Planktonic foraminifera and calcareous nannofossils record in the upper Campanian-Maastrichtian pelagic deposits of the Malatya Basin in the Hekimhan area (NW Malatya, eastern Anatolia)

Cretaceous Research 61 (2016) 91e107

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Planktonic foraminifera and calcareous nannofossils record in the upper Campanian-Maastrichtian pelagic deposits of the Malatya Basin in the Hekimhan area (NW Malatya, eastern Anatolia) Bilal Sarı a, *, Ays¸egül Yıldız b, Taner Korkmaz c, Maria Rose Petrizzo d _ Dokuz Eylül University, Engineering Faculty, Department of Geological Engineering, Tınaztepe Campus, 35160 Buca, Izmir, Turkey Aksaray University, Engineering Faculty, Department of Geological Engineering, Aksaray, Turkey c Department of Mineral Research and Exploration, General Directorate of Mineral Research and Exploration (MTA), 06520 Ankara, Turkey d Department of Earth Sciences ‘Ardito Desio’, University of Milan, Via L. Mangiagalli 34, 20133 Milano, Italy a

b

a r t i c l e i n f o

a b s t r a c t

Article history: Received 27 August 2015 Received in revised form 15 December 2015 Accepted in revised form 22 December 2015 Available online xxx

The uppermost Cretaceous (upper Campanian-Maastrichtian) pelagic successions from the Malatya Basin (NW Malatya, eastern Anatolia) were studied by 688 samples, which were collected from five stratigraphic sections in the Hekimhan area. The pelagic deposits conformably overlie rudist bearing shallowwater limestones and are overlain conformably by Maastrichtian dolomites and unconformably by Paleocene-Eocene deposits, respectively. €sehasan Formation at the base and the The pelagic successions in the Hekimhan area comprise the Ko € sehasan Formation rests over Zorbehan Formation at the top and reach up to 1100 m in thickness. The Ko the neritic rudist-bearing limestones of the Güzelyurt Formation along a sharp contact and consists mainly of flysch-type sandstone-mudstone alternation with complete and partial Bouma sequences. The carbonate content of abundant planktonic foraminifera and nannoplankton-bearing 980-m-thick succession increases upwards and the formation passes gradually to the clayey limestones and marlstones of the Zorbehan Formation to the top. Occurrences of nannoplankton Lithraphidites quadratus Bramlette and € sehasan Formation indicate that the age Martini and Micula praemurus (Bukry) in the first beds of the Ko € sehasan Formation and overlying Zorbehan Formation is of late Maasthrichtian. Another late of the Ko Maastrichtian taxa Cribrosphaerella daniae Perch-Nielsen and Arkhangelskiella maastrichtiana Burnett are observed from the lowermost part of the succession. Maastrichtian planktonic foraminifera such as Contusotruncana walfischensis (Todd) and Globotruncanita pettersi (Gandolfi) were recorded through the € sehesan successions. Although planktonic foraminifera are diverse and abundant particularly in the Ko Formation, index late Maasthrichtian species were not encountered. Campanian and SantonianCampanian planktonic foraminifera, e.g. Radotruncana calcarata (Cushman) and Globotruncanita elevata (Brotzen), obtained particularly from the lower part of the succession and calcareous nannofossils such as Broinsonia parca parca Bukry, Reinhardtites anthophorus (Deflanre) and Eiffellithus eximius (Stover) are interpreted as reworked from older strata. Trace fossils are common throughout the succession. Rareness of planktonic foraminifera and nannoplankton in the uppermost part of the succession (Zorbehan Formation) indicates maximum shallowing of the latest Maastrichtian sea in this part of the basin. Rare echinoids, bivalves and ammonites are observed in that part of the sequence. The obtained data indicate that sediment accumulation rate of the pelagic deposits is rather high and about 27.5 cm/ky for this part of the basin. Changes in thickness of the formations along short distances in the five stratigraphic sections analysed in this study should be related to the diachroneity of the depositional and erosional events. © 2015 Elsevier Ltd. All rights reserved.

Keywords: Planktonic foraminifera Calcareous nannofossil Campanian-Maastrichtian Hekimhan Malatya Basin Eastern Anatolia

* Corresponding author. E-mail address: [email protected] (B. Sarı). http://dx.doi.org/10.1016/j.cretres.2015.12.012 0195-6671/© 2015 Elsevier Ltd. All rights reserved.

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1. Introduction The Malatya Basin corresponds to the eastern part of the Anatolide-Tauride block and was tectonically affected by the convergence of the Pontides, the Anatolide-Tauride and the Arabian platforms during the Late Cretaceous-Paleocene time interval (Fig. 1). Widespread Campanian-Maastrichtian deposits were accumulated in various basins within the Neotethys Ocean € r and Kidd, system shaped by convergent plate movements (S¸engo € r and Yılmaz, 1981; Yazgan, 1984; Aktas¸ and 1979; S¸engo Robertson, 1984; Yazgan and Chessex, 1991; Gürer, 1992, 1994; € €zübol, 1992; Yılmaz, 1993; Aksoy et al., 2005; Onal and Go Gürbüz and Gül, 2005; Booth et al., 2014). Volcanic arcs and several back-arc and foreland basins developed in response to the northward subduction during the Late Cretaceous-Paleocene € r and Yılmaz, 1981; Yazgan, 1984; Aktas¸ and Robertson, (S¸engo

1984, 1990; Robertson, 2000; Aksoy et al., 2005). According to the studies above, ophiolites were emplaced southwards onto the northern edge of the Tauride-Anatolide continent during the latest Cretaceous. The Upper Cretaceous rocks in the Hekimhan area were classified as deposits of a ‘supra-ophiolite basin’ (namely the Hekimhan Basin) by Booth et al. (2014) as the sedimentary deposits lay on extensive ophiolitic rocks. According to Booth et al. (2014), the basin developed as part of the northern margin of the Tauride microcontinent during the collision and suturing of the two Neotethyan oceans to the north, namely the Inner Tauride _ Ocean and the Izmir-Ankara-Erzincan Ocean, respectively. On the contrary, Gürer (1992, 1994) claimed that the upper CampanianMaastrichtian transgressive deposits of the Hekimhan and surroundings were accumulated within a magmatically active backarc basin. Sedimentary infill of the basin begins with non-marine, mostly fluvial deposits (mainly conglomerates), which are overlain by rudist-bearing shallow-water limestones. The overlying abundant planktonic foraminifera and calcareous nannoplankton-bearing flysch-type rocks are quite thick and the outcrops are widespread and easily accessible. Numerous studies have been carried out in the Hekimhan area for several purposes. Many studies such as Blumental (1938), Stchepinsky (1944), Ayan and Bulut (1964), € _ €zübol (1992), Bozkaya (1991), Izdar and Ünlü (1985), Onal and Go Bozkaya and Yalçın (1992), Gürer (1992, 1994), Bozkaya and Yalçın (1992) yielded important information on the stratigraphic framework of the basin. Rudists (Karacabey, 1970; Karacabey€ € € Oztemür, 1976, 1979, 1980; Ozer, 1988a,b, 1992, 2002, Ozer et al., 2008; Steuber and Schlüter, 2012) and benthic foraminifera € rmüs¸, 1990, 1992a,b, 1994; 1999; Meriç and Go €rmüs¸, 1997, (Go _ €rmüs¸ et al., 2001) of the 1999, 2001; Meriç and Inan, 1997; Go succession were studied from several localities. However a few studies dealt with planktonic foraminifera and calcareous nan€ €rmüs¸, nofossils of the successions (Ozdemir and Tunç, 1993; Go € 1992a and Yıldız and Ozdemir, 1999) despite the widespread and well-preserved abundant microfossil-bearing outcrops of these deposits. Aim of this study is to better understand the ages and the stratigraphy of the deeper marine deposits according to the planktonic foraminifera and calcareous nannofossils contents analysed in five stratigraphic sections. 2. Material and methods

Fig. 1. A-Regional tectonic setting of Turkey in relation to the Afro-Arabian and Eurasian plates (after Okay and Tüysüz, 1999). B-Geological map of Malatya city and € z, 1964). surroundings and location of the study area (simplified after Erento

Five stratigraphic sections were measured bed by bed and samples were collected from transects, where stratigraphy, boundary relations and lithological properties of the units were clearly recognisable (Fig. 2). In total 688 samples were collected from the five stratigraphic sections to document the planktonic foraminifera and nannofossil content, among them 384 samples for planktonic foraminifera and 304 samples were collected for obtaining nannofossils. Planktonic foraminifera were studied in thin sections for 138 samples because of the hardness on the lithologies (i.e. clayey limestones and limestones). The standard washing method (hydrogene peroxide method) was applied for 246 samples of relatively soft lithologies (i.e. mudstones) to obtain washed residues. The samples were washed through 100, 250 and 500 mm sieves. The method worked well and we obtained good isolated specimens. Planktonic foraminifera were analysed on the 250 mm size fraction. Some hard lithologies were treated with acetic acid following the procedure proposed by Lirer (2000) to obtain isolated planktonic foraminifera. However, the results were not satisfactory, because we could not manage to disaggregate some samples or we obtained dissolved specimens and therefore they were not useful for identification at species level. Planktonic

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foraminifera observed in thin section were studied and photographed under Olympus BX40 and mounted Olympus E-330 digital camera. Isolated planktonic foraminifera were studied under a stereo microscope (Olympus SZX 10) and were photographed by SEM (JEOL JSM-6060). Biostratigraphy and species concept of Robaszynski et al. (1984), Caron (1985), Premoli Silva and Sliter (1995), Robaszynski and Caron (1995), Petrizzo et al. (2011) and Falzoni and Petrizzo (2011) is followed in this study. For calcareous nannoplankton analysis, smear slides were prepared from raw samples. No specific techniques were applied to clean or concentrate the biogenic fraction in order to maintain the original composition of the calcareous nannoplankton assemblages. Smear slides were examined and photographed under Nikon Pol-400 mark Ortholux polarizing microscope using an oilimmersion objective at a magnification of 1600. Relative abundances of the nannoplankton were estimated using the schema of Wei (1988). Based on this method, one or more taxa in each field of view was classified as abundant; one taxa in 2e10 fields as common; one taxa in 11e50 fields as few; and one taxa per 51e200 fields as rare. All the rock samples, isolated specimens, thin sections and images of the planktonic foraminifera are deposited in the Geological Engineering Department of the Dokuz Eylul University _ (Izmir, Turkey). All the rock samples, slides and images of the studied calcareous nannoplanktons are stored in the Geological Engineering Department of the Aksaray University (Aksaray, Turkey). 3. Geological setting and stratigraphy

Fig. 2. Location map of stratigraphic sections.

The uppermost Cretaceous deposits of the Malatya Basin rest unconformably on the Upper Cretaceous ophiolitic basement (Hekimhan ophiolite or Hocalıkova ophiolite) and are represented by almost 1100-m-thick succession in the Hekimhan town and surroundings (Figs. 2e4). The Upper Cretaceous sequences of the

Fig. 3. Stratigraphic column and correlation of name and ages of units according to previous studies carried out in the Hekimhan area.

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Hekimhan area have been extensively studied and several formation names and various age assumptions were applied even for the same units (Fig. 3). Nomenclature by Bozkaya and Yalçın (1992) is followed in this study. Formation names used for the units and proposed ages are summarized and correlated as shown in Fig. 3. Non-marine fluvial conglomerates (Boyalıkdere Fm.) comprise the base of the uppermost Cretaceous succession and unconformably overlie the ophiolitic rocks (Figs. 3 and 4). Upwards conglomerates are overlain by rudist-bearing Güzelyurt Fm., which shows lateral and vertical thickness and facies changes. The formation is completely made up of marine rudistbearing massive to thick bedded limestones near Hekimhan town. It is represented mainly by the rudist-bearing mudstones with bioclastic limestone interlayers in the eastern part of the study area. Based on the rudist fauna, early to ‘middle’ Maastrichtian ages were suggested for the Güzelyurt Fm. by Karacabey € € (1970), Karacabey-Oztemür (1976) and Ozer (1988b). The age of the formation was interpreted as late Campanian-Maastrichtian €rmüs¸, 1992b), while a late based on benthic foraminifera (Go Campanian age was proposed for the same rudist-bearing levels by Steuber and Schlüter (2012) based on strontium isotope stratigraphy of the rudist shells.

observed in almost all sandstone beds (Figs. 4 and 5C). Thick mudstone beds are represented by abundant planktonic foraminifera and calcareous nannoplankton. Conglomerates and sandstones with orbitoid benthic foraminifera are observed within the €sehasan Fm. (Fig. 4). pelagic deposits at the lower part of the Ko Upward rhythmic mudstone-sandstone alternation dominates the sequence (Figs. 4 and 5CeD). Carbonate content of the 997-m-thick succession increases upwards and the formation passes gradually to the clayey limestones and calcareous shales of the Zorbehan Fm. to the top (Fig. 4). First marlstone beds occur in that part of the succession. Almost all complete Bouma sequences begin with a sandstone bed and end with a marlstone bed (Fig. 5D). Calcareous mudstone and marlstone beds are represented by rare planktonic foraminifera-bearing carbonate mudstone texture (Fig. 5E). The €sehasan Fm. and various levels of the uppermost levels of the Ko 215-m-thick Zorbehan Fm. include complete or partial Bouma sequences of calciclastic turbidites (calciturbitides) and contain calcispheres, quite rare planktonic foraminifera and nannofossils (Fig. 5F). Echinoids, ammonites, bivalves and trace fossils are also observed in this stratigraphic interval. Nine lithofacies were determined from the thickest succession of the Hekimhan area (i.e. Dumlu section) (Figs. 3 and 4). Deposition was accompanied by

€ sehasan Fm. rests conformably above the neritic rudistThe Ko bearing limestones of the Güzelyurt Fm. along a sharp contact (Fig. 5A) and is dominated by flysch-type sandstone-mudstone alternation with complete and partial Bouma sequences (siliciclastic turbidites) (Figs. 4 and 5BeD). Partial Bouma sequences are

extensive extrusive and intrusive magmatism (Booth et al., 2014). Widespread outcrops of the volcanic rocks are observed in and around Hasançelebi town. A 3-m-thick tuffite layer (Deveci Volcanics) is present within the pelagic deposits of the Hekimhan succession (Figs. 3 and 4).

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4. 1. Dumlu section

Fig. 4. Simplified stratigraphic column of the Dumlu section.

Overall deepening (transgressive) trend is obvious in the succession except for the uppermost part. The basin became shallow during the latest Cretaceous as a result of regression, as indicated by the presence of rudists and benthic foraminifera in the Sarıkız Fm, which is observed in the eastern part of the basin, outside the study € rmüs¸, (1999), Meriç and Go € rmüs¸ (1999) and area. According to Go € rmüs¸ et al. (2001) benthic foraminifera indicate a Maastrichtian Go age for the Sarıkız Fm. The upper Maastrichtian deposits are unca Fm. of Paleocene-Eocene age in conformably overlain by the Yag the study area (Figs. 3 and 4). 4. Planktonic foraminiferal and calcareous nannofossils distribution Planktonic foraminiferal and calcareous nannofossils distribution and biostratigraphy are discussed for each of the stratigraphic sections analysed in this study.

The Dumlu section was measured from east of Hekimhan town between Kus¸kaya hill and Ellezinkırı hill (Fig. 2). The succession comprises 997-m-thick flysch-type sandstone-mudstone alterna€ sehasan Fm. at the base and 103-m-thick clayey tion dominated Ko limestone-calcareous mudstone alternations of the Zorbehan Fm. at € sehasan Fm. include abundant the top (Fig. 4). Mudstones of the Ko planktonic foraminifera and calcareous nannoplankton. Microfossil content of the succession decreases towards the top (Zorbehan Fm.). Particularly the topmost 60-m-thick part of the succession bears quite poor planktonic foraminifera (Appendix 1A and B). An approximately 100-m-thick stratigraphic sequence between 220 m and 320 m (stratigraphic levels 2 and 3 in Fig. 4) is mainly composed of coarse sandstones and conglomerates and is barren of planktonic foraminifera and calcareous nannofossils, but abundant orbitoid benthic foraminifera are observed within the sandstone beds. The absence of pelagic fossils and the presence of benthic foraminifera indicate a short period of shallow depositional environment within a long-lasting and deeper environment. Alternatively, this may be a coarse siliciclastic deep-water interval which does not contain pelagic sediments, and all orbitoids were reworked from shallow into deep environment. The presence of late Maastrichtian calcareous nannoplankton taxa such as Lithraphidites quadratus and Micula praemurus (Figs. 6e8; Appendix 1A and B) from the base of the succession suggest that the age of the whole succession in the Dumlu section is late Maastrichtian in age (Appendix 1A and B). In addition, late Maastrichtian taxa Cribrosphaerella daniae, Arkhangelskiella maastrichtiana and Nephrolithus frequens appear in samples 0-17, 0-29 and 0-116 respectively (Figs. 6e9; Appendix 1A and B). Radotruncana calcarata is observed in 14 samples through a 283-mthick interval (from 0-20 to 0-58) (Fig. 11I; Appendix 1A and B). As R. calcarata is an index taxon for the early part of the late Campanian (e.g., Robaszynski et al., 1984; Premoli Silva and Sliter, 1995; Robaszynski, 1998; Premoli Silva and Verga, 2004; Petrizzo et al., 2011; Gradstein et al., 2012; Coccioni and Premoli Silva, 2015, among many others), the specimens observed should have been reworked from older strata. The Santonian-Campanian taxon Globotruncanita elevata observed from samples 0-16 and 0-18 should have been reworked as well (Appendix 1A and B). Likewise, nannofossils such as Broinsonia parca parca (samples 0-110 to 0-114) and Reinhardtites anthophorus (sample 0-132) are known as Campanian and Turonian-Campanian taxa respectively and therefore must be reworked. Late Maastrichtian taxa are not observed in the Dumlu section. Maastrichtian taxa such as Globotruncanita pettersi and Contusotruncana walfischensis appear in samples 0-62 and 0-63 respectively (Figs. 10e12, Appendix 1A and B). Some double keeled (i.e. Contusotruncana fornicata, Globotruncana arca, Globotruncana bulloides, Globotruncana neotricarinata and Globotruncana ventricosa) and single keeled (i.e. Globotruncanita stuartiformis) globotruncanids are quite abundant throughout the succession (Figs. 10e12; Appendix 1A and B). 4. 2. Zorbehan section The Zorbehan section was measured at the southern flank of Zorbehan mountain located 4 km NE of Hekimhan town (Fig. 2). € sehasan The succession comprises the uppermost levels of the Ko Fm. and Zorbehan Fm. and corresponds to the upper part of the € sehasan Dumlu section (Appendix 2). Flysch-type deposits of the Ko Fm. from the lower part of the Zorbehan section contain abundant planktonic foraminifera, while nannofossils are scarce (Appendix 2). The Zorbehan Fm. is dominated by alternation of clayey limestones and calcareous mudstones and includes local bioclastic

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€sehasan and Zorbehan formations from Dumlu section. A) Sharp contact (arrow) between rudist-bearing limestones of the Fig. 5. Field and microscope photographs of the Ko €sehasan Fm. (from base of the Ko € sehasan Fm., coordinate: 37 S 409854/4296771), B) Close-up view of abundant Güzelyurt Fm. (on the left) and mudstones (on the right) of the Ko €sehasan Fm. (sample no: 0-14), C) Rhythmic mudstone-sandstone alternation with partial planktonic foraminifera and calcareous nannoplankton-bearing mudstones of the Ko Bouma sequences (sample no: 0-86), D) Details of a 20-cm-thick bed with complete Bouma sequence (sample 0-113 was taken from the mudstones just above the sandstone bed). Almost all the Bouma cycles end with a thin marlstone bed (arrow), E) microphotograph of rare planktonic foraminifera-bearing marlstones (sample no: 0-126), F) microphotograph of calcisphere and quite rare planktonic foraminifera-bearing clayey limestones (sample no: 0-158).

limestone interlayers with orbitoid benthic foraminifera and rudist fragments. Zorbehan Fm. is 215-m-thick in this section and is overlain by massive dolomites of the Zorbehan Dolomite (Appendix 2). The Zorbehan Formation has rather poor planktonic foraminiferal assemblages particularly towards the upper part of the section in fact the topmost part of the succession is barren of planktonic foraminifera (Appendix 2). Within the assemblages Maastrichtian taxa Gt. pettersi and C. walfischensis occur from the base of the succession. The nannofossil assemblages are represented by few taxa in the 110-m-thick lower part of the succession. The last 180m-thick upper part is barren of nannofossils. Within the poor nannoplankton assemblages the occurrence of C. daniae in sample 0-197 indicates a late Maastrichtian age (Appendix 2). Despite late Maastrichtian taxa were not observed in the lower part of the succession, we assume that its age is late Maastrichtian through correlation with the equivalent stratigraphic levels in the Dumlu section (Fig. 5).

€slüler section 4. 3. Ko €slüler section is located 5 km SE of Hekimhan town and The Ko comprises the uppermost 210-m-thick part of the Hekimhan succession (Appendix 3). The 120-m-thick stratigraphic section of the € sehasan Fm. is observed in the lower part of the section. The Ko formation is made up of mainly flysch-type sandstone-mudstone alternations with bioclastic limestone interlayers particularly at the base of the section (Appendix 3). Bioclastic limestone beds include benthic organisms and are intercalated by mudstones with planktonic foraminifera and nannofossils. Fining upward beds are of typical limestone turbidites. Approximately 100-m-thick Zorbehan Fm. is dominated by alternation of marlstones and clayey limestones. Planktonic foraminifera are moderate to abundant in the €sehasan Fm.), while they dramatlower part of the section (i.e. Ko ically decrease upwards (i.e. Zorbehan Fm.) as in the Dumlu and Zorbehan sections. Nannofossils are also abundant in the lower part

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Fig. 6. Calibration of latest Cretaceous calcareous nannoplankton and planktonic foraminifera biozones and some stratigraphically important taxa observed in this study Stratigraphic distributions of each selected nannoplankton taxa are derived from following studies: Micula praemurus (Bukry): 9, 10; Arkhangelskiella maastrichtiana Burnett A: 12, B: 3, 5, 6, 7, 8; Lithraphidites quadratus Bramlette and Martini: 2, 4, 3, 5, 6, 7, 8, 11; Nephrolithus frequens Gorka: 1, 2, 3, 4, 5, 6, 7, 8, 11; Cribrosphaerella daniae Perch-Nielsen: 2, 3, 4, 5, 6, 7, 8, 11 (ages and calibrations of first and last occurrences of taxa and biozones are adapted from Gradstein et al., 2012).

of the section. Late Maastrichtian taxa C. daniae and A. maastrichtiana occur almost contantly from the base to the top of the section. Another index late Maastrichtian taxon M. praemurus occurs at the top of the succession. Late Maastrichtian planktonic €slüler succession. Maasforaminifera were not observed in the Ko trichtian taxa such as Gt. pettersi and C. walfischensis appear in samples 0-228 and 0-253 respectively (Appendix 3). anınkırı section 4. 4. Ag anınkırı section was measured at the SE flank of the The Ag anınkırı hill located 8 km SE of Hekimhan town (Fig. 2). The Ag succession comprises abundant rudist-bearing calcareous mud€sehasan Fm. stones of the Güzelyurt Fm. The 192-m-thick Ko conformably overlies the rudist-bearing calcareous mudstones. The formation begins with a 15-m-thick pebbly sandstones at the base and is dominated by silty mudstones in the rest of the

succession (Appendix 4). Carbonate content of the succession increases at the top, where calcareous mudstones is the dominant lithology. The succession comprises 20-m-thick clayey limestones and marlstones of the Zorbehan Fm. at the uppermost €sehasan Fm. is dominated by mudstones throughout part. The Ko anınkırı succession. The formation is represented by the Ag alternation of mudstones and sandstones in the NW part of the €slüler sections). Thickstudy area (i.e. Zorbehan, Dumlu and Ko ness of the formation is dramatically reduced from NW (997 m) to SE (192 m). Calcareous nannofossils content of the succession is poor at the base and the uppermost part of the sequence is barren of nannofossils. Late Maastrichtian taxon C. daniae appears in sample 11-356 (Appendix 4). Planktonic foraminifera are more or less abundant in the upper part of the section. Maastrichtian taxa Gt. pettersi and C. walfischensis appear in sample 11-357 just above the level with C. daniae. Gt. elevata observed in two samples (11-359 and 11-364)

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Fig. 7. Calcareous nannoplankton observed throughout the successions. A. Arkhangelskiella maastrichtiana Burnett, sample no: 0-29, Dumlu section B. Broinsonia parca parca Bukry, sample no: 0-114, Dumlu section (reworked specimen) C. Broinsonia parca parca Bukry, sample no: 0-110, Dumlu section (reworked specimen) D. Braarudosphaera bigelowii (Gran ve Braarud), sample no: 0-29, Dumlu section E. Cribrosphaerella daniae Perch-Nielsen, sample no: 11-335, Kırankaya section F. Cribrosphaerella daniae Perch-Nielsen, sample no: 0-29, Dumlu section G. Ceratolithoides aculeus (Stradner), sample no: 0-13, Dumlu section H. Calculites obscurus (Deflandre), sample no: 0-29, Dumlu section I. Dodekapodorhabdus noeliae anınkırı section J. Eiffellithus eximius (Stover), sample no: 11-321, Kırankaya section (reworked specimen) K. Eiffellithus parallelus Perch-Nielsen, Perch-Nielsen, sample no: 11-359 Ag € slüler section L. Eiffellithus turriseiffelii (Deflandre), sample no: 11-356, Ag anınkırı section M. Glaukolithus compactus (Bukry), sample no: 0-7, Dumlu section N. sample no: 0-264, Ko Lithraphidites quadratus Bramlette and Martini, sample no: 0-115, Dumlu section

are interpreted as reworked specimens as well as the single specimen of R. calcarata found in sample 11-352. Morever, marker nannofossils species were not encountered because of overall scarcity of nannofossils in the lower part of the section. Therefore, in the absence of supporting data the age of the underlying strata could be late Campanian or older. 4. 5. Kırankaya section The Kırankaya section was measured from some 10 km SE of Hekimhan town (Fig. 2). The sedimentary succession rests unconformably over the Upper Cretaceous ophiolitic rocks of the Hekimhan ophiolite. The succession begins with approximately 75m-thick conglomerates of the Boyalıkdere Fm. and 80-m-thick

rudist-bearing mudstones dominated deposits of the Güzelyurt Fm. (Appendix 5). Mudstones include sandstone and limestone interlayers. Strontium isotope studies from the rudist shells from the middle part of the Güzelyurt Fm. yield a late Campanian age €sehasan Fm. is made (Steuber and Schlüter, 2012). The overlying Ko up of mudstones in the lower part and by flysch-type mudstonesandstone alternation in the upper part. Partial Bouma sequences are commonly observed in the sandstone beds. The abundance of planktonic foraminifera is more or less constant through the € sehasan Fm, of which lower part contains long-ranging CamKo panian-Maastrichtian taxa. The appearance of Gt. angulata in sample 11-319 suggests that this level should not be older than latest Campanian. Occurrence of Gt. pettersi in sample 11-323 marks the beginning of Maastrichtian. Calcareous nannoplankton

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anınkırı section B. Microrhabdulus undosus Fig. 8. Calcareous nannoplankton observed throughout the successions. A. Lucianorhabdus cayeuxii Deflandre, sample no: 11-359, Ag anınkırı section C. Microrhabdulus undosus Perch-Nielsen, sample no: 0-23, Dumlu section D. Microrhabdulus decoratus Deflandre, sample no: 0Perch-Nielsen, sample no: 0-356, Ag anınkırı section G. Micula praemurus 100, Dumlu E. Micula swastica Stradner ve Steinmetz, sample no: 0-62, Dumlu section F. Micula decussata Vekshina, sample no: 11-356, Ag €slüler section H. Micula praemurus (Bukry), sample no: 0-2, Dumlu section I. Reinhardites anthophorus (Deflandre), sample no: 0-132, Dumlu section J. (Bukry), sample no: 0-284, Ko Prediscosphaera cretacea (Arkhangelsky), sample no: 0-29, Dumlu section K. Tranolithus manifestus Stover, sample no: 0-1, Dumlu section L. Retecapsa crenulata (Bramlette and Martini), sample no: 11-321, Kırankaya section

Fig. 9. Calcareous nannoplankton observed throughout the successions. A-Cribrosphaerella daniae Perch-Nielsen, sample no: 0-2, Dumlu section B-Cribrosphaerella daniae PerchNielsen, sample no: 0-2, Dumlu section C-Cribrosphaerella daniae Perch-Nielsen, sample no: 0-116, Dumlu section D-Cribrosphaerella daniae Perch-Nielsen, sample no: 0-116, Dumlu section E-Cribrosphaerella daniae Perch-Nielsen, sample no: 11-116, Kırankaya section F-Cribrosphaerella daniae Perch-Nielsen, sample no: 0-116, Dumlu section G-Cribrosphaerella ehrenbergii (Arkhangelsy), sample no: 0-2, Dumlu section H-Cribrosphaerella ehrenbergii (Arkhangelsy), sample no: 0-2, Dumlu section I-Lithraphidites quadratus Bramlette and Martini, sample no: 0-3, Dumlu section J-Lithraphidites quadratus Bramlette and Martini, sample no: 0-116, Dumlu section K-Lithraphidites quadratus Bramlette and Martini, sample no: 0-116, Dumlu section L-Lithraphidites quadratus Bramlette and Martini, sample no: 0-116, Dumlu section M-Lithraphidites quadratus Bramlette and Martini, and Cribrosphaerella ehrenbergii (Arkhangelsy), sample no: 0-116, Dumlu section N-Lithraphidites quadratus Bramlette and Martini, and Cribrosphaerella ehrenbergii (Arkhangelsy), sample no: 0-116, Dumlu section O-Lithraphidites quadratus Bramlette and Martini, sample no: 0-116, Dumlu section P-Lithraphidites quadratus Bramlette and Martini, sample no: 0-116, Dumlu section R-Nephrolithus frequens Gorka, sample no: 0-116, Dumlu section S-Nephrolithus frequens Gorka, sample no: 0-116, Dumlu section

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are generally scarce throughout the succession. Occurrences of A. maastrichtiana and C. daniae in samples 11-321 and 11-335 respectively suggest a late Maastrichtian age (Appendix 5). Occurrence of Eiffellithus eximius in sample 11-321 together with A. maastrichtiana indicates that this Turonian-Campanian taxon was reworked.

5. Discussion Hekimhan town and surroundings is one of the best area in the region, that present widespread and well-preserved outcrops of Upper Cretaceous pelagic deposits. Data based on planktonic foraminifera and calcareous nannoplankton obtained from five stratigraphic sections yield important information on the age and the € sehasan Fm. is depositional evolution of these deposits. The Ko represented by abundant planktonic foraminifera and calcareous nannofossil-bearing flysch-type sandstone-mudstone alternations, with partial and complete Bouma sequences that sharply overlies the rudist-bearing limestones and mudstones of the Güzelyurt Fm. The sharp contact between rudist-bearing limestones and mudstones with abundant pelagic microfossils should be related to sudden deepening of the sedimentary basin. Dominance of partial Bouma sequences indicates that deposition occurred mostly in distal parts of the submarine fans. The presence of rich orbitoid benthic foraminifera within an interval (sandstones and conglomerates) in the lower part of the succession suggests that the basin became shallow and subsequently deepened again. Alternatively, this may be a coarse siliciclastic deep-water interval (i.e. mass-flow conglomerates) which does not contain pelagic sediments, and all orbitoids were reworked from shallow into deep environment. Carbonate content of the succession increases towards the top. Rareness and absence of pelagic microfossils in this part of the succession (i.e. Zorbehan Fm.) should have been related to maximum shallowing of the basin. Late Maastrichtian age is inferred according to the presence of late Maastrichtian nannofossil taxa such as A. maastrichtiana, C. daniae, L. quadratus, M. praemurus and N. frequens. Occurrences of €sehasan Fm. L. quadratus and M. praemurus at the base of the Ko indicate that the 1100-m-thick succession was deposited during the late Maastrichtian. Consequently, sedimentation rate of the mixed siliciclastic and calciclastic deposits in this part of the basin increased as much as about 27.5 cm/ky, which is quite high. Comparable higher sedimentation rates were documented from similar siliciclastic submarine fans (SSFs) of various localities and ages (Table 1). Sedimentation rates of calciclastic submarine fans (CSFs) are particularly low than the rates of SSFs (Table 1). €sehasan Fm. is late MaasThe age of the lower part of the Ko trichtian in the Dumlu section, while the age of the lower levels of €sehasan Fm. is late Campanian-Maastrichtian in the the Ko anınkırı and Kırankaya sections (Fig. 13). Consequently, the Ag €sehasan Fm. is interpreted to be diachronous. deposition of the Ko €sehasan Fm. is 997 m in the Dumlu section, Thickness of the Ko anınkırı section. Likewise, which decreases to 192 m in the Ag thickness of the Zorbehan Fm. is 215 m in the Zorbehan section and decreases to 103 m in the Dumlu section. These data are indicative of lateral and vertical facies and thickness changes across short distances in the basin (Fig. 13).

Despite the Hekimhan area has quite thick upper Maastrichtian successions, index late Maastrichtian globotruncanids such as Abathomphalus mayaroensis, Contusotruncana contusa and Globotruncanita conica were not identified in this study, whereas Gt. pettersi and C. walfischensis are observed in almost all stratigraphic sections analysed in this study. Hovewer, some these marker species (i.e. A. mayaroensis, C. cf. contusa and Gt. conica) were documented in the Yes¸ilyurt area from southern part of the Malatya basin (Sarı et al., 2012). The index taxa were rarely found in several upper Maastrichtian successions of western Anatolia (i.e., Sarı, 2006; 2009; 2013). In addition, biserial and multiserial heterohelcids taxa such as Pseudoguembelina palpebra, Racemiguembelina fructicosa, Pseudoguembelina hariaensis and Plummerita hantkeninoides, typical of late Maastrichtian deposits (Premoli Silva and Verga, 2004; Huber et al., 2008; Perez Rodriguez et al., 2012; Gradstein et al., 2012; Coccioni and Premoli Silva, 2015), were not encountered in the Hekimhan succession. Presence of late Campanian and Santonian-Campanian taxa, i.e., R. calcarata and Gt. elevata, respectively, within the upper Maastrichtian strata can be explained by reworking from older strata. Likewise, Turonian-Campanian taxa, E. eximius, R. anthophorus and Campanian taxon B. parca parca occurring within the upper Maastrichtian deposits, must be reworked as well. These data confirm deposition and subsequent erosion of upper Campanian anınkırı section. deposits within the basin as documented in the Ag

6. Conclusions A thick (up to 1100-m-thick) mainly pelagic succession in the Hekimhan part of the Malatya Basin is represented by abundant planktonic foraminifera and calcareous nannoplankton assem€ sehasan Fm.). blages especially in the siliciclastic lower part (i.e. Ko Distributions of two microfossil groups in five stratigraphic section show that age of the deposits ranges from late Campanian to late Maastrichtian. Occurrences of nannoplankton L. quadratus and €sehasan Formation M. praemurus in the lowermost beds of the Ko indicate that the age of the whole succession is late Maastrichtian in the Dumlu section. The data show that sediment accumulation rate of the pelagic deposits is rather high and about 27.5 cm/ky for this part of the basin. Other late Maastrichtian taxa, C. daniae and A. maastrichtiana, are observed from the lowermost part of the succession. Although planktonic foraminifera are diverse and € sehesan Formation, index late abundant, particularly in the Ko Maasthrichtian species such as A. mayaroensis, C. contusa, Gt. conica, R. fructicosa, P. palpebra, P. hariaensis and P. hantkeninoides were not encountered. Maastrichtian planktonic foraminifera such as C. walfischensis and Gt. pettersi were recorded throughout the sections. Campanian (R. calcarata) and Santonian-Campanian (Gt. elevata) planktonic foraminifera obtained particularly from the lower part of the succession and calcareous nannofossils such as Broinsonia parca parca Bukry, Reinhardtites anthophorus (Deflanre) and Eiffellithus eximius (Stover) within the upper Maastrichtian deposits are interpreted as reworked from older strata. Changes in thickness of the formations along short distances in the five stratigraphic sections analysed in this study should be related to the diachroneity of the depositional and erosional events.

Fig. 10. Three-dimensional SEM views of isolated specimens of planktonic foraminifera observed throughout the successions. Scale bar is 100 mm for all images. 1) umbilical view, 2) anınkırı section spiral view, 3) side view A. Contusotruncana fornicata (Plummer), sample no: 0-23, Dumlu section B. Contusotruncana patelliformis (Gandolfi), sample no: 11-358, Ag C. Contusotruncana walfischensis (Todd), sample no: 0-63, Dumlu section D. Globotruncana aegyptiaca Nakkady, sample no: 0-108, Dumlu section E. Globotruncana arca (Cushman), €slüler section G. Globotruncana hilli Pessagno, sample no: 0-17, Dumlu section H. Globosample no: 0-30, Dumlu section F. Globotruncana bulloides Vogler, sample no: 0-248, Ko truncana linneiana (d'Orbigny), sample no: 0-15, Dumlu section I. Globotruncana neotricarinata Petrizzo et al., sample no: 0-50, Dumlu section J. Globotruncana orientalis El-Naggar, anınkırı section sample no: 0-13, Dumlu section K. Globotruncana rosetta (Carsey), sample no: 0-58, Dumlu section L. Globotruncana ventricosa White, sample no: 11-359, Ag

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Fig. 12. Thin section photomicrographs of planktonic foraminifera observed throughout the successions. Scale bar is 250 mm for all images. A. Contusotruncana fornicata (Plummer), € slüler section B. Contusotruncana walfischensis (Todd), sample no: 0-283, Ko €slüler section C. Gansserina gansseri (Bolli), sample no: 0-258, Ko €slüler section D. sample no: 0-267, Ko Globotruncana arca (Cushman), sample no: 0-158, Dumlu section E. Globotruncana arca-orientalis, sample no: 0-193, Zorbehan section F. Globotruncana bulloides Vogler, sample no: 0-126, Dumlu section G. Globotruncana esnehensis Nakkady, sample no: 0-169, Dumlu section H. Globotruncana cf. falsostuarti Sigal, sample no: 0-169, Dumlu section I. Globoanınkırı section K. Globotruncana neotricarinata Petrizzo truncana hilli Pessagno, sample no: 0-144, Dumlu section J. Globotruncana mariei Banner and Blow, sample no: 11-374, Ag €slüler section L. Globotruncana ventricosa White, sample no: 0-266, Ko € slüler section M. Globotruncana dupeublei Caron et al., sample no: 11-370, et al., sample no: 0-281, Ko anınkırı section N. Globotruncanita pettersi (Gandolfi), sample no: 11-370, Ag anınkırı section O. Globotruncanita stuartiformis (Dalbiez), sample no: 0-159, Dumlu section P. Ag € slüler section R. Rugoglobigerina hexacamerata Broenniman, sample no: 0-147, Dumlu section S. Rugoglobigerina milaRadotruncana subspinosa (Pessagno), sample no: 0-268, Ko anınkırı section menesis Smith and Pessagno, sample no: 0-144, Dumlu section T. Rugoglobigerina rugosa (Plummer), sample no: 11-349, Ag

Fig. 11. Three-dimensional SEM views of isolated specimens of planktonic foraminifera observed throughout the successions. Scale bar is 100 mm for all images. 1) umbilical view, 2) spiral view, 3) side view A. Globotruncanella havanensis (Voorwijk), sample no: 0-83, Dumlu section B. Globotruncanita angulata (Tilev), sample no: 0-119, Dumlu section C. Gloanınkırı section (reworked specimen) D. Globotruncanita insignis (Gandolfi), sample no: 0-23, Dumlu section E. Globotruncanita botruncanita elevata (Brotzen), sample no: 11-359, Ag pettersi (Gandolfi), sample no: 0-119, Dumlu section F. Globotruncanita stuarti (de Lapparent), sample no: 0-112, Dumlu section G. Globotruncanita stuartiformis (Dalbiez), sample no: 0-15, Dumlu section H. Globotruncanita stuartiformis-insignis, sample no: 0-51, Dumlu section I. Radotruncana calcarata (Cushman), sample no: 0-51, Dumlu section (reworked specimen) J. Rugoglobigerina macrocephala Broennimann, sample no: 0-95, Dumlu section K. Rugoglobigerina milamensis Smith and Pessagno, sample no: 0-79, Dumlu section L. Rugoglobigerina rugosa (Plummer), sample no: 0-89, Dumlu section

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Table 1 Sedimentation rates of some siliciclastic and calciclastic submarine fans. Locality or Fan

Age

Calciclastic Submarine Fans (CSF) Albacore CSF Miocene Anotz CSF Eocene Monte Corvo CSF Late Cretaceous Siliciclastic Submarine Fans (SSF) Hecho Fans Eocene Mt. Messenger Fan Late Miocene Ondarroa (northern Iberia) Middle Albian Bornova Flysch Zone Late Maastrichtian

Sedimentation rate (cm/ky)

Study

22e25 20 2.31

Bernecker et al. (1997) Payros et al. (2007) Van Konijnenburg et al. (1999)

60e80 70e80 60e450 9.84

Payros et al. (1999), Oms et al. (2003), Remacha et al. (2005) Browne and Slatt (2002) Agirrezabala and Garcia-Mondejar (1994) Sarı (2013) (micritic limestone interlayer within flysch-type siliciclastic deposits)

Fig. 13. Correlation of stratigraphic sections and stratigraphic distributions of index taxa.

Acknowledgements _ This study was financially supported by a TÜBITAK Grant no. € 109Y035, which is acknowledged. We thank to Omer Ilgın and

Cemile Solak for their helps during sample washing. Two anonymous reviewers are thanked for their constructive and helpful reviews. We extend our thanks to editor of Cretaceous Research Eduardo Koutsoukos for his suggestions. All the reviews and

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suggestions significantly improved the previous version of the manuscript.

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Appendix A. Supplementary data Supplementary data related to this article can be found at http://dx.doi.org/10. 1016/j.cretres.2015.12.012.