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Late Maastrichtian-Late Palaeocene planktic foraminiferal biostratigraphy of the matrix of the Bornova Flysch Zone around Bornova (İzmir, Western Anatolia, Turkey)

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The Bornova Flysch Zone (BFZ), located between the Menderes Massif and the İzmir-Ankara Suture in westernmost Anatolia (Turkey), forms the westernmost part of the Anatolide-Taurides. The BFZ comprises intensely sheared Upper Cretaceous-Palaeocene matrix and blocks of various origins. The matrix of the BFZ is mainly made up of unfossiliferous flysch-type sediments (alternations of sandstones and shales).

Turkish Journal of Earth Sciences http://journals.tubitak.gov.tr/earth/ Research Article Turkish J Earth Sci (2013) 22: 143-171 © TÜBİTAK doi:10.3906/yer-1107-2 Late Maastrichtian-Late Palaeocene planktic foraminiferal biostratigraphy of the matrix of the Bornova Flysch Zone around Bornova (İzmir, Western Anatolia, Turkey) Bilal SARI* Dokuz Eylül University, Faculty of Engineering, Department of Geological Engineering, Tınaztepe Campus, 35160, Buca-İzmir, Turkey Received: 17.07.2011 Accepted: 15.02.2012 Published Online: 04.01.2013 Printed: 25.01.2013 Abstract: The Bornova Flysch Zone (BFZ), located between the Menderes Massif and the İzmir-Ankara Suture in westernmost Anatolia (Turkey), forms the westernmost part of the Anatolide-Taurides The BFZ comprises intensely sheared Upper Cretaceous-Palaeocene matrix and blocks of various origins The matrix of the BFZ is mainly made up of unfossiliferous flysch-type sediments (alternations of sandstones and shales) In Bornova (İzmir, western Turkey) and its surroundings, these clastics locally include planktic foraminiferabearing pelagic micritic limestone and calcareous shale lenses and interbeds (Beytitepe Limestone) As a result of studies focusing on the planktic foraminifera-bearing pelagic interlayers in three areas (Gửkdere, Iklar and Kocaỗay areas) around Bornova, a detailed planktic foraminiferal biostratigraphy of the rocks is documented for the first time The thickness of the laminated micritic limestones attains 360 m in the Gökdere area Occurrences of late Maastrichtian species such as Abathomphalus mayaroensis (Bolli), Contusotruncana contusa (Cushman), Globotruncanita conica (White) and Racemiguembelina fructicosa (Egger) within planktic foraminifera assemblages obtained from the laminated micritic limestones and red calcareous shales in the three areas suggest a late Maastrichtian age for these rocks The occurrence of various species of Globanomalina, Morozovella, Igorina and Parasubbotina within the calcareous shales in the Işıklar area suggests a late Palaeocene age The Kocaỗay area has well-preserved outcrops showing the stratigraphy of the matrix, despite the more complex geology The upper Maastrichtian laminated micritic limestones are gradationally overlain by upper Maastrichtian calcareous shales The calcareous shales are represented by rich planktic foraminiferal assemblages and include blocks derived from laminated micritic limestones The upper Mastrichtian calcareous shales are overlain by Palaeocene red calcareous shales Poor assemblages including Parasubbotina varianta (Subbotina), Subbotina triangularis (White), Subbotina cf velascoensis (Cushman), Globanomalina compressa (Plummer) and Globanomalina planoconica (Subbotina) indicate a late Palaeocene age for the lower part and a latest Palaeocene age for the upper part of the calcareous shale sequence Therefore, the age of conglomerates and flysch overlying the calcareous shales should be latest Palaeocene or younger in the Kocaỗay area Key Words: Planktic foraminifer; biostratigraphy; late Maastrichtian - late Palaeocene; Bornova Flysch Zone; Western Anatolia Introduction The Bornova Flysch Zone (BFZ) forms a 50 to 90 km wide and approximately 230 km long tectonic zone between the Menderes Massif and the İzmir-Ankara Suture (Okay & Altıner 2007) in westernmost Turkey (Figure 1) It corresponds to the western part of the İzmir-Ankara Zone of Brinkmann (1966) The rocks of this zone cropping out in İzmir and its surroundings were named the Bornova mélange by Erdoğan (1990b) According to Okay et al (2012) the Upper Cretaceous rocks of the BFZ were deposited in a narrow basin on the northern margin of the Anatolide-Tauride Block located between the NeoTethyan Ocean to the west and a strike-slip tear fault to the east As the tear fault separated the basin fill and the continental subduction zone to the east, the BFZ escaped Tertiary metamorphism while the coeval rocks of the Menderes Massif underwent HP/LT metamorphism * Correspondence: bilal.sari@deu.edu.tr The BFZ comprises intensely sheared matrix and blocks of Mesozoic limestone, mafic volcanic rocks, radiolarites and serpentinites (Erdoğan 1990b; Okay & Siyako 1993) The limestone blocks derived from the platform range up to 20 km across and their ages range from Triassic to Late Cretaceous (Özer & İrtem 1982; Özer 1989; Erdoğan 1990a, 1990b; Erdoğan et al 1990; Okay & Siyako 1993; İşintek et al 2000; İşintek et al 2006; Okay & Altıner 2007; Senowbari-Daryan & İşintek 2008; İşintek et al 2009a, 2009b) The matrix of the BFZ in the İzmir area comprises mainly unfossiliferous flysch-type sediments (alternations of sanstones and shales), which locally include calcareous shales and micritic limestone lenses and interbeds with planktic foraminifera suggesting a Campanian-early Palaeocene (Danian) age according to previous studies (Konuk 1977; Yağmurlu 1980; Özer & İrtem 1982; Erdoğan 1990b) 143 Sarı-Figure SARI / Turkish J Earth Sci a Rhodope-Stranja Massif 42° Black Sea Thrace Basin e Zon İstanbul ul İstanb Sea of Marmara lag Pe Sakarya Zone on Tavşanlı Zone ian IAS Zo Afyon Zone BF Z ne Aegean Sea 38° Menderes Massif İzmir Figure 1b Athens Lycian Nappes N Cycladic Islands BFZ: BORNOVA FLYSCH ZONE IAS: İZMİR-ANKARA SUTURE b 10000 20000 Yamanlar Da Q Balatỗk ầili 60000 200 km Mediterranean Sea Spil Da Kocaỗay area Bornova Karyaka İzmir İzmir Bay N 30000 Işıklar area Kemalpaşa Q Narlıdere 50000 Buca Balỗova Gỹzelbahỗe Gửkdere area Mahmut Da Dakzlca 40000 Q Efemỗukuru 10 km Cumaovas Q alluvium Neogene Neogene sedimentary volcanic rocks rocks Cretaceous flysch and carbonate rocks Paleozoic-Mesozoic metamorphic rocks study areas Figure (a) Main tectonic units of western Anatolia and eastern Greece (after Görür & Tüysüz 2001) Study area is situated in the Bornova Flysch Zone, which corresponds to the westernmost part of the Tauride-Anatolides (b) Simplified geological map of İzmir and surroundings, showing locations of the study areas (simplified after Erentöz 1964) 144 SARI / Turkish J Earth Sci Well-preserved outcrops of calcareous shales and micritic limestones occur around Bornova (İzmir) and its surrounding area (Figure 1) These calcareous pelagic interlayers, named the Beytitepe Limestone by Yağmurlu (1980), are an unique palaeontological data resource within the matrix of the BFZ as they yielded rich planktic foraminifera assemblages Hence, they possess important data relating to the opening and closing ages and the sedimentological and tectonostratigraphic evolution of the basin However, few studies have dealt with the palaeontological aspects of these rocks (Konuk 1977; Yağmurlu 1980; Özer & İrtem 1982; Erdoğan 1990b) The planktic foraminiferal content of the pelagic interlayers has not been documented in detail until today despite its importance in dating the matrix of the BFZ A planktic foraminifera based biostratigraphic study of the calcareous shales and micritic limestones of the Beytitepe Limestone is documented here in order to help chronostratigraphic determinations (Figure 2) Material and methods This study is based on detailed geological mapping and systematic sampling through the measured stratigraphic sections Four hundred seventy nine samples were collected from the pelagic micritic limestones and calcareous shales of the Beytitepe Limestone in order to study the planktic foraminiferal content A standard washed-sample method did not work as the limestones AGE Upper Cretaceous (middle-upper Santonian) uppermost Palaeoceneupper Maastrichtian upper Maastrichtian and calcareous shales are mostly indurated and cut by numerous pressure solution seams as a result of intense shearing Therefore, thin sections were prepared from 390 samples, from which axially oriented forms were picked to identify most taxa with a high degree of confidence, as most of the diagnostic criteria can be recognized in such axial and/or subaxial sections This method is widely used in planktic foraminifera studies, especially in the Cretaceous (Wonders 1979; Fleury 1980; Sliter 1989; Premoli Silva & Sliter 1994; Sliter 1999; Robaszynski et al 2000; Premoli Silva & Verga 2004) Papers specific to Turkey include Farinacci & Yeniay (1986), Özkan & Kưylüoğlu (1988), Ưzkan Altıner & Ưzcan (1999), Sarı (1999), Sarı & Özer (2002), Sarı (2006a, 2006b, 2009) and Okay & Altıner (2007), which are based on planktic foraminifera identified in thin section Hovewer, there have been few attempts to study Palaeocene planktic foraminifera from thin section The resolution of thinsection zonation is nearly as precise as zonal schemes based on isolated specimens for the Cretaceous (Sliter 1989) In addition to these contributions, Robaszynski et al (1984) is also frequently cited for late Maastrichtian planktic foraminiferal species identification The Latest Cretaceous planktic foraminiferal zonation of Premoli Silva & Sliter (1994), Premoli Silva & Sliter (1999) and Premoli Silva & Verga (2004) is followed in this study (Figure 3) Palaeocene planktic foraminifera identification is based on Berggren et al (1995), Olsson et al (1999) and Olsson LITHOLOGY LITHOLOGY EXPLANATION rudist-bearing bioclastic limestone planktic foraminifera-bearing micritic limestone planktic foraminifera-bearing calcareous shale planktic foraminifera-bearing laminated micritic limestone conglomerates UNIT Işıklar Limestone Beytitepe Limestone STUDIED INTERVAL Kocaỗay Conglomerate deformed, highly sheared, sheared flysch flysch-type sandstone-mudstone alternation (mudstone dominated) Figure Simplified columnar section of the matrix of the Bornova Flysch Zone around Bornova This study focuses on the planktic foraminifera-bearing Beytitepe Limestone, consisting of laminated micritic limestones and calcareous shales 145 SARI / Turkish J Earth Sci 146 Thanetian 56 60 61 62 63 PLANKTIC FORAMINIFERA BIOZONES P5 M velascoensis P4c Ac soldadoensisGl pseudomenardii P4b Ac subsphaerica Selandian 59 EARLY 58 pseudomenardiiP4a Gl P variospira P3b I albeari P3a I pusilla P2 P uncinata Gl compressaP1c P inconstans Danian 57 PALAEOCENE LATE 64 P1b S triloculinoides P1a P pseudobulloides 65 Pα & P0 P eugubina & G cretacea Maastrichtian 66 69 70 71 72 73 74 75 76 C contusa - R fructicosa Ga gansseri late 68 A mayaroensis early late 67 Campanian Geological setting and previous studies The BFZ consists of chaotically deformed CampanianLower Palaeocene flysch-type matrix and blocks of various sizes and origins (Erdoğan 1990b; Okay & Siyako 1993) Many of the blocks comprise shallow water limestones, some of which can be as large as 20 km in diameter These limestone blocks were the subject of several studies, that showed that their ages range from Triassic to Late Cretaceous (Özer & İrtem 1982; Özer 1989; Erdoğan 1990a, 1990b; Erdoğan et al 1990; Okay & Siyako 1993; İşintek et al 2000; İşintek et al 2006, 2007; Okay & Altıner 2007; Senowbari Daryan & İşintek 2008; İşintek et al 2009a, 2009b) They were stratigraphically and palaeontologically correlated with the Karaburun Mesozoic successions (Erdoğan 1990a, 1990b) Some of the neritic blocks include pelagic interlayers in their stratigraphically upper parts A Tithonian-Turonian pelagic level in a block from south of Bigadiỗ (NE of the Zone) was documented by Okay & Altıner (2007), who correlated the stratigraphy of the block with similar successions from the Lycian nappes to the south Turonian-Maastrichtian, CampanianMiddle Maastrichtian and Santonian-Campanian ages were also recorded from the pelagic parts of the blocks (Erdoğan 1990b) Blocks of radiolarian cherts also yielded palaeontological data Recently, Mid to Late Triassic (late Ladinian to middle Carnian), Middle Jurassic (late Bathonian to early Callovian) and Middle Jurassic to Late Cretaceous (latest Bajocian to late Cenomanian) ages were documented based on the radiolaria in various chert blocks by Tekin & Göncüoğlu (2007), Tekin & Göncüoğlu (2009) and Tekin et al (2010) respectively Some palaeontological studies have data about planktic foraminifera, which give information on the fossiliferous pelagic interlayers within the flysch-type rocks of the matrix A Turonian-Early Campanian age was documented for the flysch in the Seferihisar area by Akartuna (1962) A late CampanianMaastrichtian age was obtained from Manisa and its surroundings by Oğuz (1966) According to Marengwa (1968), the age of the flysch in the Işıklar area is TuronianCampanian Konuk (1977) described some planktic foraminifera assemblages from the Kocaỗay area (north of Bornova, zmir), where the pelagic calcareous rocks are late Campanian - late Maastrichtian and are overlain by Palaeocene or younger conglomerates and flysch respectively The calcareous pelagic interlayers were named the Beytitepe Limestone by Yağmurlu (1980), who used the stratigraphical positions for three different flysch formations south of Bornova to establish their Campanian, Maastrichtian-Early Palaeocene and Middle- TIME EPOCH AGE (Ma) CRETACEOUS LATE et al (2011) Biozonation of Berggren et al (1995), Olsson et al (1999), Berggren & Pearson (2005) and Olsson et al (2011) is followed here (Figure 3) Because it is not easy to separate some Palaeocene species from two dimensional axial views in thin section, these species are grouped as Morozovella angulata (White) - Morozovella aequa (Cushman & Renz) group and Morozovella conicotruncana (Subbotina) - Morozovella velascoensis (Cushman) group G aegyptiaca Gl havanensis Ra calcarata Figure Chronostratigraphic chart showing the latest Cretaceous-Palaeocene planktic foraminiferal zonation The latest Cretaceous zonation plotted against the time scale of Gradstein et al (1994) is derived from Premoli Silva & Sliter (1994), Robaszynski (1998), Premoli Silva & Sliter (1999) and Premoli Silva & Verga (2004) Palaeocene zonation is from Berggren et al (1995), Olsson et al (1999), Berggren & Pearson (2005) and Olsson et al (2011) Time scale is adapted from Berggren et al (1995) Late Palaeocene ages A Danian age was documented from nanoplankton assemblages from the Işıklar area by Özer & İrtem (1982) Erdoğan (1990b) documented a more detailed planktic foraminiferal data from the matrix SARI / Turkish J Earth Sci of the BFZ in the area between Karaburun, Seferihisar and Manisa He obtained a Campanian-Maastrichtian age from the Gökdere area, a Middle MaastrichtianDanian age from the Kocaỗay area, an upper Campanianlower Maastrichtian age from the Pınarbaşı section (SE of Bornova), and a Campanian and middle-late Maastrichtian age from Spil Mountain (Manisa) İşintek et al (2007) examined limestone blocks from the Kocaỗay Conglomerate, which overlies the Palaeocene calcareous shales in the Kocaỗay area They obtained Late CretaceousPalaeocene, Palaeocene, middle-late Palaeocene ages from the neritic limestone blocks and suggested that the age of the conglomerates should be middle-late Palaeocene or younger The base of the pelagic limestones and overlying flyschtype rocks were observed at two localities The first locality is from the Karaburun peninsula, where a Mesozoic (Aptian-Albian) neritic sequence is unconformably overlain by Lower Campanian to Middle Maastrichtian pelagic limestones and flysch-type rocks of the Balıklıova Formation (Brinkmann et al 1977; Tansel 1990; Erdoğan 1990b; Erdoğan et al 1990) At the second locality, in the Kemalpaşa area (east of İzmir), Poisson & Şahinci (1988) documented the stratigraphy of a Mesozoic block and suggested that the Mesozoic neritic sequence was overlain by Maastrichtian pelagic rocks, middle Palaeocene or younger conglomerates and flysch respectively The flysch deposits and the blocks of the BFZ are unconformably overlain by undeformed upper Lower Eocene (late Cuisian) neritic limestones north of Akhisar (Akdeniz 1980; Önoğlu 2000) Therefore deformation affecting the BFZ must have predated the late Early Eocene The rocks of the BFZ are unconformably overlain by the conglomerates, claystones and clayey limestones of the Miocene Sabuncubeli Formation in Bornova and its surroundings (Erdoğan 1990b) Stratigraphy and planktic foraminiferal biostratigraphy of the Beytitepe Limestone The matrix of the BFZ dominantly comprises intensely sheared flysch-type deposits (alternations of sandstones and shales), which include conglomerates, micritic limestones and calcareous shales as lenses or conformable interbeds (Figure 2) This study focuses on the micritic limestones and calcareous shales, known as the Beytitepe Limestone, as they include rich planktic foraminiferal assemblages (Figure 2) The stratigraphy and planktic foraminiferal biostratigraphy of the micritic limestones and calcareous shales of the Beytitepe Limestone were studied in detail in the Gửkdere, Iklar and Kocaỗay areas around Bornova (Figure 1) 4.1 The Gökdere area The Gökdere area, covering approximately 12 km2, is located 10 km southeast of Bornova (Figures 1, 4) The Beytitepe Limestone occurs as a thick interlayer within flysch-type rocks and shows significant fluctuations in thickness over short distances (Figure 4) Numerous levels of variable thickness and size were also observed within the flysch Two stratigraphic sections, the Beytitepe and the Gökdere sections, were measured from the Gökdere area Details of the stratigraphic and palaeontological data obtained from these measured stratigraphic sections are presented below The Beytitepe stratigraphic section The Beytitepe Limestone is bounded both below and above by sandstoneshale alternations (Figures 4, 5, 6) The sandstone beds overlying the limestones show partial Bouma sequences The Beytitepe Limestone consists of grey laminated micritic limestones (Figure 7a) Pinkish grey and pale greenish-grey interlayers were also observed Lamina thickness is millimetric to centimetric Fifty nine samples were collected through the section The carbonate content of the sandstone-shale alternation increases towards the flysch-limestone contact and flysch gradually passes into the laminated limestones at the bottom of the sequence (Figure 6) Neritic blocks and sand-size clasts were observed at the base of the micritic limestones In addition, reworked orbitoid benthic foraminifera were also observed throughout this level The limestones have a planktic foraminiferal mudstone/wackestone depositional texture (Figures 7c, d) The abundance of planktic foraminifera varies from sample to sample (Figure 6) Some levels were severely affected by intense shearing As a result, rock and the planktic foraminifera were cut by pressure solution seams (Figure 7d) However, some levels escaped the effect of shearing, and many complete specimens of planktic foraminifera were observed (Figure 7c) An echinoid fragment was observed 149 m above the section base (Figures 6,7b) The specimen belongs to the holasterid group and probably is a species of the genus Echinocorys (Andy Gale, Pers comm 2010) The laminated micritic limestones of the Beytitepe stratigraphic section mostly have a moderate to poor planktic foraminifera content But, some rich planktic foraminifera-bearing levels were also observed (Figure 6) The following planktic foraminifera were observed in the Beytitepe stratigraphic section: Abathomphalus mayaroensis (Bolli), Contusotruncana contusa (Cushman), C fornicata (Plummer), C patelliformis (Gandolfi), Contusotruncana walfischensis (Todd), Gansserina cf gansseri (Bolli), Globotruncana arca (Cushman), G arca-orientalis, G dupeublei Caron et al., G esnehensis Nakkady, G falsostuarti Sigal, G linneiana (d’Orbigny), G mariei Banner & Blow, G orientalis El Naggar, G ventricosa White, Globotruncanella havanensis (Voorwijk), Globotruncanita angulata (Tilev), G conica (White), G pettersi (Gandolfi), G stuarti (de Lapparent), G stuartiformis (Dalbiez), Racemiguembelina fructicosa (Egger), Rugoglobigerina rugosa (Plummer), Praegublerina acuta (de Klasz) and Praegublerina robusta (de Klasz) (Figure 6; Plate 1) The occurrence of A mayaroensis throughout the succession indicates that age of the laminated micritic limestones in the Beytitepe stratigraphic section is late Maastrichtian (Figures 3, 6) The late Maastrichtian Abathomphalus mayaroensis is the index species of the homonym biozone (Figure 3) (Bolli, 1957; Robaszynski et al 1984; Caron 1985; Premoli Silva 147 SARI / Turkish J Earth Sci 21000 22000 23000 EXPLANATION Bornovalı T 51 61 78 sheared flysch undifferentiated Mesozoic blocks (Işıklar Limestone) 84 nlık Sa D ka yl Ya llı nı n D aba ğla r rı S 58 Berbersalih T upper Maastrichtian 70 Kara Kocaỗay Conglomerate laminated micritic limestone Beytitepe Limestone N 52000 36 unmapped area 51000 60 49 Kapuz D fault 32 24 52 45 50 79 62 65 puz 47 mi 42 kay D stream ası kD ? Beyti T 33 Ovacık T Beytitepe MSS 26 25 rsi 45 nli kD 49000 33 53 41 42 Gökdere MSS 46 settlement 25 22 35 58 56 56 32 D 61 43 Sivrikaya Ayı lı 40 38 measured stratigraphic section (MSS) line 50 66 34 54 road dirt tracts 49 30 Me peak of hill highway 64 strike and dip of overturned bedding axis of overturned syncline Ge Gư 50 62 45 Çıtırlık T 64 Ortaburun T 22 75 D 25 68 50000 strike and dip of bedding vertical bedding Ka 30 68 83 contact Yaylaarkası T 41 55 46 56 59 45 38 48000 49 70 pınar Kara Gökdere D 500 m Figure Geological map of the Gökdere area (See Figure 1b for location of the area) & Sliter 1994; Sliter 1989; Premoli Silva & Sliter 1999; Robaszynski et al 2000; Premoli Silva & Verga 2004; Sarı, 2006a, 2006b, 2009) The presence of C contusa and R fructicosa also indicates a late Maastrichtian age The coexistence of the two species suggests the presence of the C contusa-R fructicosa zone (Premoli Silva & Bolli 1973; Premoli Silva & Sliter 1994; Premoli Silva & Sliter 1999; Premoli Silva & Verga 2004), which corresponds to the lowermost part of the late Maastrichtian (Figure 3) 148 In addition, G conica, another late Maastrichtian species, is also recorded throughout the section (Figure 6) These data update the previous age assignment for these levels (Campanian-Maastrichtian) by Erdoğan (1990b) The Gökdere stratigraphic section A very thick pile of laminated micritic limestones crops out just north of the Gökdere Village This increased thickness was caused by an overturned syncline Partial Bouma sequences were observed in the sandstone-shale alternations to the SE and SARI / Turkish J Earth Sci sheared flysch 230 220 FOSSIL EXPLANATION echinoid Fossil Symbol Sample No N-61 N-60 N-59 N-58 N-57 N-56 N-55 210 N-54 200 190 Fossil occurrences N-44 N-43 N-42 170 N-41 160 N-40 N-39 N-37 150 N-36 N-35 N-34 140 N-33 130 relative abundance of a taxon N-32 N-31 N-30 120 110 occurrence of a taxon N-53 N-52 N-51 N-50 N-47 N-46 N-45 180 conglomerate rudist-bearing bioclastic limestone Lithology Thickness (m) Unit Stage thin laminated micritic limestone laminated clayey micritic limestone laminated clayey limestone with poor clay content laminated micritic limestone with sand to block-size limestone clasts calcareous shale (with rich carbonate content) calcareous shale (with poor carbonate content) flysch (sandstoneshale alternation) sandstone bed with erosive lower bed surface (with partial Bouma sequences) and sandstone lens Beytitepe Limestone upper Maastrichtian BLOCKS MATRIX laminated micritic limestone Abathomphalus mayaroensis Contusotruncana fornicata Contusotruncana patelliformis Globotruncana dupeublei Globotruncanella havanensis Globotruncanita stuarti Globotruncanita stuartiformis Gublerina sp Racemiguembelina fructicosa Rugoglobigerina rugosa Globotruncana linneiana Globotruncanita conica Contusotruncana contusa Globotruncanita angulata Globotruncana arca Globotruncana ventricosa Globotruncana esnehensis Globotruncana mariei Contusotruncana walfischensis Globotruncana falsostuarti Globotruncanita pettersi Gansserina gansseri Globotruncana arca-orientalis Globotruncana orientalis Planktic Foraminifera EXPLANATION N-29 100 N-28 N-27 90 N-26 N-25 probable occurrence of a taxon 80 Figure Lithology and fossil explanations for stratigraphic sections 70 60 NW of the micritic limestones The position of the Bouma sequences indicates that the SE flank of the fold is normal and the NW flank is overturned (Figures 4, 8) The whole limestone package was measured from SE to NW in order to correlate the limestones with the Beytitepe stratigraphic section A 720 m thick limestone sequence was measured through the section line Hence, the thickness of the laminated micritic limestones increases southwestwards from 220 m to 360 m within km (Figure 4) The body of the laminated micritic limestones shows thickness reduction from the Beytitepe measured section to the NE and grades laterally into flysch-type rocks Similarly, a single body of the micritic limestones is separated into several large and small lenses north of Beyti Tepe They N-24 N-23 N-22 N-21 50 N-20 N-19 N-18 N-17 40 30 20 N-16 N-15 N-13 N-12 N-10 N-9 N-8 N-7 N-6 N-5 N-4 N-3 10 sheared flysch N-2 N-1 Figure Beytitepe stratigraphic section (See Figure for location of the section and Figure for explanation) 149 SARI / Turkish J Earth Sci a b planktic foraminifera cut by solution seams complete planktic foraminifera shells pressure solution seams 500 µm c d 500 µm Figure Field and photomicrographs of the laminated micritic limestones observed in the Gökdere area; (a) Close-up view of the micritic limestones, which are mainly characterized by distinct lamination (Coordinate: 0520815/4248786) (b) Field photograph of a Holasterid echinoid (probably Echinocorys) from the 149th metre of the Beytitepe stratigraphic section (c) Photomicrograph of laminated micritic limestones, which escaped the effect of shearing Planktic foraminifera are observed as complete specimens within the wackestone/mudstone microfacies (Sample no: N-3) (d) Photomicrograph of laminated micritic limestones, which contain numerous pressure solution seams cutting planktic foraminifera embedded within the wackestone/mudstone microfacies (Sample no: N-28) overturned flank NW N-227 X normal flank N-150 X N-76 X SE 250 m sandstone beds with partial Bouma sequences Figure Gökdere stratigraphic section The section comprises laminated micritic limestones within the flysch-type deposits, which formed an overturned syncline This section presents the thickest package of laminated micritic limestones, which are 360-m-thick (See Figure for location of the section) 150 interfinger with the flysch-type rocks and pinch out NE of the study area (Figure 4) The lithological, sedimentological and palaeontological aspects of the micritic limestones of the Gökdere stratigraphic section are similar to the limestones in the Beytitepe stratigraphic section (Figure 8) One hundred and fifty two limestone samples were collected for thin section examination The planktic foraminiferal assemblages in the Gökdere stratigraphic section include all the species observed in the Beytitepe stratigraphic section, with, in addition, C fornicata-patelliformis, C plicata (White), C plummerae (Gandolfi), G bulloides Vogler, G hilli Pessagno, G insignis (Gandolfi), G petaloidea (Gandolfi), G elevata (Brotzen), Radotruncana subspinosa (Pessagno), Rugoglobigerina milamensis Smith & Pessagno, Rugoglobigerina pennyi Brönnimann and biserial and multiserial heterohelicids (See Plate for the images) The occurrence of A mayaroensis indicates that the age of the SARI / Turkish J Earth Sci EXPLANATION 20000 Miocene conglomerate (Sabuncubeli Fm.) unconformity upper Maastrichtianupper Palaeocene sheared flysch undifferentiated Late Cretaceous blocks (Işıklar Limestone) 42 S-4 Beytitepe Limestone calcareous shale laminated micritic limestone unmapped area contact covered contact fault strike and dip of bedding vertical bedding 50 stream S-2 S-3 67 46 35 ı dağ em bad Acı 52000 ak D S-2 peak of hill section line and section number S-1 73 Ka lab 22 20 N 36 250 m Canavar T 51000 20000 Figure Geological map of the Işıklar area Many lenses and blocks of the Beytitepe Limestone seen at or close to matrix-block contact (See Figure 1b for location of the area) micritic limestones in the Gökdere stratigraphic section is late Maastrichtian, as in the Beytitepe stratigraphic section Abathomphalus mayaroensis existed for 3.66 my from 68.66 my to 65.0 my (Robaszynski 1998) (Figure 3) During this time interval, a sequence at least 360 m thick, made up of laminated micritic limestones, was deposited Therefore, the sedimentation rate of the laminated micritic limestones was approximately 9.84 cm/ky Because flyschtype sediments were observed at the base and top of the limestones, the sedimentation rate obviously exceeded 9.84 cm/ky in this part of the basin 4.2 The Işıklar area Matrix and blocks of the BFZ were observed in the Işıklar area (Figure 9) The contact between the matrix and the blocks trends SW-NE and is mostly faulted The matrix consists mainly of sheared flysch, including laminated micritic limestone and calcareous shale lenses in variable thickness These lenses occur mostly along or near the block-matrix contact (Figure 9) The contacts between the lenses and adjacent flysch deposits are generally sharp While original stratigraphic contact relations are generally preserved, some micritic limestones have sheared contacts 151 upper Palaeocene upper Maastrichtian CampanianMaastrichtian ? Palaeocene uppermost CampanianMaastrichtain Abathomphalus mayaroensis Contusotruncana fornicata Contusotruncana patelliformis Contusotruncana plicata Contusotruncana plummerae Contusotruncana walfischensis Globotruncana arca Globotruncana dupeublei Globotruncana linneiana Globotruncana orientalis Globotruncanella havanensis Globotruncanita conica Globotruncanita stuarti Globotruncanita stuartiformis Globotruncanita pettersi Racemiguembelina fructicosa Rugoglobigerina milamensis Rugoglobigerina pennyi Rugoglobigerina rugosa Gublerina sp Multiserial heterohelicid Globanomalina ehrenbergi Globanomalina ehrenbergipseudomenardii Globanomalina planoconica Igorina albeari Morozovella acuta gr M angulata-M aequa Parasubbotina variospira Globanomalina chapmani Subbotina velascoensis Globanomalina sp Figure 10 Section is represented by many laminated micritic limestone levels within the flysch and comprises many packages separated by faults (See Figure for explanation and Figure for location of the section) with the flysch 16 lenses and lensoid laminated micritic limestone and calcareous shale blocks were sampled and mapped Although some lenses are a few metres thick, they were indicated on the geological map exaggeratedly as they contain important palaeontological data 64 samples were collected from the Işıklar area Laminated micritic limestones are mostly light grey and similar to the micritic limestones, somewhat as in the Gökdere area with respect to lithological aspects, depositional texture and planktic foraminiferal content Some lenses have rather poor planktic foraminifera content without any diagnostic species Therefore, four relevant sections are presented here to save space; Section This section comprises several laminated micritic limestone interlayers, which are intercalated with flysch and separated by numerous faults (Figure 10) Sample N-268 yielded a rich planktic foraminiferal assemblage The occurrence of A cf mayaroensis in the assemblage seemingly indicates that the age of the laminated micritic limestone is late Maastrichtian Other late Maastrichtian species such as G conica and R fructicosa were also observed in this sample (Figure 10; Plate 2) Samples N-271 and N-273 include rare Maastrichtian planktic foraminifera The lenses from which samples N-269, N-270 and N-272 were collected are similar to the other lenses lithologically, but include late Palaeocene planktic foraminifera such as Globanomalina cf chapmani (Parr), Globanomalina ehrenbergi (Bolli), Globanomalina ehrenbergi-pseudomenardii, Globanomalina planoconica (Subbotina), Igorina albeari (Cushman & Bermúdez), Morozovella acuta (Toulmin), gr Morozovella angulata (White) - Morozovella aequa (Cushman & Renz), Parasubbotina cf variospira (Belford) and Subbotina velascoensis (Cushman) (Figure 10; Plate 2) This section 152 X 1m 254 253 X N- X W 1m N- NE 252 N-268 X N- X 251 N270 X SW N- X N269 N- N271 27 X N272 SARI / Turkish J Earth Sci X E Globotruncana arca Globotruncana dupeublei Globotruncana falsostuarti Globotruncana mariei Globotruncanella havanensis Globotruncanita conica Globotruncanita stuarti Globotruncanita stuartiformis Racemiguembelina fructicosa Multiserial heterohelicid Globotruncana esnehensis Globotruncanita pettersi Globotruncana bulloides Globotruncana linneiana upper Maastrichtian Figure 11 Section shows a 2-m-thick laminated micritic limestone lens within the flysch (See Figure for explanation and Figure for location of the section) illustrates the magnitude of deformation that affected the BFZ matrix, as lenses from various stratigraphic intervals are in contact with each other (Figure 10) Section This section comprises a 2-m-thick laminated micritic limestone interlayered within the flysch sediments The occurrence of G conica and R fructicosa suggests a late Maastrichtian age (Figure 11; Plate 2) Section This section includes three laminated micritic limestone levels The lower two levels include sand to block-size neritic and pelagic lithoclasts and reworked benthic foraminifera, which are embedded within a planktic foraminifera-bearing micrite matrix Sample N-264 was collected from the topmost level, and its late Maastrichtian age is documented by the presence of G conica and R fructicosa (Figure 12) Section This section comprises a beigish-grey to pinkish-grey calcareous shale lens, which appears at the matrix-block contact (Figure 9) The calcareous shales gradationally overlie the flysch and include silt to fine sand-size clasts at the base Carbonate content increases upwards 12 samples were collected from the calcareous shales (Figure 13), which mainly consist of planktic foraminifera-bearing mudstones/wackestones throughout (Figure 14) Planktic foraminifera assemblages including Acarinina cf strabocella (Loeblich & Tappan), G chapmani, G compressa-ehrenbergi, G ehrenbergi (Bolli), G cf pseudomenardii (Bolli), I albeari, I pusilla (Bolli), gr M angulata - M aequa, Morozovella occlusa (Loeblich & Tappan), Morozovella praeangulata-angulata, P variospira, S triangularis (White) and S velascoensis are dominated by keeled Palaeocene forms, which became dominant during the late Palaeocene (Olsson et al 2011) The occurrences of keeled Morozovella species such as gr M angulata - M aequa, M occlusa and the other species in the planktic foraminiferal assemblages, such as A cf SARI / Turkish J Earth Sci calcareous shales K-20 S X calcareous shales X X fault X X K-99 X 98 97 K- 96 X K- X K- X 95 94 conglomerates K- X K- KX K- K K- -91 X K K -9 X K- -89 X K 21 X K- -88 X X 87 X N 92 93 calcareous shales with rich carbonate content laminated micritic limestones bituminous micritic limestones K-23 K-24 1m Globotruncanita sp Orbitoid foraminifera Abathomphalus mayaroensis Contusotruncana contusa Contusotruncana fornicata Globotruncana dupeublei Globotruncana esnehensis Racemiguembelina fructicosa Contusotruncana patelliformis Globotruncanita angulata Globotruncanita stuarti Rugoglobigerina rugosa Multiserial heterohelicids Globotruncana arca Globotruncanita conica Globotruncanella havanensis Rugoglobigerina milamensis Contusotruncana plicata Biserial heterohelicids Gublerina sp Globotruncana mariei unidentified ?Paleocene species Globotruncanita insignis upper Maastrichtian ?Palaeocene upper Maastrichtian Figure 18 Section 7, showing the stratigraphic relations of various lithologies of the Beytitepe Limestone (See Figure for explanation and Figure 15 for location of the section) mayaroensis, C contusa, G conica and R fructicosa at these levels (Figure 18; Plates 3, 4) suggest a late Maastrichtian age Another upper Maastrichtian calcareous shale level, which is overlain by conglomerates, was observed in the southern part of the section (Figure 18) The colour of the one meter thick uppermost layer of the calcareous shales is pale greenish grey Three lithologies seem to be conformable, as a discontinuity surface was not observed at the contacts The presence of reworked orbitoid benthic foraminifera, abundant shell fragments and the scarceness of planktic foraminifera in the bituminous micritic limestones indicate the proximity of the shallow sea environment Occurrences of planktic foraminifera, together with calcispheres in laminated micritic limestones, suggest a deeper depositional environment than in the underlying orbitoid benthic foraminifera-bearing micritic limestones The abundance of the K-selected specialists within the planktic foraminiferal assemblages in the red calcareous shales means a deeper distal depositional environment, as they dominate in open oceans, mainly during the onset of highstands of sea level (Robaszynski & Caron 1995) In summary, a deepening trend is clearly seen from the micritic limestones to the calcareous shales in the northern part of Section Red calcareous shales with very scarce planktic foraminifera occurring in mid- section are similar to the Palaeocene calcareous shales in Section Section Calcareous shales, a laminated micritic limestone block within the calcareous shales and overlying conglomerates were observed in this section (Figure 19) The laminated micritic limestone block is embedded within the calcareous shale matrix and is very similar to the laminated micritic limestones observed in Section In thin section, they show a depositional texture featuring planktic foraminifera, calcisphere and thin shell fragments-bearing wackestone Another small laminated micritic limestone clast, 20 cm in diameter (sample K-59), was observed within the calcareous shales (Figure 19) Calcareous shales were observed beneath and above the laminated micritic limestones and the contact between the two lithologies is very similar to the contact in Section Calcareous shales fill the hollows in the laminated micritic limestones with its uneven, undulating surface (Figure 19) Calcareous shales also resemble calcareous shales observed in Sections 5, and Occurrences of rich late Maastrichtian assemblages in both laminated micritic limestones and calcareous shales indicates that laminated micritic limestones were deposited, lithified, and then subsequently fragmented and transported to the deeper part of the basin during the late Maastrichtian 157 SARI / Turkish J Earth Sci laminated micritic limestone block section line N K-61 X 1m X X K-59 K-60 K-37 X K-57 X K-56 K-58 X X Kocaỗay Conglomerate calcareous shales (Beytitepe Limestone) slightly recristallized laminated micritic limestones (Beytitepe Limestone) a laminated micritic limestone block X K-60 X K-37 X K- K-61 59 NW X K-58 X K-57 K-56 X X K-62 X 1m SE Globotruncana arca Globotruncana bulloides Globotruncana linneiana Rugoglobigerina hexacamerata Rugoglobigerina pennyi Rugoglobigerina rugosa Globotruncanella havanensis Abathomphalus mayaroensis Contusotruncana walfischensis Globotruncana dupeublei Globotruncana esnehensis Globotruncana rosetta Globotruncanita stuartiformis Racemiguembelina fructicosa Multiserial heterohelicids Biserial heterohelicids Contusotruncana contusa Globotruncanita conica Globotruncanita pettersi Globotruncanita stuarti Gublerina sp Contusotruncana patelliformis Contusotruncana walfischensis Globotruncana mariei b upper Maastrichtian upper Maastrichtian Figure 19 Section 8; (a) Sketch map, (b) Cross-section showing a late Maastrichtian laminated micritic limestone block within late Maastrichtian calcareous shales (See Figure for explanation and Figure 15 for location of the section) 158 SARI / Turkish J Earth Sci block contact sample numbers planktic foraminifers calcisphere calcareous shales (Beytitepe Limestone) shell fragments laminated micritic limestones (Beytitepe Limestone) a b 500 µm red calcareous shales (Beytitepe Limestone) pressure solution seams X K-66 thick-walled planktic foraminifers c X K-65 d globular-chambered Palaeocene planktic foraminifers e f 500 µm pressure solution seams 500 µm Figure 20 Field photographs and photomicrographs of the various lithologies of the Beytitepe Limestone in the Kocaỗay area (a) Contact between the laminated micritic limestones and the calcareous shales Numbers stand for sample numbers, which are indicated in Section (b) Photomicrograph of the laminated micritic limestones, represented by wackestones (Sample no: K-32 in Section 5), (c) Close-up view of the upper Maastrichtian calcareous shales from Section (Numbers stand for sample numbers, which are indicated in Section 6), (d) Upper Maastrichtian calcareous shales are represented by abundant planktic foraminifera-bearing wackestones The rock and the planktic foraminifera are mostly cut by numerous pressure solution seams (Sample no: K-65 in Section-6), (e) Close-up view of the upper Palaeocene calcareous shales (26.5th metre of Section 6, where sample K-82 was collected), (f) Palaeocene calcareous shales, mainly represented by rare planktic foraminifera-bearing wackestones and mudstones Pressure solution seams commonly cut planktic foraminifera (Sample no: K-80 in Section-6) 159 SARI / Turkish J Earth Sci STAGE LITHOLOGY MATRIX BLOCKS LITHOLOGY EXPLANATION UNIT highly sheared sandstone-shale alternation sheared flysch conglomerate with large limestone blocks Kocaỗay Conglomerate laminated micritic limestone block upper Maast upperuppermost Palaeocene calcareous shale block calcareous shale with limestone block and pebbles calcareous shale laminated micritic limestone block upper Maast Beytitepe Limestone laminated micritic limestone middle-upper Santonian upper Maastrichtian ?lower Palaeocene rudist-bearing bioclastic limestone Işıklar micritic limestone with Limestone planktic foramifers laminated micritic limestone upper Maastrichtian sandstone bed with Bouma sequence laminated micritic limestone lens Beytitepe Limestone laminated micritic limestone Beytitepe Limestone conglomerate lens highly sheared sandstone-shale alternation late Maastrichtian planktic foraminifera Palaeocene planktic foraminifera middle-late Santonian planktic foraminifera sheared flysch Kocaỗay Conglomerate late Palaeocene planktic foraminifera rudist reworked orbitoid benthic foraminifera Figure 21 Detailed stratigraphic column of the matrix of the Bornova Flysch Zone around Bornova The column is based on data derived from all three areas The age of the Beytitepe Limestone and accompanying flysch-type rocks is late Maastrichtian in the Gökdere area and late Maastrichtian and late Palaeocene in the Işıklar area The age of the Beytitepe Limestone is late Maastrichtian-latest Palaeocene in the Kocaỗay area The age of the Kocaỗay Conglomerate and flysch, which overlie the calcareous shales must be latest Palaeocene or younger 160 SARI / Turkish J Earth Sci Discussion and conclusions Detailed studies based on the planktic foraminiferal biostratigraphy of the Beytitepe Limestone in the matrix of the BFZ around Bornova (İzmir) have revealed new data about the stratigraphy and age of the matrix (Figure 21) The age of the laminated micritic limestones in the Gökdere area, indicated by the occurrence of zonal maker A mayaroensis together with other late Maastrichtian species such as C contusa, G conica and R fructicosa, is late Maastrichtian The layer thickness attains 360 m, indicating a sedimentation rate of at least 9.84 cm/ky A previous Campanian-Maastrichtian age assigned for this level by Erdoğan (1990b) is revised in this study The Işıklar area has thin lenses of laminated micritic limestones and calcareous shales within the flysch-type deposits A late Maastrichtian age was indicated for the laminated micritic limestones by the presence of A mayaroensis, C contusa, G conica and R fructicosa A late Palaeocene age was also documented from the calcareous shale lenses, which contain an assemblage including many keeled Morozovella species such as gr M angulata - M aequa, M occlusa and other late Palaeocene species such as A cf strabocella, G chapmani, G cf pseudomenardii, I albeari, I pusilla, P variospira and S velascoensis Late Maastrichtian and late Palaeocene ages are documented for the first time in the Işıklar area by this study The Kocaỗay area has a complicated geology and provides important information about the stratigraphy and age of the matrix of the BFZ Laminated micritic limestones are very similar to their counterparts observed in the Gökdere and Işıklar areas A late Maastrichtian age, based on the occurrences of A mayaroensis, C contusa, G conica and R fructicosa, was obtained from the laminated micritic limestones, which are gradationally overlain by the calcareous shales (Figure 21) which contain a rich late Maastrichtian planktic foraminiferal assemblage They are dominated by diverse, large, thick-walled complex morphotypes (K-selection), which indicate a deeper distal depositional environment The assemblage, including A mayaroensis, C contusa, G conica and R fructicosa, suggests a late Maastrichtian age Blocks and pebbles of the laminated micritic limestones were observed within the calcareous shales, which are overlain by Palaeocene calcareous shales (Figure 21) The Late Maastrichtian and Palaeocene calcareous shales are similar in appearance but the Palaeocene calcareous shales have a scarce planktic foraminifera content Poor assemblages, including P varianta, S triangularis, S cf velascoensis, G compressa and G planoconica, indicate a late Palaeocene age for the lower part and a latest Palaeocene age for the upper part of the calcareous shale sequence In this study, index species such as A mayaroensis, G conica, R fructicosa and many other Maastrichtian species have been documented from this area for the first time It appears that the age of the calcareous shales extends to the latest Palaeocene, which is also new information about this area (Figure 21) The Kocaỗay Conglomerate overlies various stratigraphic levels of the calcareous shales and laminated micritic limestones (Figure 21) Flysch-type sediments are the younger lithologies in the Kocaỗay area and overlie the Kocaỗay Conglomerate (Figure 21) Based on the palaeontological data from the planktic foraminifera from all three areas, it can be concluded that the age of the Beytitepe Limestone and accompanying flysch-type sediments is late Maastrichtian in the Gökdere area, late Maastrichtian and late Palaeocene in the Işıklar area and late Maastrichtian - latest Palaeocene in the Kocaỗay area The age of the Kocaỗay Conglomerate and overlying flysch-type deposits in the Kocaỗay area must be latest Palaeocene or younger (Figure 21) Acknowledgements This study was financially supported by a TUBİTAK grant 109Y182 and Dokuz Eylül University (BAP) grant 2009 KB.FEN.064, which are gratefully acknowledged Dan Georgescu and an anonymous reviewer are thanked for their valuable constructive reviews The help of Atilla Kandemir and Ömer Ilgın during the field studies is appreciated I also would like to thank Taner Korkmaz for participating in the field studies and for his help in drawing some of the figures I would like to thank Maria Rose Petrizzo for valuable comments of some planktic foraminifera identifications, especially the Palaeocene species References Akartuna, M 1962 İzmir-Torbalı-Seferihisar-Urla bölgesinin jeolojik etüdü [Geological investigation of İzmir-TorbalıSeferihisar-Urla region] İstanbul Üniversitesi Fen Fakültesi Monografisi 18, 22–29 [in Turkish] Akdeniz, N 1980 Başlamış Formasyonu [Başlamış Formation] Jeoloji Mühendisliği 10, 39–47 [in Turkish] Berggren, W.A., Kent, D.V., Swisher, C.C III & Aubry M.P 1995 A revised Cenozoic geochronology and chronostratigraphy In: Berggren, W.A., Kent, D.V., Swisher, C C., III, Aubry, M.P & Hardenbol, J (eds), Geochronology, Time Scales and Global Stratigraphic Correlation Society for Sedimentary Geology, Special Publication 54, 129–212 Berggren, W.A & Pearson, P.N 2005 A revised tropical to subtropical Paleogene planktic foraminiferal zonation Journal of Foraminiferal Research 35, 279–298 Bolli, H.M 1957 The 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Geological Congress of Turkey, Ankara, Abstracts, p 270–272 Özer, S 1989 Sur une faune d’ Hippuritides des calcaires du Cretace superieur de la zone d’ İzmir-Ankara (Anatolie occidentale) Interet paleontologique et stratigraphique Revue de Paleobiologie 8, 335–343 Özer, S & İrtem, O 1982 Işıklar-Altındağ (Bornova-zmir) alan ĩst Kretase kireỗtalarnn jeolojik konumu, stratigrafisi ve fasiyes özellikleri [Geological setting, stratigraphy and facies characteristics of the Upper Cretaceous limestones in the Işıklar-Altındağ (Bornova-İzmir) area] Türkiye Jeoloji Kurumu Bülteni 25, 41–47 [in Turkish with English abstract] Özkan, S & Köylüoğlu, M 1988 Campanian-Maastrichtian planktic foraminiferal biostratigraphy of the Beydağları Autochthonous Unit, Western Taurides, Turkey Middle East Technical University, Journal of Pure and Applied Sciences 21, 377–388 Özkan-Altıner, S & Özcan, E 1999 Upper Cretaceous planktic foraminiferal biostratigraphy from NW Turkey: calibration of the stratigraphic 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Verga, D 2004 Practical manual of Cretaceous planktic foraminifera In: Verga, D & Rettori, R (eds.), International School on planktic foraminifera, 3rd Course: Cretaceous Universities of Perugia and Milan, Tiporafia Pontefelcino, Perugia (Italy), pp 283 Robaszynski, F 1998 Planktic foraminifera-Upper Cretaceous, Chart of Cretaceous Biochronostratigraphy In: de Graciansky, P.C., Hardenbol, J & Vail, P.R (eds), Mesozoic and Cenozoic sequence stratigraphy of European basins Society For Sedimentary Geology (SEPM), Special Publication 60, pp.782 Robaszynski, F & Caron, M 1995 Cretaceous planktic foraminifera: comments on the Europe-Mediterranean zonation Bulletin de la Société Géologique de France 166, 681–692 Robaszynski, F., Caron, M., Gonzales Donoso, J.M & Wonders, A.A.H 1984 Atlas of Late Cretaceous Globotruncanids Revue de Micropaleontologie 26, 145–305 Robaszynski, F., Gonzales Donoso, J.M., Linares, D., Amedro, F., Caron, M., Dupuis, C., Dhondt, A.V & Gartner, S 2000 Le Crétacé supérieur de la région de Kalaat Senan, Tunisie centrale Litho-biostratigraphie intégrée: zones d’ammonites, de foraminifères planctoniques et de nannofossiles du Turonien supérieur au Maastrichtien Bulletin des Centres de Recherches Exploration-Production Elf-Aquitaine 22, 359–490 Senowbari-Daryan, B & İşintek, İ 2008 Izmirella cretacea nov gen., nov sp., an enigmatic bioconstructing alga from the Lower Cretaceous, NE of Bornova-İzmir/Turkey Geologia Croatica 61, 273–295 Sarı, B 1999 Biostratigraphy of the Upper Cretaceous Sequences in the Korkuteli Area (Western Taurides) MSc thesis, Dokuz Eylül University, İzmir Turkey [Unpublished] Sarı, B 2006a Upper Cretaceous planktic foraminiferal biostratigraphy of the Bey Dağları autochthon in the Korkuteli Area, Western Taurides, Turkey Journal of Foraminiferal Research 36, 241–261 Sarı, B 2006b Foraminifera-rudist biostratigraphy, Sr-C-Isotope stratigraphy and microfacies analysis of the Upper Cretaceous sequences of the Bey Dağları autochthon (western Taurides, Turkey) PhD thesis, Dokuz Eylül University, İzmir-Turkey [Unpublished] Sarı, B 2009 Planktic foraminiferal biostratigraphy of the ConiacianMaastrichtian sequences of the Bey Dağları Autochthon, western Taurides, Turkey: Thin section zonation Cretaceous Research 30, 1103–1132 Sarı, B & Özer, S 2002 Upper Cretaceous stratigraphy of the Beydağları carbonate platform, Korkuteli area (Western Taurides, Turkey) Turkish Journal of Earth Sciences 11, 39–59 Sliter, W.V 1989 Biostratigraphic zonation for Cretaceous planktic foraminifers examined in thin section Journal of Foraminiferal Research 19, 1–19 Sliter, W.V 1999 Cretaceous planktic foraminiferal biostratigraphy of the Calera Limestone, Northern California, USA Journal of Foraminiferal Research 29, 318–339 Tansel, İ 1990 Balıklıova formasyonunun (Karaburun-İzmir) planktik foraminiferlere göre yaş konağı [Age of Balklova formation (Karaburun-zmir) according to planktic foraminifers] Selỗuk Üniversitesi Mühendislik-Mimarlık Fakültesi Dergisi, 41–50 [in Turkish with English abstract] Tekin, U.K & Göncüoğlu, M.C 2007 Discovery of oldest (late Ladinian to middle Carnian) radiolarian assemblages from the Bornova Flysch Zone in western Turkey: implications for the evolution of the Neotethyan İzmir-Ankara Ocean Ofioliti 32, 131–150 Tekin, U.K & Göncüoğlu, M.C 2009 Late Middle Jurassic (Late Bathonian-Early Callovian) radiolarian cherts from the Neotethyan Bornova Flysch Zone, Spil Mountains, Western Turkey Stratigraphy and Geological Correlation 17, 298–308 Tekin, U K., Göncüoğlu, M.C & Uzuncimen, S 2010 An olistolith with continuous latest Bajocian to late Cenomanian pelagic deposition within the Bornova Flysch Zone in western Turkey: Radiolarian Assemblages XIX Congress of the CarpathianBalkan Geological Association, Geologica Balcanica 39, 386– 387 Wonders, A.A.H 1979 Middle and Late Cretaceous pelagic sediments of the Umbrian sequence in the Central Apennines Koniklijke Nederlandse Akademie Van Wetenshappen Proceedings 82, 171–205 Yağmurlu, F 1980 Bornova (İzmir) güneyi filiş topluluklarının jeolojisi [The geology of the flysch assemblages in southern Bornova (İzmir)] Türkiye Jeoloji Kurumu Bülteni 23, 141–152 [in Turkish with English abstract] 163 SARI / Turkish J Earth Sci Plate Planktic foraminifera observed in the Gökdere area Abathomphalus mayaroensis (Bolli), Sample no: N-44, Abathomphalus mayaroensis (Bolli), Sample no: N-90, Abathomphalus mayaroensis (Bolli), Sample no: N-16 Contusotruncana contusa (Cushman), Sample no: N-17 Contusotruncana fornicata (Plummer), Sample no: N-130 Contusotruncana fornicata-patelliformis, Sample no: N-116 Contusotruncana patelliformis (Gandolfi), Sample no: N-102 Contusotruncana walfischensis (Todd), Sample no: N-92 Gansserina cf gansseri (Bolli), Sample no: N-53 10 Globotruncana arca (Cushman), Sample no: N-38 11 Globotruncana arca-orientalis, Sample no: N-97 12 Globotruncana bulloides Vogler, Sample no: N-206 13 Globotruncana stuarti (de Lapparent), Sample no: N-110 14 Globotruncana esnehensis Nakkady, Sample no: N-81 15 Globotruncana cf falsostuarti Sigal, Sample no: N-193 16 Globotruncana hilli Pessagno, Sample no: N-211 17 Globotruncana linneiana (d’Orbigny), Sample no: N-101 18 Globotruncana ventricosa White, Sample no: N-42 19 Globotruncanella havanensis (Voorwijk), Sample no: N-102 20 Globotruncanita conica (White), Sample no: N-20 21 Globotruncanita elevata (Brotzen), Sample no: N-99 22 Globotruncanita pettersi (Gandolfi), Sample no: N-193 23 Racemiguembelina fructicosa (Egger), Sample no: N-17 24 Rugoglobigerina milamensis Smith & Pessagno, Sample no: N-116 25 Rugoglobigerina pennyi Brönnimann, Sample no: N-52 26 Rugoglobigerina rugosa (Plummer), Sample no: N-212 27 Praegublerina acuta (de Klasz), Sample no: N-227 28 Multiserial heterohelicids, Sample no: N-101 29 Praegublerina robusta (de Klasz), Sample no: N-111 164 SARI / Turkish J Earth Sci 10 11 12 13 14 16 15 19 18 17 23 21 20 22 27 28 24 29 25 26 500 µm 165 SARI / Turkish J Earth Sci Plate Planktic foraminifera observed in the Işıklar area Acarinina cf strabocella (Loeblich & Tappan), Sample no: N-234, Globanomalina chapmani (Parr), Sample no: N-245, Globanomalina chapmani (Parr), Sample no: N-232, Globanomalina ehrenbergi (Bolli), Sample no: N-232, Igorina albeari (Cushman & Bermúdez), Sample no: N-232, gr Morozovella angulata (White) - Morozovella aequa (Cushman & Renz), Sample no: N-232, Morozovella acutispira (Bolli & Cita), Sample no: N-275, gr Morozovella angulata (White) - Morozovella aequa (Cushman & Renz), Sample no: N-233, Globanomalina cf pseudomenardii (Bolli), Sample no: N-236, 10 Globanomalina planoconica (Subbotina), Sample no: N-269, 11 Igorina albeari (Cushman & Bermúdez), Sample no: N-245, 12 Acarinina cf strabocella (Loeblich & Tappan), Sample no: N-231, 13 gr Morozovella conicotruncana (Subbotina) - Morozovella velascoensis (Cushman), Sample no: N-245, 14 Subbotina triangularis (White), Sample no: N-234, 15 Parasubbotina variospira (Belford), Sample no: N-231, 16 Subbotina velascoensis (Cushman), Sample no: N-245, 17 Contusotruncana plicata (White), Sample no: N-268, 18 Contusotruncana walfischensis (Todd), Sample no: N-268, 19 Globotruncana arca (Cushman), Sample no: N-268, 20 Globotruncana dupeublei (Caron et al.), Sample no: N-252, 21 Globotruncana linneiana (d’Orbigny), Sample no: N-249, 22 Globotruncana mariei Banner & Blow, Sample no: N-251, 23 Globotruncana orientalis El Naggar, Sample no: N-268, 24 Globotruncanella havanensis (Voorwijk), Sample no: N-268, 25 Globotruncanita stuarti (de Lapparent), Sample no: N-251, 26 Globotruncanita pettersi (Gandolfi), Sample no: N-268, 27 Rugoglobigerina hexacamerata Brönnimann, Sample no: N-246, 28 Rugoglobigerina milamensis Smith & Pessagno, Sample no: N-268, 29 Racemiguembelina fructicosa (Egger), Sample no: N-268, 30 Multiserial heterohelicids, Sample no: N-251, 166 SARI / Turkish J Earth Sci 10 11 13 12 17 15 14 18 16 19 22 20 21 23 25 24 29 28 26 27 30 500 µm 167 SARI / Turkish J Earth Sci Plate Planktic foraminifera observed in the Kocaỗay area Eoglobigerina cf spiralis (Bolli), Sample no: K-27 Globanomalina compressa (Plummer), Sample no: K-74, Globanomalina planoconica (Subbotina), Sample no: K-77, Igorina cf pusilla (Bolli), Sample no: K-27 Parasubbotina varianta (Subbotina), Sample No: K-85 Abathomphalus mayaroensis (Bolli), Sample no: K-22, Abathomphalus mayaroensis (Bolli), Sample no: K-92, Abathomphalus mayaroensis (Bolli), Sample no: K-59, Abathomphalus mayaroensis (Bolli), Sample no: K-88, 10 Contusotruncana contusa (Cushman), Sample no: K-88, 11 Contusotruncana contusa (Cushman), Sample no: K-59, 12 Contusotruncana contusa (Cushman), Sample no: K-21, 13 Contusotruncana fornicata (Plummer), Sample no: K-32, 14 Contusotruncana patelliformis (Gandolfi), Sample no: K-36, 15 Contusotruncana walfischensis (Todd), Sample no: K-32 168 SARI / Turkish J Earth Sci 10 11 13 14 12 15 500 µm 169 SARI / Turkish J Earth Sci Plate Planktic foraminifera observed in the Kocaỗay area Globotruncana esnehensis Nakkady, Sample no: K-88, Globotruncana hilli Pessagno, Sample no: K-32, Globotruncanita conica (White), Sample no: K-90, Globotruncanita pettersi (Gandolfi), Sample no: K-59, Globotruncanita stuarti (de Lapparent), Sample no: K-32, Rugoglobigerina pennyi Brönnimann, Sample no: K-49, Racemiguembelina fructicosa (Egger), Sample no: K-88, Multiserial heterohelicids, Sample no: K-21, Multiserial heterohelicids, Sample no: K-22, 10 Biserial heterohelicids, Sample no: K-32, 11 Dicarinella asymetrica (Sigal), Sample no: K-6, 12 Dicarinella concavata (Brotzen), Sample no: K-6, 170 SARI / Turkish J Earth Sci 11 10 12 500 µm 171 ... column of the matrix of the Bornova Flysch Zone around Bornova The column is based on data derived from all three areas The age of the Beytitepe Limestone and accompanying flysch- type rocks is late. .. in the Gökdere area and late Maastrichtian and late Palaeocene in the Işıklar area The age of the Beytitepe Limestone is late Maastrichtian-latest Palaeocene in the Kocaỗay area The age of the. .. foraminiferal biostratigraphy of the Beytitepe Limestone in the matrix of the BFZ around Bornova (İzmir) have revealed new data about the stratigraphy and age of the matrix (Figure 21) The age of the laminated

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