Eulepidina undetermined

Eulepidina sp. (Fig. 5H, I) REMARKS The identification is based only upon axial sections. The test is lenticular, its diameter ranges from 8.1 to 11.2 mm and its thickness from 1.1 to 1.7 mm. The equatorial chambers are polygonal in shape. DISCUSSION ON THE LARGER FORAMINIFERAL RECORD The study of Oligocene hyaline larger foraminifera, based on the biometric study of the nummulitids and lepidocyclinids, from western Taurids, gives insights on their palaeobiogeography in the Tethys. These groups show that they are closely related with the coeval assemblages known from the European basins. The larger benthic foraminiferal association from the Burdur-2 section correlates with the Shallow Benthic Zone (SB) 22, late Rupelian-early Chattian, based on the time range of Nummulites fichteli and Nephrolepidina praemarginata (Cahuzac & Poignant 1997). In the upper part of the Burdur-2 section, N. praemarginata and N. fichteli are associated with Operculina complanata, Eulepidina sp., Asterigerina sp., Planorbulina sp., and Amp- histegina sp. (Fig. 6). Some species of this assemblage have a longer stratigraphical range such as Operculina complanata which extends from the base of the Oligocene to the Late Miocene (Cahuzac & Poignant 1997). This evidence dates the Hayrettin Formation as late Rupelian-early Chattian (SB 22). In the Mediterranean realm, the evolutionary lineage of Nephrolepidina praemarginata - N. morgani - N. tournoueri is used as key criteria in Oligo-Miocene biostratigraphy. Although Douvillé (1908, 1925) reported N. praemarginata from the early Oligocene of Italy and from the Oligocene-Miocene transition in France, Cahuzac & Poignant (1997) demonstrated that this form is limited to the biozone SB 22. This taxon is poorly documented in Turkey. Some specimens of this species have been described in eastern Turkey Numerical SERIES STAGE Age (Ma) Zonation Larger foraminifera M. cushmani / mediterranea M. mediterranea E BURDIGALIAN SB25 N. tournoueri N PLURISPIRALLED MIOGYPSINA Miolepidocyclina spp. E C LOWER M. globulina Aust. howchini O 20.44 I M M. socini M. tani AQUITANIAN SB24 M. gunteri UNISPIRALLED MIOGYPSINA M. GUNTERI GROUP 23.03 M. complanatus / formosensis gr. Num. bouillei SB23 Borelis pygmaea Num. fichteli E M. complanatus N UPPER MIOGYPSINOIDES CHATTIAN E C SB22B LEPIDOCYCLINA O CYCLOCLYPEUS Num. vascus G I L 27.82 O Nephrolepidina praemarginata SB22A Bullalveolina bulloides Eulepidina formosoides LEPIDOCYCLINA BULLALVEOLINA LOWER RUPELIAN Borelis pygmaea Operculina complanata N. VASCUS Num. vascus SB21 Bullalveolina bulloides Num. fichteli N. FICHTELI 33.9 as Nephrolepidina partita based on the presence of coarse granules in the umbonal part of the test (Sirel 2003; Gedik 2014, 2015). According to Sirel (2003), N. praemarginata is associated in the Sarıbuğday section (Elazıǧ region, eastern Turkey) with Nummulites fichteli, N. vascus, N. cf. germanicus, Borelis pygmaea, B. inflata, B. merici, Operculina complanata, Neorotalia lithothamnica, N. pinarensis, N. cf. tectoria, N. viennoti, Austrotrillina asmariensis, Eulepidina sp., Thalmannita sp. and other smaller benthic foraminifera. This foraminiferal association corresponds with the biozones SB 21 and SB 22 of Cahuzac & Poignant (1997). It is present at the Rupelian/Chattian boundary (G. opima opima zone; P 21) in the Kelereşdere section (Muş region, eastern Turkey) which yielded N. partita, B. merici, B. cf. inflata, A. striata, Eulepidina sp. corresponding to the biozone SB 22. According to Özcan et al. (2009), in the Korkuteli area (namely Kabaktepe, Yuvaköy, Hacıbekar sections) and in the Tavas-Burdur Basin (Kızılcaağaç section), N. praemarginata is associated with Eulepidina dilatata, Operculina complanata, Nummulites kecskemetii, Heterostegina assilinoides. This foraminiferal association corresponds to SB 22B (early Chattian). As inferred by Gedik (2014, 2015), N. praemarginata is associated in the Develi section (W of Malatya, eastern Turkey) with Archaias kirkukensis, Austrotrillina asmarien- sis, A. brunni, Peneroplis cf. laevigatus, Nephrolepidina sp. This foraminiferal association corresponds with biozones SB 21, 22 of Cahuzac & Poignant (1997). It occurs at the Rupelian/Chattian boundary in the Edilme section (W Malatya, eastern Turkey) together with Heterostegina assilinoides, Nummulites cf. vascus, Eulepidina cf. formosoides, Risananeiza crassaparies, and Neorotalia lithothamnica corresponding to the biozone SB 22. An early Rupelian to early Chattian (SB 21-22B) age is known for Nummulites fichteli in Europe and Mediterranean area (Cahuzac & Poignant 1997; Sirel 2003; Gedik 2008). This species is known from the lower Oligocene shallow marine deposits in central and southern Iran (SB 21-22A) (Ehrenberg et al. 2007; Van Buchem et al. 2010; Yazdi- Moghadam 2011). In the Denizli Basin, which is located adjacent to the study area, Nummulites fichteli is associated with Nummulites vascus and Operculina complanata, indicating a Rupelian-early Chattian age (SB 21-22; Gedik 2008). Nummulites vascus is a key species for the Oligocene but we did not find it in the examined strata. CONCLUDING REMARKS Southwestern Anatolia has been under the influence of an extension regime since the Oligocene (Seyitoğlu et al. 2004; Karadenizli et al. 2009, 2017), with thick sequences deposited in graben basins opened by normal faults.An example of this system is seen in the Burdur region where a 840 m thick fan sequence developed in a graben basin (Fig. 3). A simple stratigraphic succession developed in the Burdur Fan during the Oligocene, which consists of the Çardak and Hayrettin formations. The ten lithofacies have been grouped into four facies associations (Fig. 2) based on their lateral and vertical relations (Fig. 3). Sedimentary environments of these facies associations show that the Burdur region was invaded by a shallow sea from the west, and that the sea penetrated into Anatolia. The basin fill is controlled by the Burdur Normal Fault which formed the southern edge of the basin. Along this margin, alluvial-fluvial fan and fan-delta facies associations developed, while in the northern part sedimentation was limited to fan-delta successions (Fig. 3). These facies mainly consist of coarse-grained sediments derived from the Taurus tectonic unit. There is no evidence for sediment derivation from the metamorphics of the Menderes Massif. A beach facies is present towards the center of the basin (Fig. 3). Ramp-type carbonate platforms also developed depending on the shelf topography in the intervals when clastic input was minimal (Fig. 3). A moderately diverse and well-preserved assemblage of hyaline and porcellaneous larger foraminifera was found in the late Rupelian-early Chattian shallow marine deposits of the Hayrettin Formation in the Burdur Basin, SW Anatolia. The foraminiferal association includes 7 genera. Larger foraminifera from the Hayrettin Formation, classified under the genera Nummulites, Operculina, Nephrolepidina, Eulepidina, Planorbulina, Amphistegina and Asterigerina show close similarity to the coeval assemblages already known from the European and circum-Mediterranean marine sedimentary sequences. Their western Tethyan affinity allowed us to apply the standard biozonation scheme (SB zonation) for our study area in SW Turkey. The late Rupelian-early Chattian age, i.e., SB 22 Zone of Cahuzac & Poignant (1997) for the Burdur-2 section is documented by the presence of Nephrolepidina praemarginata, together with Nummulites fichteli. This evidence dates the Hayrettin Formation as late Rupelian-early Chattian (SB 22).Published as part of Gedik, Fatma & Karadenizli, Levent, 2021, Oligocene larger benthic foraminifera and sedimentation of the Burdur Basin, SW Anatolia, Turkey, pp. 377-389 in Geodiversitas 43 (13) on pages 383-387, DOI: 10.5252/geodiversitas2021v43a13, http://zenodo.org/record/503692

Operculina complanata

Operculina complanata (Defrance, 1822) (Fig. 5A, B) Lenticulites complanata Defrance, 1822: 453. Operculina complanata – Souaya 1963: pl. 53, figs 1, 2. — Cherif 1980: pl. I, figs 4, 10; pl. II, figs 1, 5. — Abdelgany 2002: pl. II, figs 2-4. — Sirel 2003: pl. III, figs 1-9. — Gedik 2008: pl. 2, figs 6-10. REMARKS The test is thin, bilateral and symmetric. Its diameter ranges from 2.5 to 2.9 mm, and the thickness from 0.4 to 1.8 mm. The test is planispiral and evolute, with numerous narrow chambers in many rapidly expanding whorls, so that the height of the chambers may be five times the width of the chambers (Fig. 5A, B). The proloculus is spherical and small (90 µ diameter).Published as part of Gedik, Fatma & Karadenizli, Levent, 2021, Oligocene larger benthic foraminifera and sedimentation of the Burdur Basin, SW Anatolia, Turkey, pp. 377-389 in Geodiversitas 43 (13) on page 383, DOI: 10.5252/geodiversitas2021v43a13, http://zenodo.org/record/503692

Grands foraminifères benthiques de l’Oligocène et sédimentation du bassin de Burdur, sud-ouest de l’Anatolie, Turquie

Cette étude se concentre sur les successions de l’Oligocène du bassin de Burdur, au sud-ouest de l’Anatolie (Turquie), qui contiennent principalement des calcaires siliciclastiques avec de grands foraminifères benthiques. Les coupes des niveaux oligocènes de Burdur-1 et de Burdur-2 sont décrites et ont été échantillonnées pour la lithologie, la biostratigraphie, l’analyse des microfaciès et le contenu paléontologique. Les plus grands foraminifères benthiques ont été principalement échantillonés dans les calcaires de la partie supérieure de la coupe de Burdur-2. L’analyse des lames minces de l’assemblage de grands foraminifères benthiques révèle que la partie supérieure de la coupe de Burdur-2 contient Nummulites fichteli Michelotti, 1841, Operculina complanata (Defrance, 1822), Nephrolepidina praemarginata (Douvillé, 1908), Eulepidina sp, Planorbulina sp., Amphistegina sp. et Asterigerina sp. Cette association de foraminifères représente la Zone de foraminifères benthiques peu profonds n°22 (SBZ 22) d’âge Rupélien-Chattien inférieur. L’analyse sédimentologique des coupes de Burdur-1 et Burdur-2 a révélé une association de conglomérat massif non organisé, de grès à litages parallèles, de mudstone massif, de conglomérat massif, de grès massif, de conglomérat organisé bien trié, de grès à lits parallèles bien trié et de faciès calcaire à lits parallèles contenant des microfossiles. Les communautés de faciès carbonatés de type éventail alluvial/rivière, fan-delta, plage et plateforme peu profondes ont été identifiées par corrélation latérale et verticale des faciès. Il en est déduit que le cône alluvial de Burdur s’est développé dans un bassin de Graben qui s’est ouvert et a été inondé par une branche de l’océan Téthys qui a envahi le sud-ouest de l’Anatolie pendant l’Oligocène.This study focuses on the Oligocene successions that contain predominantly siliciclastic, limestones with larger benthic foraminifera in the Burdur Basin of southwest Anatolia, Turkey. The Burdur-1 and Burdur-2 sections in the Oligocene deposits are described sedimentologically and were sampled for lithology, biostratigraphy, microfacies analysis and fossil content. Larger benthic foraminifera were mainly recovered from limestones in the upper part of the Burdur-2 section. Thin-section analysis of the larger benthic foraminiferal assemblage reveals that the upper part of the Burdur-2 section includes Nummulites fichteli Michelotti, 1841, Operculina complanata (Defrance, 1822), Nephrolepidina praemarginata (Douvillé, 1908), Eulepidina sp., Planorbulina sp., Amphistegina sp., and Asterigerina sp. This foraminiferal association represents the Shallow Benthic Foraminifera Zone 22 (SBZ 22) of Rupelian-early Chattian age. Sedimentological analysis in the Burdur-1 and Burdur-2 sections has revealed an association of massive-unorganized conglomerate, parallel-bedded sandstone, massive mudstone, graded-massive conglomerate, graded-massive sandstone, well-sorted organized conglomerate, well-sorted parallel-bedded sandstone and microfossil-bearing parallel-bedded limestone facies. Alluvial fan / river, fan-delta, beach and shallow shelf carbonate facies communities were identified by lateral and vertical correlation of facies. It is concluded that the large Burdur Fan developed in a graben basin that opened and was flooded by a branch of the Tethyan Ocean that invaded southwest Anatolia during the Oligocene.</p

Nummulites fichteli Michelotti 1841

Nummulites fichteli Michelotti, 1841 (Fig. 4 A-J; 5C, J) Nummulites fichteli Michelotti, 1841: 296, figs 7a, b. — Cole 1960: pl. 3, figs 9-18. — Schaub 1981: pl. 50, figs 5-18. — Sirel 2003: pl. II, figs 12-19. — Gedik 2008: pl. 1, figs 1-14, 22. Nummulites intermedius D’Archiac, Sirel & Gündüz, 1976: pl. I, figs 5-9. REMARKS This reticulate species belongs to the N. fabianii lineage. This form has inflated lenticular shell with rounded periphery. The diameter of test ranges from 2 to 6.4 mm and the thickness from 0.5 to 1.8 mm. The test surface is covered with a reticulation that has rectangular or subrectangular mesh (Fig. 4A, C-E; Fig. 5C). The large microsphere (diameter 0.3 to 0.4 mm) is followed by the regular coiled whorls.Published as part of Gedik, Fatma & Karadenizli, Levent, 2021, Oligocene larger benthic foraminifera and sedimentation of the Burdur Basin, SW Anatolia, Turkey, pp. 377-389 in Geodiversitas 43 (13) on page 383, DOI: 10.5252/geodiversitas2021v43a13, http://zenodo.org/record/503692

Nephrolepidina praemarginata

Nephrolepidina praemarginata (Douvillé, 1908) (Fig. 5 D-G) Lepidocyclina praemarginata Douvillé, 1908: 91-92, figs 1, 2, 4a. Nephrolepidina praemarginata – Douvillé 1924: 51-123, pl. 6, figs 4, 6. — Gomez Llueca 1929: 1-400, pl. 32, figs 4-10. — Flandrin 1935: 251-272, pl. 15, figs 14-18. — Poignant 1967: 197-211, pl. V, fig. 2. — Gedik 2014: 101, pl. 6, figs 1-14. REMARKS The identification is based only upon axial sections. The small test is inflated, lenticular with a central umbo, so that the shell is thicker towards the center. The diameter of the test ranges from 1.5 to 2.1 mm and the thickness from 0.6 to 0.9 mm. The large, central umbo consists of numerous small pustules (Fig. 5E, G). Lateral chambers are numerous at the surface of test and rosette shaped, and this feature forms a comb-like surface appearance (Fig. 5E). The embryo consists of subspherical small protoconch (diameter 0.25 mm) and reniform deuteroconch (diameter 0.22 mm). Secondary chambers are very small and their sizes are almost equal to each other. The equatorial chambers are subrectangular or rhombic in outline. There are 6-7 orders of lateral chambers in the center of the test.Published as part of Gedik, Fatma & Karadenizli, Levent, 2021, Oligocene larger benthic foraminifera and sedimentation of the Burdur Basin, SW Anatolia, Turkey, pp. 377-389 in Geodiversitas 43 (13) on page 383, DOI: 10.5252/geodiversitas2021v43a13, http://zenodo.org/record/503692

The position of Akkașdağı mammal locality in the neo-tectonic framework of Çankırı basin, Turkey

Seyitoğlu, Gürol, Karadenizli, Levent, Kazanci, Nizamettin, Sen, Sevket (2005): The position of Akkașdağı mammal locality in the neo-tectonic framework of Çankırı basin, Turkey. Geodiversitas 27 (4): 519-525, DOI: http://doi.org/10.5281/zenodo.537443

3D model related to the publication: Orliac M.J., Karadenizli L., Antoine P.-O., Sen S. 2015. Small suids (Mammalia, Artiodactyla) from the late Early Miocene of Turkey and a short overview of Early Miocene small suoids in the Old World.

International audience3D model related to the publication: Orliac M.J., Karadenizli L., Antoine P.-O., Sen S. 2015. Small hyotheriine suids (Mammalia, Artiodactyla) from the late early Miocene of Turkey and a short overview of early Miocene small suoids in the Old World. METHODS Before restoration of the fragmentary cranium n° SMT-1, a portion of the left upper molar raw (broken appart) was scanned in order to visualize the morphology of the roots of the molars (Orliac et al., 2015: fig. 3). AVIZO 6.3 (Visualization Sciences Group) software was used to produce the 3D surface model. This 3D model is provided in .ply format, and as such can be opened with a wide range of freeware. ACKNOWLEDGEMENT

Late Miocene−early Pliocene rodents and lagomorphs (Mammalia) from the southern part of Çankırı Basin, Turkey

International audienc

Small hyotheriine suids (Mammalia, Artiodactyla) from the late early Miocene of Turkey and a short overview of early Miocene small suoids in the Old World

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Çameli Havzası'nın sedimantolojik incelemesi (Geç miyosen-geç pliyosen, Denizli, GB Anadolu)

Çalışma, batı Anadolu grabenlerinden biri olan Çameli Havzası tortul dolgusunun sedimantolojik yöntemlerle incelenmesini ve böylece oluşumundan günümüze kadar geçirdiği jeolojik evrimi açıklamayı amaçlar. Havzanın temelini oluşturan Likya naplarının yerleşimi Geç miyosen başında tamamlanır. Bu yerleşimin ardından Çameli havzası, Memeli fosil bulgularına göre, Geç Miyosen'de (10.8-9.7 My), doğuda Dirmil fayı batıda ise Bozdağ fayı denetiminde graben havzası tarzında açılmaya başlar ve dolgulanması Geç Pliyosen'e kadar sürer. Alüvyon yelpazesi, flüvyal ve gölsel tortullardan oluşan, havzanın ilk ürünleri içinde yaygın olarak görülen büyüme fayları, genişlemenin yoğun bir şekilde devam ettiğini gösterir. Oldukça etkin olan bu genişleme evresi memeli fosillerine göre Orta Piliyosen'e (3,8-3,2 My) kadar devam eder ve bu zamanda havza, bir traverten seviyesi ile belirgin olan büyük bir faylanma ile ikiye bölünür (Sarıkavak-Kumaşfarı fayı). Bu dönemden sonra genişleme tektoniğinin etkinliği nispeten azalır ve havza büyük bir göl ortamına dönüşür. Gölsel tortullar havza kenar fayları dahil, havzayı sonradan ikiye bölen fayı da aşar ve bu dönem memeli fosillerine göre Geç Piliyosen'e (3,5-2,5 My) kadar sürer. Bu göl ortamı kenarlardan yelpaze deltaları ve deltaların ilerlemesi ile tortulla doldurularak sığlaşır ve aynı zamanda havzanın merkez kesimlerinde sığ göl karbonatları depolanır. Havza bu dönemden sonra kenar faylarına paralel olmak üzere ve bir traverten seviyesi ile belirgin olan iki ayrı fay sistemi (Alcı-Kelekçi ve Uzunoluk-Çameli Fayları) ile en Geç Pliyosen sonunda yeniden kırılır. (3,0-2,0 My) Havzanın en son ürünleri bu faylanma evresinin neden olduğu alüvyon yelpazesi tortullarıdır. Bu kırılma evresinden sonra depolanan tortullar içinde görülen büyüme fayları genişlemenin yeniden etkinlik kazandığını gösterir. Bu olayın ardından Çameli Havzası'nın ve dolayısı ile Çameli Formasyonu'nun oluşumu tamamlanır