different (Keskin and Tüysüz, 1999, dard processing involved chemical treatment of 40 g of the sample 2001; Keskin et al, 2003). Hippolyteetal.(2010)disregarded the with HCl to remove the calcareous fraction and with HF to remove sili- Dereköy Formation and assumed a stratigraphic gap between the Late cates. Sieving was performed with a 10 μm nylon mesh, and the samples Albian and Coniacian. were centrifuged to concentrate the residues. Three slides of each Both volcanic units are dominantly composed of volcano- sample were prepared. Whole slides of residues were investigated sedimentary rocks associated with basaltic and andesitic lava, as well under a binocular transmitted light microscope to identify and count as pyroclastics; the total thickness of both volcanic units exceeds the organic particles and dinoflagellate cysts. The palynological perma- 3000 m in places. Some Campanian to Maastrichtian intrusive bodies nent mounts are stored at the Institute of Geological Engineering at the also exist, such as the Demirköy and Dereköy Plutons in the Rhodope– VSB — Technical University of Ostrava, Czech Republic. Strandja Zone in the westernmost Pontides (Fig. 1a; Moore et al., Calcareous nannofossils were investigated in the fraction of 2–30 μm

1980; Aydın, 1982; Ohta et al., 1988), the Çavuşbaşı Granitoide in the vi- separated by decantation method using 7% solution of H2O2.Atfirst, cinity of Istanbul (Şahin et al., 2012) and the Hamitli rhyodacite near the red-brown limestone was disintegrated into fine powder. Smear- Cide in the Western Pontides (Akyol et al., 1974), as well as the Dodurga slides were mounted with Canada Balsam and inspected at 1000× granitoides, located south of Sinop, in the Central Pontides (see Fig. 1b; magnification, using an oil-immersion objective on a Nikon Microphot- Tüysüz, 1993). FXA transmitting light microscope. Biostratigraphic data were Red pelagic limestones and calcareous shales are present as thin in- interpreted applying Burnett (1998) UC (Upper Cretaceous) zones. terlayers at different horizons within both these volcanic and post- Calcareous nannoplankton taxonomic identification follows Perch- volcanic successions. Some of these horizons can be traced at regional Nielsen (1985) and Burnett (1998). level, tens of kilometres (see Unaz Formation, Tüysüz et al., 2012) along the Pontides, while some others have a local lateral extension. 4. Results All these red pelagic sediments were erroneously grouped into a single formation, namely the Kapanboğazı Formation (Gedik and Korkmaz, 4.1. Kayadibi section 1984; Görür et al., 1993; Hippolyte et al., 2010). Some of the red pelagic sediments occurring in the Kapanboğazı Formation overlie Lower This section is located north of Boyabat Town in Sinop Province Cretaceous dark grey shales; hence, this lithological modification was (Fig. 1b) just to the north of Günpınar–Kayadibi Village (36 T 647280/ interpreted as indicator of changing depositional conditions from an an- 4614340, WGS84). The oldest sediments of the region are Triassic turbi- oxic to an oxic depositional regime (Görür et al., 1993). dites of the Akgöl Formation (Ketin and Gümüş,1963), unconformably Görür et al. (1993) concluded that the rifting of the Black Sea back- overlain by Upper Jurassic red continental conglomerates and mud- arc basin initiated during the Aptian, and was followed by syn-rift stones (the Bürnük Formation), and by Kimmeridgian to Berriasian sedimentation and subsidence until the Late Cenomanian, when ocean platform carbonates (the İnaltı Formation). floor spreading and thermally induced subsidence began. After the ThebaseoftheKayadibisectionisformedbytheÇağlayan Formation breakup of the continental crust during the Late Cenomanian, the south- represented by siliciclastic turbidites with abundant debris-flow horizons ern margin of the Black Sea subsided and tilted basinward, which and olistoliths exceeding 1 km in size. The Çağlayan Formation was de- caused a wide transgression. As a result of this transgression a major posited in a highly active tectonic environment, as indicated by the em- post-breakup unconformity developed at the base of the pelagic lime- placement of huge olistoliths from underlying units, i.e., Permian up to stones and marls. Following the onset of spreading in the Black Sea, the lowermost Cretaceous, as well as by laterally and vertically changing the anoxic conditions of the rift stage were replaced by oxic conditions, facies properties and thickness. This formation is regarded as having been giving way to the deposition of red pelagic sediments. Tüysüz (1999) deposited during the rifting phase of the Sinop Basin that took place be- and Tüysüz et al. (2012) also agree with this tectonic scenario but, tween the Hauterivian and the Albian stages (Görür, 1988; Yiğitbaş et al., based on both new biostratigraphic data from the sediments below 1990; Tüysüz, 1990, 1993; Hippolyte et al, 2010). The youngest part of and above this unconformity and absence of subduction-related the Çağlayan Formation, beginning of the section studied, is represented magmatism before the Turonian, they concluded that the back-arc by black to dark grey, thinly bedded to laminated siliceous shales alter- rifting of the Western Black Sea Basin occurred during the Turonian– nating with fine to very fine grained lithic silts and sandstones (Fig. 4; Early Santonian period, and that the regional unconformity at the base Plate 1a and 1b). Td-e Bouma's (1962) sequences within this fine- of the Upper Santonian sediments corresponds to the break-up of the grained part of the formation imply a distal turbidite environment. Up continental crust and beginning of oceanic spreading. Based on offshore the section, the silts and sandstones replaced by red shales alternating seismic data, Nikishin et al. (2015a, 2015b) also agree to the Turonian– with thin (0.5–3 cm) dark-grey and blackish shales and the Çağlayan For- Early Santonian rifting model. mation passes into the Kapanboğazı Formation. Towards the top of the section, red silicified shales, marls, and light grey micritic limestones with some black shale alternations are the main lithological components 3. Material and methods ( Plate1b). In fact, the uppermost 10 m of the section exhibit cm to mm cyclic alternations of red shales, marls and cherts, with no dark grey or The Kapanboğazı Formation, occurring in the Sinop Basin of the black shale (Plate 1c). The total thickness of the Kapanboğazı Formation Sakarya Zone, was studied in two outcrops, the Kayadibi and Namazlık in the section described above is about 27 m (Fig. 4). sections, and one borehole, the Fasıllı-1 well (Fig. 3). Sections were The dark-grey shales of the upper part of the Çağlayan Formation investigated from a lithological point of view and sampled for yielded non-calcareous dinoflagellates (Figs. 4 and 5; Table 1)with

Fig. 3. The simpliﬁed geological map of the Sinop Basin showing location of studied sections.

the stratigraphically signiﬁcant taxa Cerbia tabulata, Florentinia stellata, The dinoﬂagellate assemblages found in the dark-grey shales in the and Systematophora cretacea, indicating Lower and Middle Albian ages uppermost part of the Çağlayan Formation and in the alternating black (Skupien, 2003). and red shales and micritic limestones in the lowermost part of the

Fig. 4. Litho- and biostratigraphy of the Kayadibi and Namazlıksections.

Plate 1. Outcrop photos of the Çağlayan and Kapanboğazı formations. a) Albian black shales alternating with thin-bedded turbiditic sandstones, the Kayadibi Section, b) Albian, Cenomanian and Turonian units in the Kayadibi Section, c) Turonian red shales and cherts in the Kayadibi Section, d) Turonian red calcareous shales and micritic limestones in the NamazlıkSection.

Kapanboğazı Formation contain, above others, the marker species intermedium (specimens with 5 segments) (Table 2; Figs. 4 and 6). Many F. stellata, Odontochitina costata and Palaeohystrichophora infusorioides authors have argued that the Cenomanian–Turonian boundary falls with- (see Table 1) that support a latest Albian to Early Cenomanian age in the UC5c subzone, and hence the first occurrence of the nannofossil (Skupien et al., 2009). The occurrence of the dinocyst species Q. intermedium is the youngest Cenomanian nannofloral event (Burnett, O. costata (Fig. 4, sample D5) indicates Cenomanian (Skupien et al., 1998; Paul et al., 1999; Hardas and Mutterlose, 2006; Wagreich et al., 2009). 2008; Švábenická, 2012; Melinte-Dobrinescu et al., 2013). Nannofossils identified in the samples collected from the lower part Radiolarian assemblages found in the uppermost part of the Kayadibi of the Kapanboğazı Formation indicate Cenomanian and lowermost section contain the taxa Crucella cachensis, Alievum superbum, Patellulla Turonian (Fig. 4). In these horizons, nannofossils were found only in verteoensis, Patellulla elliptica, Stichomitra mediocris, Stichomitra the red marls and limestones that provided mostly fragmented and stocki, Dictyomitra multicostata, Pseudodictyomitra pseudomacrocephala, strongly overgrowth specimens. Watznaueria barnesiae forms about Diacanthocapsa ovoidea, Halesium triacanthum, Pessagnobrachia fabianii, 60–70% of the assemblage and this phenomenon may indicate Cavaspongiae c. uganea and Pseudoaulophacus putahensis. According to strong dissolution (Roth and Krumbach, 1986). The co-occurrence of these data, Luo (2005) assumed a Turonian age for the Kapanboğazı Corollithion kennedyi and Prediscosphaera cretacea indicates the upper Formation at this locality. part of the UC1 zone, Lower Cenomanian (Figs. 4 and 6). Recently, Yılmaz et al. (2010) have established a biostratigraphic Upwards in the section, the nannoplankton assemblages contain framework for the same section, by using planktic foraminiferal and biostratigraphically significant taxa indicating Middle Cenomanian radiolarian microfaunas. A late Cenomanian age was determined for (UC3a zone): Gartnerago theta, Gartnerago segmentatum, Gartnerago the Kapanboğazı Formation based on the successive occurrence of nanum, Axopodorhabdus albianus and Microrhabdulus decorates the planktic foraminifer Rotalipora cushmani total range zone and (Table 2, Figs. 4 and 6). Dicarinella algeriana partial zone, respectively, and the presence of A latest Cenomanian–early Turonian age, UC5c subzone for the middle the Dactyliosphaera silviae radiolarian total range zone (Fig. 4). The part of the section is indicated by the end-Cenomanian marker Quadrum Cenomanian–Turonian boundary interval was pointed out by the

Fig. 5. Dinoﬂagellate cysts from the dark-grey shales of the upper part of the Çağlayan Formation (1–9) and from dark-grey shales of the lowermost part of the Kapanboğazı Formation (10–16), Kayadibi section. Scale bars 20 μm. 1 — Circulodinium distinctum,2— Callaiosphaeridium asymmetricum,3,4— Palaeoperidinium cretaceum,5— Hystrichodinium pulchrum, 6 — Spiniferites ramosus,7— Florentinia laciniata,8— Oligosphaeridium complex,9— Tehamadinium tenuiceras,10— Palaeohystrichophota infusorioides,11— Coronifera oceanica, 12 — Pervosphaeridium sp., 13 — Pervosphaeridium pseudhystrichodinium,14— Surculosphaeridium longifurcatum,15— Odontochitina costata,and16— O. operculata.

Table 1 Kayadibi Section — non-calcareous dinoﬂagellte cyst distribution and stratigraphic interpretation. Bold — stratigraphically signiﬁcant taxa, * present.

Fig. 6. Calcareous nannofossils from the red marlstones to limestones, lower part of the Kapanboğazı Formation, Kayadibi section, Lower Cenomanian. Specimens are mostly fragmented and highly overgrown. Photographs in cross-polarized light (XL), 13 and 19 in plane-polarized light (PL). 1, 2 — Eiffellithus turriseiffelii,3,4— Corollithion kennedyi,5— Gartnerago nanum (fragment), 6 — Axopodorhabdus albianus,7— Biscutum ellipticum,8— Broinsonia enormis,9— Rhagodiscus achlyostaurion,10— Zeugrhabdothus bicrescenticus,11,12— Zeugrhabdothus embergerii (highly overgrown specimens), 13, 14 — Prediscosphaera columnata, owergrowth specimen in PL and XL, 15 — Prediscosphaera sp. (spine), 16 — Lithraphidites carniolensis, 17 — Cretarhabdus striatus (fragment), 18 — Manivitella pemmatoidea (fragment), 19–21 — Eprolithus ﬂoralis (19 and 20 same specimen in PL and XL), 22 — Watznaueria barnesiae, 23 — Watznaueria biporta,and24— Quadrum intermedium.

Table 2 Kayadibi Section nannofossil distribution and stratigraphic interpretation. Abundance of nannofossil taxa: F (few) = ±1 specimen/1 field of view, R (rare) = 1–9specimens/10fields of view, VR (very rare) = b1specimen/10fields of view, EP = only 12 specimens were found, f = fragments. Sample abundance: L = N5 specimens/10 fields of view, VL = 1–5 specimens/ 10 field of view, EL = b1 specimen/10 fields of view. Nannofossil preservation: VP (very poor) = nannofossils are dissolved and/or fragmented and some specimens are difficult to identify, EP (extremely poor) = nannofossils are dissolved, fragmented, most of the specimens are difficult to identify.

presence of planktonic foraminifera Whiteinella archeocretacea partial below these. From 1246 m depth down to its base at 2626 m the drill range zone and the radiolarian Alievium superbum/C. cachensis partial traverses a thick sequence of low-grade metamorphosed spilitic lava range zones. and serpentinites, possibly belonging to the Triassic ophiolites of the Küre Unit (see Güner, 1980; Tüysüz, 1990, 1999; Okay et al., 2013, 4.2. Namazlıksection 2014). The contact between the ophiolites and the overlying red limestone/ This section is located on Namazlık Hill (36 T 632412/4623760, WGS shale succession does not crop out in the ﬁeld; hence, its nature remains 84), about 1 km NE of Kapanboğazı Hill (Kirici et al., 2011; Fig. 3) and controversial. Based on the complicated tectonics in the region, with represents the stratotype of the Kapanboğazı Formation (Ketin and many folds and imbricate thrusts (see Sunal and Tüysüz, 2002), the ex- Gümüş,1963). In this outcrop, the base and the top of the formation is istence of a detachment fault, a member of a duplex structure developed covered and the contact with underlying and overlying formations is during the Eocene, may be assumed. On the other hand, identiﬁcation of not obvious. Red and dark grey calcareous/siliceous radiolarian shales, serpentinite fragments at the base of Cretaceous red strata may suggest cherts and micritic limestones are exposed at the visible base of the sec- a nonconformity at the base of red pelagic limestones and shales. This tion (Plate 1d), very similar to those described in the Kayadibi section. phenomenon may explain the absence of the Albian dark-grey shales Below these red strata, black shales of the Çağlayan Formation occur, in- that were discovered in the surface sections. The ophiolitic rocks cluding thin turbiditic sandstone intercalations, containing the Late at the base of the Fasıllı-1 can also be interpreted as a huge syn- Albian dinocyst taxon Litosphaeridium siphoniphorum. sedimentary block within the Çağlayan Formation. Such blocks, exceed- Similar to the Kayadibi section, the contact between the Çağlayan ing 1–2 km in size, were already found in some outcrops of this forma- and Kapanboğazı formations, i.e., between the distal turbidites and the tion (Yiğitbaş et al., 1990; Tüysüz, 1993; Aydınetal.,1995). overlying red sediments, is probably gradual at Namazlık Hill. The red The lowermost part of the red limestones, shales and radiolarian calcareous/siliceous radiolarian shales, cherts and micritic limestones cherts, interpreted as the Kapanboğazı Formation, contains foraminifer- of the Kapanboğazı Formation are barren of fossils here. al assemblages with Parathalmanninella appenninica, Praeglobotruncana Up the section, thin-bedded argillaceous, brownish red micritic gibba, Muricohedbergella cf. delrioensis, Rotalipora sp., Muricohedbergella limestones and wackestones occur. This 35 m thick horizon (Fig. 4)is sp., Macroglobigerinelloides sp., Heterohelix sp. and some undetermined rich in radiolarian tests and comprises planktic foraminifers including radiolarian tests, indicating uppermost Albian and Cenomanian. Helvetoglobotruncana helvetica, Whiteinella praehelvetica, Whiteinella Up the section, in the red, pinkish and white, thinly bedded micritic paradubia, Praeglobotruncana stephani, Praeglobotruncana cf. gibba, limestones alternating with basaltic and andesitic lava, pyroclastics Dicarinella hagni, Dicarinella canaliculata, Dicarinella imbricata, tuffs and volcanoclastic sandstones, the foraminiferal microfauna Marginotruncana renzi, Marginotruncana coronata, Muricohedbergella contains the following taxa: Marginotruncana angusticarinata, M. cf. cf. ultramicrus/prainehillensis, Muricohedbergella simplex, Macro- coronata, Marginotruncana pseudolinneiana, Dicarinella cf. imbricata, globigerinelloides sp., Praeglobotruncana sp., Dicarinella sp. and Muricohedbergella sp., Macroglobigerinelloides sp. and Heterohelix Heterohelix sp. (Fig. 7), indicating Middle–Late Turonian age sp., and undetermined radiolarian tests (Fig. 9). Foraminifers indicate (Robaszynski and Caron, 1979; Premoli Silva and Verga, 2004). Turonian–Coniacian (Postuma, 1971; Robaszynski and Caron, 1979; The Kapanboğazı Formation in the Namazlık section is Robaszynski et al, 1984; Caron, 1985; Premoli Silva and Verga, 2004). disconformably overlain by whitish beige, sandy limestones enclosing Based on its lithology, age and stratigraphic position this part of some volcanic fragments. These bioclastic grainstones and wackestones the section can be attributed to the Dereköy Formation (Tüysüz et al., can be correlated with the Upper Santonian–Campanian Unaz Forma- 2012). tion in the Zonguldak Basin by means on their fossil content (Kirici On top of the volcanic and volcanogenic units is a thin horizon of et al., 2011), lithology and stratigraphic position (Tüysüz et al., 2012). pinkish to white, thinly bedded micritic limestones of the Unaz Forma- tion with an intraclastic conglomerate at the base. This part of the sec- 4.3. Fasıllı-1 Well tion is overlain by volcanic and volcanogenic units of the Cambu Formation that also contain some interbedded red limestones. Lime- The Fasıllı-1 exploration well was drilled in 1967. It is situated about stones of both formations contain rich foraminiferal assemblages with 20 km NW of the Kayadibi location, on the crest of the Domuz anticline Globotruncanita conica, Globotruncanita stuarti, Globotruncana arca, (36 T 639645/4630491, WGS84) of the Sinop Basin (Demirer and Kirici, Contusotruncana fornicata, Globotruncana gr. linneiana, Globotruncana 1996; Fig. 3). The Fasıllı-1 well (Fig. 8) penetrated Upper Cretaceous sp., Muricohedbergella sp., Macroglobigerinelloides sp., and Heterohelix volcanic and volcanogenic units, and red pelagic limestones and shales sp., indicating a depositional interval from the Santonian up to

Fig. 7. Planktic foraminifera from the NamazlıkSection.1–4 Whiteinella preahelvetica,5— Helvetoglobotruncana helvetica,6— Marginotruncana renzi,7— Marginotruncana coronata,8–10 — Dicarinella hagni,11— Praeglobotruncana cf. gibba,12,13— Praeglobotruncana stephani,14— Dicarinella imbricata,15— Muricohedbergella ﬂandrini, 16 — M. simplex,and17— Radiolaria.

Maastrichtian (Robaszynski et al., 1984; Caron, 1985; Premoli Silva and 5. Discussion Verga, 2004). Although it was not detected in the borehole log, existence of an unconformity is assumed at the base of the Santonian The presented stratigraphic sections indicate the existence of a deep micritic limestones (Unaz Formation). This hypothesis is supported by marine environment in the Sakarya Zone during the Albian to Turonian the surface relationships observed in the same region in the Upper interval, before the development of the Pontide magmatic arc. This con- Cretaceous sediments, and by the occurrence of intraclastic conglomer- clusion differs from previous interpretations that proposed a strati- ates, which are characteristic of the base of the Unaz Formation (see graphic gap within the Albian–Coniacian (Hippolyteetal.,2010)or Tüysüz et al., 2012). In contrast to the Kayadibi section, the Çağlayan Albian–Turonian interval (Okay et al., 2013). Tüysüz et al. (2012) dark-grey shales were not observed in the lowermost parts of the mapped a regional unconformity at the base of the Late Santonian all Fasıllı-1 well, but microfossil data from the base of the sediments, pen- along the Istanbul Zone. According to our ﬁeld observations, this uncon- etrated by the drilling, indicate an open marine setting during the up- formity also continues into the Sakarya Zone to the east. In contrast to permost Albian–Cenomanian interval. the Istanbul Zone (see Akyol et al., 1974 and Tüysüz et al., 2012),

Fig. 8. Borehole log for Fasıllı-1 well.

detailed stratigraphy of the Upper Cretaceous volcanic sequence in the breaking up of the continental crust, and by a thick Campanian Sakarya Zone have not been studied yet, and the whole unit is grouped volcanosedimentary unit. In the Istanbul Zone, in the vicinity of Cide into a single formation, the Yemişliçay Formation (Ketin and Gümüş, (Fig. 1b), badly sorted and angular Upper Barremian to Cenomanian 1963). In fact, the Late Santonian unconformity is a widespread event blocks and pebbles are present within the Middle Turonian pelagic sed- and had also been documented in the northern part of the Black Sea, iments of the Dereköy Formation. This phenomenon indicates intense in Crimea (Nikishin et al, 2015a, 2015b), in the Çankırı Basin of the erosion due to fast uplifting of the horsts (Tüysüz et al., 2012). Central Anatolia (Tüysüz and Dellaoğlu, 1992) and in the Haymana In the Istanbul Zone, sedimentation in the Zonguldak and Ulus basins Basin in the SW Sakarya Zone. Tüysüz et al. (2012) showed that the Is- began during the Late Barremian (Tüysüz,1999;Masseetal,2009), with tanbul Zone was affected by an intense normal faulting (rifting) period normal fault-controlled continental to shallow marine deposition, and that created a horst–graben topography during the Middle Turonian to initiated the development of a short-lived Urgonian-type carbonate plat- Early Santonian time. This extensional period is attributed to the period form along the northern parts of the Istanbul Zone during Late Barremian of the opening of Western Black Sea Basin. Uplifted areas by normal to Early Aptian times (Yılmaz and Altıner, 2007). Fast deepening of the faults (horst or rift shoulders) became emerged and were eroded at region as a result of the opening of the Zonguldak Basin caused the de- this time, but sedimentation was more or less continuous within the mise of this platform (Masse et al., 2009) and the filling of the basin grabens, where a disconformity corresponding to the Late Santonian with deepening upward siliciclastic sediments (Görür, 1997; Tüysüz, unconformity is obvious. All these units were covered first by thin but 1999; Hippolyte et al., 2010). The Ulus Basin to the south was filled main- widespread Upper Santonian pelagic micritic limestones of the Unaz ly by turbidites with debris flow horizons, olistoliths and some Formation, indicating sudden subsidence of the whole region due to hemipelagic mudstones, representing deeper part of the Zonguldak

Fig. 9. Planktic foraminifera from the Fasıllı-1 Well 1: Parathalmanninella appenninica,2,3— Rotalipora spp., 4 — Praeglobotruncana gibba,5— Heterohelix sp., 6–8 — Macroglobigerinelloides spp., 9 — Muricohedbergella cf. delrioensis,and10— Muricohedbergella sp.

Basin. Both basins were probably a southward dipping single basin, but 1931; Türkünal, 1962). Therefore, there is not any precise and reliable later on the overlying Devrek Tertiary Basin separated them. age data from the Istanbul Zone indicating the deposition of The Zonguldak and the Ulus basins were possibly affected by a latest Cenomanian sediments. The regional unconformity at the base of the Aptian continental collision to the south (Okay et al., 2006, 2013). Based Turonian–Coniacian Dereköy Formation (Tüysüz et al., 2012)alsoindi- on fossil data, there is no indication for deposits of Albian age in the Ulus cates an erosional period between the Late Albian and Turonian. Basin. This southern basin was probably uplifted and emerged during Data presented above show that marine sedimentation continued the Albian and Cenomanian. In contrast, deposits of the Zonguldak from the Late Barremian to the Late Albian in most parts of the Pontides. Basin provided nannofossils with Tranolithus orionatus (Tüysüz et al., The exception forms the westernmost part of the Istanbul Zone, that 1997) and dinocyst L. siphoniphorum (Hippolyte et al., 2010), and gave possibly remained emerged during the Late Jurassic–Late Santonian in- evidence for marine conditions in the Middle and Upper Albian. Except terval (see Tüysüz et al., 2012), but the most of this zone was emerged for the ammonite assemblage described by Tokay (1952), there is no during the Cenomanian. other fossil data from the Istanbul Zone supporting that this tectonic The litho- and biostratigraphy of the sections described in this paper unit was not emerged during the Cenomanian. Tokay (1952) assigned imply that, in contrast to the Istanbul Zone, deep marine conditions a Cenomanian age to the Tasmaca Formation (Fig. 2), based on the am- prevailed in the Sakarya Zone during the whole Albian–Turonian inter- monite species Schloenbachia inﬂata, Hoplites auritas and Scaphites val. Siliciclastic sedimentation in the Sinop Basin started during the hugardianum. The same ammonite assemblages from the Tasmaca For- Hauterivian (Hippolyte et al., 2010), earlier than in the Istanbul Zone, mation were originally attributed to the Late Albian interval (Arni, and no Urgonian carbonate platform developed before or during the

Please cite this article as: Tüysüz, O., et al., The Kapanboğazı formation: A key unit for understanding Late Cretaceous evolution of the Pontides, N Turkey, Palaeogeogr. Palaeoclimatol. Palaeoecol. (2015), http://dx.doi.org/10.1016/j.palaeo.2015.06.028 14 O. Tüysüz et al. / Palaeogeography, Palaeoclimatology, Palaeoecology xxx (2015) xxx–xxx early deposition interval (Hauterivian–Barremian) of the Çağlayan For- Tüysüz (1999, 2009) concluded that, regarding the facies difference mation. In contrast to the Istanbul Zone, the black shales and very fine of the Lower Cretaceous sediments in both zones and the age of the grained distal turbidites together with the radiolarian cherts in the up- Araç–Daday Shear Zone, the Intra-Pontide Ocean separating the Istanbul permost part of the Çağlayan Formation indicate that, the Sinop Basin and Sakarya zones was closing during the Albian–Cenomanian period, continued deepening during the Albian. The Cenomanian and Turonian definitely before the deposition of the Dereköy Formation (Middle radiolarian cherts indicate deep marine palaeoenvironment: the abyssal Turonian to Coniacian). Differences in the palaeoenvironmental setting zone. Deepening of the depositional areas within the Cenomanian– within the Albian up to the Cenomanian stratigraphic interval of the Is- Turonian interval documented by variegated radiolarian cherts was tanbul and Sakarya zones, indicated by the data presented in this paper, also reported from other Tethyan areas, i.e., the Outer Western supports this tectonic evolution scenario (Fig. 10). Carpathians, Poland (Bąk, 2007) and Czech Republic (Stráník et al., The Zonguldak and the Ulus basins probably existed as a single basin 1996; Skupien et al., 2009), the Eastern Carpathians, Romania in the Istanbul Zone (Fig. 10), and the depth of the basin increased to- (Melinte-Dobrinescu and Roban, 2011), the Middle East (Oman, wards the Intra-Pontide Ocean to the south. The Istanbul Zone collided Cowan et al., 2014) and many other regions. This change is coincident with the Sakarya Zone along the Intra-Pontide Suture during the late with the highest eustatic level of the Cretaceous recorded for the Albian and its southern part was metamorphosed and uplifted. The Is- Cenomanian–Turonian interval (Haq et al., 1987; Haq, 2014). tanbul Zone was emerged during the Cenomanian. The Sinop Basin de- The Istanbul and the Sakarya zones are separated by the Araç–Daday veloped in the Sakarya Zone reached its deepest stage during the Shear Zone, which is regarded as an eastern continuation of the Intra- Cenomanian and Turonian. The Pontide magmatic arc started to be ac- Pontide suture (Tüysüz, 1999). This zone is mainly formed by tive after the juxtaposition of the Istanbul and the Sakarya zones. Hauterivian to Albian turbidites, enclosing debris flow horizons and huge olistoliths of Upper Jurassic limestones, and tectonic slices of pil- 6. Conclusions low lava and radiolarian cherts. Chert slices alternating with basaltic lava contain radiolarian taxa of the Middle and Late Jurassic, Late Field observations and geological mapping during the past thirty- Bathonian to Callovian (Bragin et al., 2002), and Oxfordian (Kuru et al., five years, some results of which are summarized here, show that 1994) intervals. However, some of the magmatic rocks within this com- Cenomanian and Turonian deep marine sediments are present in the plex were dated as 137 Ma, thus being Early Cretaceous, Valanginian in Sakarya Zone. In contrast, pelagic sedimentary rocks of the same age age (Terzioğlu et al., 2000). The geochemistry of the Jurassic magmatic are absent in the Istanbul Zone because it was mainly emerged or locally rocks indicates their oceanic origin (Kibaroğlu and Satır, 2000; Tüysüz drowned by shallow marine waters. This assumption is supported by et al., 2000). This unit was affected by syn- and post-sedimentary defor- our multidisciplinary study including microbiostratigraphy, according mation and is regarded as an accretionary complex that developed to non-calcareous dinoflagellates, foraminifers, radiolarians and calcar- within the Intra-Pontide Ocean (Tüysüz, 1999; Tüysüz et al, 2000). eous nannofossils.

Fig. 10. Palinspastic palaeogeography of the Pontides from the Albian up to the Turonian. Red Vs indicate location of Pontide magmatic arc. (For interpretation of the references to colour in this ﬁgure legend, the reader is referred to the web version of this article.)

The Kapanboğazı Formation, originally defined by Ketin and Gümüş Biscutum ellipticum (Górka, 1957) Grün in Grün and Allemann, 1975 (1963), is lithostratigraphically redefined here. We recommend to Broinsonia enormis (Shumenko, 1968) Manivit, 1971 apply this term only to the Cenomanian and Turonian deep marine sed- Broinsonia signata (Noël, 1969) Noël, 1970 iments overlying the Hauterivian–Albian siliciclastic turbidites and Corollithion kennedyi Crux, 1981 black shales of the Çağlayan Formation, the latter being related to the Cretarhabdus striatus (Stradner, 1963) Black, 1973 rifting and deepening phase of the Sinop Basin (Görür, 1988; Tüysüz, Cribrosphaerella ehrenbergii (Arkhangelsky, 1912) Deflandre in 1993; Görür and Tüysüz, 1997; Leren, 2003; Leren et al., 2007; Espurt Piveteau, 1952 et al., 2014). A wider application of the term “Kapanboğazı Formation” Eiffellithus turriseiffelii (Deflandre in Deflandre and Fert, 1954) to various lithologic units, such as different red pelagic limestone levels, Eprolithus floralis (Stradner, 1962) Stover, 1966 as it was done in some previous studies (Gedik and Korkmaz, 1984; Eprolithus moratus (Stover, 1966) Burnett, 1998 Görür et al., 1993; Hippolyte et al., 2010; Okay et al., 2013), would result Eprolithus octopetalus Varol, 1992 in inappropriate structural and stratigraphic interpretations of the geo- Gartnerago nanum Thierstein, 1974 logical evolution of the Pontides, and should therefore be avoided. Gartnerago obliquum (Stradner, 1963) Noël, 1970 The changes from black to red deep marine sediments within the Gartnerago segmentatum (Stover, 1966) Thierstein, 1974 Albian–Cenomanian interval point to palaeoenvironmental fluctuations Gartnerago theta (Black in Black and Barnes, 1959) Jakubowski, 1986 in the Pontides during mid-Cretaceous time. Black shale deposition indi- Helenea chiastia Worsley, 1971 cates prevailing anoxic conditions during the Albian in the Sinop Basin, Isocrystallithus compactus Verbeek, 1976 while the occurrence of CORBs (Cretaceous Oceanic Red Beds; Hu et al., Lithraphidites acutus Verbeek and Manivit in Manivit et al. 1977 2009; Wagreich et al., 2009) mirrors a shift to oxic conditions in the Lithraphidites carniolensis Deflandre, 1963 Cenomanian–Turonian interval. Yet, alternating dark grey and red Manivitella pemmatoidea (Deflandre in Manivit, 1965) Thierstein, shales and cherts indicate a cyclicity of oxic and anoxic conditions dur- 1971 ing the Cenomanian, while an oxic setting prevailed in the Pontides Microrhabdulus decoratus Deflandre, 1959 after the Cenomanian–Turonian interval. The positive excursion of Nannoconus truitti Brönnimann, 1955 δ13C – the overprint of the Oceanic Anoxic Event 2 (OAE2) within the Placozygus fibuliformis (Reinhardt, 1964) Hoffmann, 1970 Cenomanian–Turonian interval – was identified in the Kayadibi section Prediscosphaera columnata (Stover, 1966) Perch-Nielsen, 1984 presented above (Yılmaz et al., 2010). Similar palaeoenvironmental Prediscosphaera cretacea (Arkhangelsky, 1912) Gartner, 1968 changes within the Albian–Cenomanian boundary interval, from black Prediscosphaera ponticula (Bukry, 1969) Perch-Nielsen, 1984 and dark-grey shales to CORBs has also been described in detail from Quadrum intermedium Varol, 1992 other Tethyan areas (Hu et al., 2005, 2012; Wagreich and Krenmayr, Retacapsa angustiforata Black, 1971 2005; Wang et al., 2009; Roban and Melinte-Dobrinescu, 2012; Retacapsa crenulata (Bramlette and Martini, 1964) Grün in Grün and Melinte-Dobrinescu et al., 2015,amongmanyothers). Allemann, 1975 Although the red colour of the Cretaceous deep marine sediments Rhagodiscus achlyostaurion (Hill, 1976) Doeven, 1983 has mainly been attributed to the climatic changes so far, at least for Rhagodiscus angustus (Stradner 1963) Reinhardt 1971 the Cretaceous sediments, previous studies from the Pontides show Rhagodiscus asper (Stradner 1963) Reinhardt 1967 that the volcanism was one of the controlling mechanisms of the depo- Tranolithus gabalus Stover, 1966 sition of such strata (Tüysüz et al., 2012). In addition to this, in the Tranoltithus orionatus (Reinhardt, 1966a) Reinhardt, 1966b Yenipazar region (SW Sakarya Zone) the Upper Cenomanian pyroclastic Watznaueria barnesiae (Black, 1959) Perch-Nielsen, 1968 succession directly below the Cenomanian–Turonian boundary (Yılmaz Watznaueria biporta Bukry, 1969 et al., 2010) could have contributed to the deposition of red coloured Watznaueria ovata Bukry, 1969 beds. Zeugrhabdothus bicrescenticus (Stover, 1966) Burnett in Gale et al. As discussed above, in the Middle Turonian to Campanian 1996 volcanosedimentary formations, many red pelagic limestone/shale horizons alternate with the volcanic and volcanogenic sediments. Two of Appendix B. List of non-calcareous dinoflagellte cyst mentioned in thesehorizons,theKapanboğazı and the Unaz formations were possibly the text, in alphabetical order of genera epithets not affected by volcanism. There is no direct evidence of volcanism before the Middle Turonian in the Pontides indicating a connection of the Achomosphaera neptunii (Eisenack, 1958a) Davey and Williams, red colour of the sediments of the Kapanboğazı Formation with magmat- 1966 ic activity; hence, we assume that in this interval the deposition of CORBs Achomosphaera ramulifera (Deflandre, 1937b) Evitt, 1963 is linked to the anoxic to oxic mid-Cretaceous palaeoceanographic Callaiosphaeridium asymmetricum (Deflandre and Courteville, 1939) changes (Wang et al., 2009; Hu et al., 2012). Davey and Williams, 1966 Canningia sp. Acknowledgements Cauca parva (Alberti, 1961) Davey and Verdier, 1971 Cerbia tabulata (Davey and Verdier, 1974) Below, 1981 This study is a contribution to the UNESCO/IUGS IGCP Project 609 Chlamydophorella nyei Cookson and Eisenack, 1958 ‘Climate-environmental deteriorations during greenhouse phases: Chlamydophorella sp. Causes and consequences of short-term Cretaceous sea-level changes’. Circulodinium distinctum (Deflandre andCookson, 1955) Jansonius, We also thank the Turkish Petroleum Company for supporting field 1986 studies of Okan Tüysüz and Sabri Kirici. We also thank two anonymous Circulodinium sp. reviewers, and editors of this special publication, Michael Wagreich and Cribroperidinium sp. Benjamin Sames. Cleistosphaeridium? multispinosum (C. Singh, 1964) Brideaux, 1971 Coronifera oceanica Cookson and Eisenack, 1958 Appendix A. List of calcareous nannofossils mentioned in the text, Cyclonephelium paucimarginatum Cookson and Eisenack, 1962b in alphabetical order of genera epithets Dapsilidinium warrenii (Habib, 1976) Lentin and Williams, 1981 Dissiliodinium globulus Drugg, 1978 Axopodorhabdus albianus (Black, 1967) Wind and Wise in Wise and Endoscrinium campanula (Gocht, 1959) Vozzhennikova, 1967 Wind, 1977 Endoscrinium sp.

Florentinia laciniata Davey and Verdier, 1973 and Rize regions). Unpublished PhD Thesis (In Turkish), Istanbul Technical University, Istanbul, 112 pp. Florentinia radiculata (Davey and Williams, 1966) Davey and Cowan, R.J., Searle, M.P., Waters, D.J., 2014. Structure of the metamorphic sole of the Verdier, 1973 Oman Ophiolite, Sumeini Window and Wadi Tayyin: implications for ophiolite Florentinia stellata (Maier, 1959) Below, 1981 obduction processes. In: Rollinson, H.R., Searle, M.P., Abbasi, I.A., Al-Lazki, A., fl Al-Kindi, M.H. (Eds.), Tectonic Evolution of the Oman Mountains. Geological Society Hystrichodinium pulchrum De andre, 1935 Special Publication 392, pp. 155–177. Kiokansium polypes Tasch, 1964 Demirer, A., Kirici, S., 1996. Boyabat Baseni'nde açılan Fasılı-1, Akveren-1, Soğuksu-1, Kleithriasphaeridium sp. Erfelek-1, Boyabat-1, Boyabat-2, Boyabat-3, Boyabat-4 ve Ekinveren-1 kuyularının fi ı ı ğ Litosphaeridium siphoniphorum (Cookson and Eisenack, 1958) Davey stratigra si. Stratigraphy of the Fas l -1,Akveren-1,So uksu-1, Erfelek-1, Boyabat-1, Boyabat-2, Boyabat-3, Boyabat-4 and Ekinveren-1 wells that drilled in the Boyabat and Williams, 1966 Basin. Turkish Petroleum Co. Internal Report, No: 2173. p. 24 (In Turkish). Odontochitina costata (Wetzel, 1933) Deflandre and Cookson, 1955 Espurt, N., Hippolyte, J.C., Kaymakcı, N., Sangu, E., 2014. Litospheric structural control on Odontochitina operculata (Wetzel, 1933) Deflandre and Cookson, inversion of the southern margin of the Black Sea Basin, Central Pontides, Turkey. Litosphere 6 (1), 26–34. 1955 Gedik, A., Korkmaz, S., 1984. Sinop havzasının jeolojisi ve petrol olanakları (Geology and Oligosphaeridium? asterigerum (Gocht, 1959) Davey and Williams, petroleum potential of the Sinop Basin). J. Geol. Eng. 19, 53–79 (In Turkish). 1969 Görür, N., 1988. Timing of opening of the Black Sea basin. Tectonophysics 147, 247–262. Görür, N., 1997. Cretaceous syn- to postrift sedimentation on the southern continental Oligosphaeridium complex (White, 1842) Davey and Williams, 1969 margin of the Western Black Sea Basin. In: Robinson, A.G. (Ed.), Regional and Palaeohystrichophora infusorioides Deflandre, 1935 Petroleum Geology of the Black Sea and Surrounding Region. AAPG Memoir 68, Palaeoperidinium cretaceum Pocock, 1962 pp. 227–240. fl Görür, N., Tüysüz, O., 1997. Petroleum geology of the southern continental margin of the Pervosphaeridium pseudhystrichodinium (De andre, 1937) Yun, 1981 Black Sea. In: Robinson, A.G. (Ed.), Regional and Petroleum Geology of the Black Sea Pervosphaeridium sp. and Surrounding Region. AAPG Memoir 68, pp. 241–254. Spiniferites ramosus (Ehrenberg, 1838) Mantell, 1854 Görür, N., Tüysüz, O., Aykol, A., Sakınç, M., Yiğitbaş, E., Akkök, R., 1993. Cretaceous red pelagic carbonates of northern Turkey: their place in the opening history of the Black Spiniferites sp. Sea. Eclogae Geol. Helv. 86 (3), 819–838. Subtilisphaera perlucida (Alberti, 1959b) Jain and Millepied, 1973 Güner, M., 1980. Küre civarının masif sülfit yatakları ve jeolojisi, Pontidler (Kuzey Subtilisphaera sp. Türkiye) (Geology of the massive sulphide deposits of Küre region, Pontides, N Surculosphaeridium? longifurcatum (Firtion, 1952) Davey et al., 1966 Turkey) Bulletin of General Directorate of the Mineral Research and Exploration. 93/94 pp. 65–109. Systematophora cretacea Davey, 1979 Haq, B.U., 2014. Cretaceous eustacy revisited. Glob. Planet. Chang. 113, 44–58. Systestaphora sp. Haq, B.U., Hardenbol, J., Vail, P.R., 1987. Chronology of fluctuating sea levels since the – Tanyosphaeridium isocalamus (Deflandre and Cookson, 1955) Davey Triassic. Science 235, 1156 1167. Hardas, P., Mutterlose, J., 2006. Calcareous nannofossil biostratigraphy of the and Williams, 1969 Cenomanian/Turonian boundary interval of ODP Leg 207 at the Demerara Rise. Rev. Tehamadinium tenuiceras (Eisenack, 1958) Jan du Chêne et al., 1986 Micropaleontol. 49, 165–179. Trichodinium sp. Hippolyte, J.C., Müller, C., Kaymakci, N., Sangu, E., 2010. Dating of the Black Sea Basin: new nannoplankton ages from its inverted margin in the Central Pontides (Turkey). In: Wallodinium krutzschii (Alberti, 1961) Habib, 1972 Stephenson, R.A., Kaymakci, N., Sosson, M., Starostenko, V., Bergerat, F. (Eds.), Sedi- mentary Basin Tectonics from the Black Sea and Caucasus to the Arabian Platform. Geological Society London, Special Publications 340, pp. 113–136. References Hu, X.M., Jansa, L., Wang, C.S., Sarti, M., Bak, K., Wagreich, M., Michalik, J., Sotak, J., 2005. Upper Cretaceous oceanic red beds (CORBs) in the Tethys: occurrences, lithofacies, Akın, H., 1978. Geologie, Magmatismus und Lagerstättenbildung im ostpontischen age, and environments. Cretac. Res. 26, 3–20. Gebirge/Türkei aus Sicht der Plattentektonik. Geol. Rundsch. 68, 253–283. Hu, X.M., Wang, C., Scott, R.W., Wagreich, M., Jansa, L., 2009. Cretaceous Oceanic Red Beds: Akıncı, Ö.T., 1984. The Eastern Pontide volcano–sedimentary belt and associated massive stratigraphy, composition, origins, and paleoceanographic and paleoclimatologic sig- sulphide deposits. In: Dixon, J.E., Robertson, A.H.F. (Eds.), The Geological Evolution nificance. SEPM Spec. Publ. 91 (276 pp). of the Eastern Mediterranean. Geological Society Special Publication 17, pp. 415–428. Hu, X., Scott, R., Cai, Y., Wang, C., Melinte-Dobrinescu, M., 2012. Cretaceous Oceanic Red Akyol, Z., Arpat, E., Erdoğan, B., Göğer, E., Şaroğlu, F., Şentürk, İ., Tütüncü, K., Uysal, Ş., Beds (CORBs): different time scales, different origin models. Earth-Sci. Rev. 115, 1974. Cide–Kurucaşile dolayının jeoloji haritası (Geology Map of Cide–Kurucaşile 217–248. and surroundings). General Directorate of Mineral Research and Exploration, Series Karacık, Z., Tüysüz, O., 2010. Petrogenesis of the Late Cretaceous Demirköy Igneous Com- of 1:50.000 scale Geology map of Turkey, Ankara (Explanation in Turkish). plex in the NW Turkey: implications for magma genesis in the Strandja Zone. Lithos Arni, P., 1931. Zur Stratigraphie und Tektonik der Kreideschichten östlich Ereğli an der 114 (3–4), 369–384. Schwarzmeerküste. Eclogae Geol. Helv. 24, 305–345. Keskin, M., Tüysüz, O., 1999. Geochemical evidence for nature and evolution of the rift Atlas of Late Cretaceous Globotruncanids. In: Robaszynski, F., Caron, M., Gonzales Donoso, volcanism related to opening of the Black Sea, Central Pontides, Turkey. J. Conf. J.M., Wonders, A.H. (Eds.), Rev. Micropaleontol. 26, 145–305. Abstr. EUG vol. 4 (1), 816. Aydın, Y., 1982. YıldızDağları (Istranca) Masifinin Jeolojisi (Geology of Yıldız–Istranca Keskin, M., Tüysüz, O., 2001. Interaction between magmas derived from diverse litho- Mountains). Unpublished Docentus Thesis, Istanbul Technical University, Faculty of spheric and asthenospheric sources during the opening of the Black Sea, Western Mines, Istanbul, Turkey, 107 p. (In Turkish). Pontides, Turkey. Fourth International Turkish Geology Symposium. Work in Progress Aydın,M.,Demir,O.,Özçelik,Y.,Terzioğlu, N., Satır, M., 1995. Geological revision on the Geology of Turkey and Its Surroundings, Abstracts, p. 119. of Inebolu, Devrekani, Ağlı, and Küre areas: new observations in PaleoTethys– Keskin, M., Ustaömer, T., Yeniyol, M., 2003. İstanbul kuzeyinde yüzeylenen Üst Kretase yaşlı NeoTethys sedimentary successions. In: Erler, A., Ercan, T., Bingöl, E., Örçen, S. volkano–sedimenter birimlerin stratigrafisi, petrolojisi ve tektonik ortamı (Stratigra- (Eds.), Geology of the Black Sea Region. Directorate of the Mineral Research and phy, petrology and tectonic environment of Upper Cretaceous volcano–sedimentary Exploration, Ankara, pp. 33–38. units cropping out in the north of Istanbul). İstanbul'un Jeolojisi Sempozyumu Aykol, A., Tokel, S., 1991. The geochemistry and tectonic setting of the Demirköy–Istranca pp. 23–35 (in Turkish). granitoid chain, NW Turkey. Mineral. Mag. 55, 249–256. Ketin, İ., 1966. Anadolu'nun tektonik birlikleri (Tectonic Units of Asia minor). Bulletin of Di- Bąk, K., 2007. Deep-water facies succession around the Cenomanian/Turonian boundary rectorate of the Mineral Research and Exploration, Ankara 66 pp. 20–34 (in Turkish). in the Outer Carpathian basin: sedimentary, biotic and chemical records in the Ketin, İ., Gümüş, A., 1963. Sinop–Ayancık güneyinde üçüncü bölgeye dahil sahaların Silesian Nappe, Poland. Palaeogeogr. Palaeoclimatol. Palaeoecol. 248, 255–290. jeolojisi hakkında rapor (2.Kısım: Jura ve Kretase formasyonlarının etüdü) (Report Berza, T., Constantinescu, E., Vlad, S.N., 1998. Upper-Cretaceous magmatic series and asso- on the geology of district-III to the south of Sinop–Ayancık, (Part-2: Jurassic and Cre- ciated mineralization in the Carpathian–Balkan orogen. Resour. Geol. 48 (4), 291–306. taceous formations)). Turkish Petroleum Co. Internal Report. 288 p. 33 (in Turkish). Bouma, A.H., 1962. Sedimentology of some flysch deposits. A Graphic Approach to Facies Kibaroğlu, M., Satır, M., 2000. Geochemistry of basaltic rocks af the Küre–Ophiolitic Com- Interpretation. Elsevier, Amsterdam (160 pp). plex and volcanics of Kervansaray, Central Pontides, Northern Turkey. Abstract in Bragin, N.Yu., Tekin, U.K., Özçelik, Y., 2002. Middle Jurassic Radiolarians from the Akgöl IESCA 2000, İzmir p. 109. Formation, Central Pontides, northern Turkey. Neues Jb. Geol. Paläontol. Monat. 10, Kirici, S., Güran, H.Ö., Yılmaz, E., Geyikçioğlu, B., Alay, Z., 2011. Petrography, sedimentolo- 609–628. gy, biostratigraphy and reservior characteristics of the Upper Cretaceus–Early Eocene Burnett, J.A., 1998. Upper Cretaceous. In: Bown, P.R. (Ed.), Calcareous Nannofossil Biostra- carbonates, central Pontides Black Sea area (Seydiler–Devrekani–Taşköprü/ tigraphy, British Micropalaeontological Society Publication Series. Chapman and Hall Kastamonu field). Turkish Petroleum Co. Internal Report. No: 3609p. 236 (in Turkish). Ltd/Kluwer Academic Press, London, pp. 132–199. Kuru, F., Bragin, N.Y., Özçelik, Y., 1994. Radiolarian biostratigraphy of Jurassic–Cretaceous Caron, M., 1985. Cretaceous Planktic Foraminifera. In: Bolli, H.M., Saunders, J.B., Perch- units in the Western Black Sea Region. Turkish Petroleum Co. Internal Report Nilsen, K. (Eds.), Cambridge Earth Science SeriesPlankton Stratigraphy. Cambridge 2015p. 29 (in Turkish). University Press, pp. 17–86. Leren, B.L.S., 2003. Late Cretaceous to Early Eocene Sedimentation in the Sinop–Boyabat Çoğulu, E., 1975. Gümüşhane ve Rize granitik plütonlarının mukayeseli petrografikve Basin, North-Central Turkey: Facies Analysis of Turbiditic to Shallow Marine Deposits. jeokronometrik etüdü (Petrological and geochronological studies in the Gümüşhane Unpublished Cand. Scient. Thesis, University of Bergen, 140 pp.

Leren, B.L.S., Janbu, N.E., Nemec, W., Kırman, E., Ilgar, A., 2007. Late Cretaceous to Early Skupien, P., Bubík, M., Švábenická, L., Mikuláš, R., Vašíček, Z., Matýsek, D., 2009. Creta- Eocene sedimentation in the Sinop–Boyabat Basin, north-central Turkey: a deep- ceous Oceanic Red Beds in the Outer Western Carpathians of the Czech Republic. water turbiditic system evolving into littoral carbonate platform. In: Nichols, G., In: Hu, X., Wang, C., Scott, R.W., Wagreich, M., Jansa, L. (Eds.), Cretaceous Oceanic Williams, E.A., Paola, C. (Eds.), Sedimentary Processes. Environments and Basins: A Red Beds: Stratigraphy, Composition, Origins, and Paleoceanographic and Paleocli- Tribute to Peter Friend. IAS Special Publication 38, pp. 401–456. matic Significance. SEPM Special publication 91, pp. 99–109. Luo, H., 2005. Radiolarians from Upper Cretaceous oceanic red beds in Sinop basin, north- Stráník, Z., Bubík, M., Čech, S., Švábenická, L., 1996. The Upper Cretaceous in South Mora- ern Turkey. Earth Sci. Front. 12 (2), 45–50 (In Chinese with English abstract). via. Věstnik Českého geologického ústavu 71 (1), 1–30. Masse, J.P., Tüysüz, O., Fenerci-Masse, M., Özer, S., Sarı, B., 2009. Stratigraphic organisa- Sunal, G., Tüysüz, O., 2002. Palaeostress analysis of Tertiary post-collisional structures in tion, spatial distribution, palaeoenvironmental reconstruction, and demise of Lower the Western Pontides, Northern Turkey. Geol. Mag. 139 (3), 343–359. Cretaceous (Barremian–lower Aptian) carbonate platforms of the Western Pontides Švábenická, L., 2012. Nannofossil record across the Cenomanian–Coniacian interval in the (Black Sea region, Turkey). Cretac. Res. 30 (5), 1170–1180. Bohemian Cretaceous Basin and Tethyan foreland basins (Outer Western Carpathians), Melinte-Dobrinescu, M.C., Roban, R.D., 2011. Cretaceous oxic–anoxic changes in the Czech Republic. Geol. Carpath. 63, 201–217. Romanian Carpathians. Sediment. Geol. 235, 79–90. Terzioğlu, M.N., Satır, M., Saka, K., 2000. Geochemistry and geochronology of basaltic Melinte-Dobrinescu, M.C., Bernandez, E., Kaiho, K., Lamolda, M.A., 2013. Cretaceous Oce- rocks of Küre basin, Central Pontides (N Turkey). Abstract in IESCA 2000, İzmir. 219. anic Anoxic Event 2 in the Arobes section, northern Spain: calcareous nannofossil Tokay, M., 1952. Karadeniz Ereğlisi–Alaplı–Kızıltepe–Alacaağız Bölgesi jeolojisi (Contribu- fluctuations and isotopic events. In: Bojar, A.V., Melinte-Dobrinescu, M.C., Smit, J. tion à l'étude géeologique de la région comprise entre Ereğli, Alaplı,Kızıltepe et (Eds.), Isotopic Studies in Cretaceous Research. Geological Society, London, Special Alacaağzı). MTA Dergisi 42/43pp. 35–78 (In French with Turkish Abstract). Publication 382, pp. 82–98. Türkünal, M., 1962. Türkiye'de Ammonit Faunasıİhtiva Eden Lokaliteler Hakkında Not — Melinte-Dobrinescu, M.C., Roban, R.D., Stoica, M., 2015. Palaeoenvironmental changes Kısım II: Kuzey Anadolu Bölgesi İle Bazı Münferit Lokaliteler (A report on the ammo- across the Albian–Cenomanian boundary interval of the Eastern Carpathians. Cretac. nite bearing regions of Turkey. Part II: North Anatolia and some individual outcrops). Res. 54, 68–85. Bull. Mineral Res. Explor. Inst. Turk. 59, 107–122 (in Turkish). Moore, W.J., McKee, E.H., Akıncı, Ö., 1980. Chemistry and chronology of plutonic rocks in Tüysüz, O., 1990. Tectonic evolution of a part of the Tethyside orogenic collage: the Kargı the Pontide mountains, northern Turkey: Symposium on the European copper de- massif, Northern Turkey. Tectonics 9 (1), 141–216. posits: Belgrade, Yugoslavia. pp. 209–216. Tüysüz, O., 1993. Karadeniz'den Orta Anadolu'ya bir Jeotravers: Kuzey Neo-Tetisin Nikishin, A.M., Okay, A.I., Tüysüz, O., Demirer, A., Amelin, N., Petrov, E., 2015a. The Black Tektonik evrimi. Turk. Assoc. Pet. Geol. Bull. 5 (1), 1–33 (in Turkish with English Sea basins structure and history: new model based on new deep penetration regional abstract). seismic data. Part 1: Basins structure and fill. Mar. Pet. Geol. 59, 638–655. Tüysüz, O., 1999. Geology of the Cretaceous sedimentary basins of the Western Pontides. Nikishin, A.M., Okay, A.I., Tüysüz, O., Demirer, A., Wannier, M., Amelin, N., Petrov, E., Geol. J. 34, 75–93. 2015b. The Black Sea basins structure and history: New model based on new deep Tüysüz, O., 2009. A new approach to the tectonic evolution of the Pontides. IPETGAS 2009 penetration regional seismic data. Part 2: Tectonic history and paleogeography. 17th International Petroleum and Natural Gas Congress and Exhibition of Turkey, Mar. Pet. Geol. 59, 656–670. May 13th–15th, 2009 Proceedings Book, pp. 20–24. Ohta, E., Doğan, R., Batık, H., Abe, M., 1988. Geology and mineralization of Dereköy Porphyry Tüysüz, O., Dellaloğlu, A.A., 1992. Çankırı havzasının tektonik birlikleri ve jeolojik evrimi copper deposits, northern Thrace, Turkey. Bull. Geol. Surv. Jpn. 39 (2), 115–134. (Tectonic Units and Geological Evolution of the Çankırı Basin). 9th Petroleum Okay, A.İ., 1989. Tectonic units and sutures in the Pontides, northern Turkey. In: Şengör, Congress of Turkey, Chamber of Petroleum Geologists and Chamber of Petroleum A.M.C. (Ed.), Tectonic Evolution of the Tethyan Region. Kluwer Academic Publ., Engineers, Ankara, Presentations, Geology, pp. 333–349 (in Turkish). pp. 109–116. Tüysüz, O., Kirici, S., Sunal, G., 1997. Geology of Cide–Kurucaşile Region. Turkish Okay, A.İ., Tüysüz, O., 1999. Tethyan sutures of northern Turkey. In: Durand, B., Jolivet, L., Petroleum Co. Internal Report No: 3736p. 127 (in Turkish). Hovarth, F., Séranne, M. (Eds.), The Mediterranean Basins: Tertiary Extension within Tüysüz, O., Keskin, M., Natalin, B., Sunal, G., 2000. Geology of İnebolu–Ağlı–Azdavay the Alpine Orogen. Geological Soc. London Spec. Publ. 156, pp. 475– 515. Region. Turkish Petroleum Co. Internal Report No: 4250p. 240 (in Turkish). Okay, A.İ., Tüysüz, O., Satır, M., Özkan-Altıner, S., Altıner, D., Sherlock, S., Eren, R.H., 2006. Tüysüz, O., Aksay, A., Yiğitbaş, E., 2004. Batı Karadeniz Bölgesi Litostratigrafi Birimleri. Cretaceous and Triassic subduction–accretion, HP/LT metamorphism and continental (Stratigraphic Nomenclature of the Western Black Sea Region, General Directorate growth in the Central Pontides, Turkey. Geol. Soc. Am. Bull. 118 (9/10), 1247–1269. of Mineral Research, Ankara). Maden Tetkik ve Arama Genel Müdürlüğü, Stratigrafi Okay, A.İ., Sunal, G., Sherlock, S., Altıner, D., Tüysüz, O., Kylander-Clark, A.R.C., Aygül, M., Komitesi Litostratigrafi Birimleri Serisi-1, Ankara p. 92 (in Turkish). 2013. Early Cretaceous sedimentation and orogeny on the active margin of Eurasia: Tüysüz, O., Yılmaz, İ.Ö., Š vabenická, L., Kirici, S., 2012. The Unaz Formation: a key unit in Southern Central Pontides, Turkey. Tectonics 32, 1–25. the Western Black Sea Region, N Turkey. Turk. J. Earth Sci. 21, 1009–1028. Okay, A.İ., Sunal, G., Tüysüz, O., Sherlock, S., Keskin, M., Kylander, R.C., 2014. Low pres- von Quadt, A., Moritz, R., Peytcheva, I., Heinrich, C.A., 2005. Geochronology and sure–high temperature metamorphism during extension in a Jurassic magmatic arc, geodynamics of Late Cretaceous magmatism and Cu–Au mineralization in the Central Pontides, Turkey. J. Metamorph. Geol. 32, 49–69. Panagyurishte region of the Apuseni–Banat–Timok–Srednogorie belt, Bulgaria. Ore Paul, C.R.C., Lamolda, M.A., Mitchell, S.F., Vaziri, M.R., Gorostidi, A., Marshall, J.D., 1999. The Geol. Rev. 27, 95–126. Cenomanian–Turonian boundary at Eastbourne (Sussex, UK): a proposed European Wagreich, M., Krenmayr, H.G., 2005. Upper Cretaceous oceanic red beds (CORB) in the reference section. Palaeogeogr. Palaeoclimatol. Palaeoecol. 150, 83–121. Northern Calcareous Alps (Nierental Formation, Austria): slope topography and clas- Perch-Nielsen, K., 1985. Mesozoic calcareous nannofossils. In: Bolli, H.M., Saunders, J.B., tic input as primary controlling factors. Cretac. Res. 26, 57–64. Perch-Nielsen, K. (Eds.), Plankton Stratigraphy. Cambridge University Press, Wagreich, M., Bojar, A.V., Sachsenhofer, R.F., Neuhuber, S., Egger, H., 2008. Calcareous Cambridge, pp. 329–426. nannoplankton, planktonic foraminiferal, and carbonate carbon isotope stratigraphy Postuma, J.A., 1971. Manual of Planktonic Cretaceous Foraminifera. Elsevier Publ. Co., of the Cenomanian–Turonian boundary section in the Ultrahelvetic Zone (Eastern Amsterdam (420 pp). Alps, Upper Austria). Cretac. Res. 29, 965–975. Premoli Silva, I., Verga, D., 2004. Practical manual of Cretaceous foraminifera. Course 3. In: Wagreich, M., Neuhuber, S., Egger, H., Wendler, I., Scott, R., Malata, E., Sanders, D., 2009. Verga, D., Rettori, R. (Eds.), International School on Planktonic Foraminifera. Univer- Cretaceous oceanıc red beds (CORBs) in the Austrian Eastern Alps: passive-margin sities of Perugia and Milan, Tipografia Pontefelcino, Perugia (283 pp). vs. active-margin depositional settings. SEPM Spec. Publ. 91, 73–88. Roban, R.D., Melinte-Dobrinescu, M.C., 2012. Lower Cretaceous lithofacies of the black Wang, C., Hu, X., Huang, Y., Scott, R.W., Wagreich, M., 2009. Overview of cretaceous oce- shales rich Audia Formation, Tarcău Nappe, Eastern Carpathians: genetic significance anic red beds (CORBs): a window on global oceanic and climate change. SEPM Spec. and sedimentary palaeoenvironments. Cretac. Res. 38, 52–67. Publ. 91, 13–33. Robaszynski, F., Caron, M., The European Working Group on Planktonic Foraminifera Yiğitbaş, E., Tüysüz, O., Serdar, H.S., 1990. Orta Pontidlerde Üst Kretase yaşlı aktif kıta (Eds.), 1979. Atlas of Mid Cretaceous planktonic Foraminifera (Boreal Sea and Te- kenarının jeolojik özellikleri (Geology of Late Cretaceous active continental margin thys), Parts 1-2, Cahiers de Micropaléentologie 366p, 80 pl. in Central Pontides). 8th Petroleum Congress of Turkey, Chamber of Petroleum Geol- Roth, P.H., Krumbach, K.R., 1986. Middle Cretaceous calcareous nannofossil biogeography ogists and Chamber of Petroleum Engineers, Ankara, PresentationsGeology and preservation in the Atlantic and Indian oceans: implications for palaeoceanography. pp. 141–151(inTurkishwithEnglishabstract). Mar. Micropaleontol. 10, 235–266. Yılmaz, İ.Ö., Altıner, D., 2007. Cyclostratigraphy and sequence boundaries of inner plat- Şahin, S.Y., Aysal, N., Güngör, Y., 2012. Petrogenesis of Late Cretaceous adakitic form mixed carbonate–siliciclastic successions (Barremian–Aptian) (Zonguldak, magmatism in the İstanbul Zone (Çavuşbaşı Granodiorite, NW Turkey). Turk. NW Turkey). J. Asian Earth Sci. 30, 253–270. J. Earth Sci. 21, 1029–1045. Yılmaz, İ.Ö., Altıner, D., Tekin, U.K., Tüysüz, O., Ocakoğlu, F., Açıkalın, S., 2010. Şengör, A.M.C., Yılmaz, Y., 1981. Tethyan evolution of Turkey: a plate tectonic approach. Cenomanian–Turonian Oceanic Anoxic Event (OAE2) in the Sakarya Zone, north- Tectonophysics 75, 181–241. western Turkey: sedimentological, cyclostratigraphical and geochemical records. Skupien, P., 2003. Dinoflagellate study of the Lower Cretaceous deposits in the Pieniny Cretac. Res. 31 (2), 207–226. Klippen Belt (Rochovica section, Slovak Western Carpathians). Bull. Czech Geol. Surv. 78 (1), 67–82.