The Paleogeographic and Paleoecologic Characteristics of the Miocene Aged Molluscan Fauna in Antalya and Kasaba Basins (West- Central Taurus, Sw Turkey)

Home , Anadara, Anadara diluvii, Parthenina interstincta

Mineral Res. Expl. Bull, 126, 11-42, 2003

THE PALEOGEOGRAPHIC AND PALEOECOLOGIC CHARACTERISTICS OF THE MIOCENE AGED MOLLUSCAN FAUNA IN ANTALYA AND KASABA BASINS (WEST- CENTRAL TAURUS, SW TURKEY)

Yeşim İSLAMOĞLU* and Güler TANER**

ABSTRACT.- Throughout this study, the paleogeographical and paleoecological characteristics of the samples of the Miocene aged molluscan fauna have been described which identified in Antalya and Kasaba basins, in west and central Taurus. In addition to the presence of the species belonging to Tethys realm such as Cingula ventri- cosella Cerulli-lrelli, Cerithium appenninicum dertosulcata Sacco, and Xenophora infundibulum (Brocchi), the Hydrobia (Hydrobia) frauenfeldi (Hoernes), Pirenella gamlitzensis gamlitzensis (Hilber), Irus (Paphirus) gregarius Partsch and Glossus (Cytherocardia) cf. deshayesi (Kutassy) type species known in marinal stages of Central Paratethys are also found. Similarly, in Kasaba basin; together with the presence of the Turritella terebralis turritissima Sacco, Conus antiquus Lamarck, Conus clavatulus d'Orbigny, Pecten benedictus Lamarck and Pecten fuschi Fontannes known only in the Tethys province, the Cerithium zejsneri Putsch, Divaricella ornata subornata Hilber, Pitar (Paradione) lilacinoides Schaffer and Venus (Antigona) burdigalensis producta Schaffer type species restricted to Central Paratethys are found. Besides, it is known that, in the investigated basins, the rest of the fauna as a whole is widespread in both provinces. In order to make contribution to the environmental interpretations, the geochemical analyses have been carried out on 14 and 16 fossil casts from Antalya and Kasaba basins respectively. In this way, the fossil casts with aragonite composition have low Mg content. The 1000 Sr/Ca ratios are propotional to salinity. Consequently, the salinity of seawater in Miocene aged Antalya basin is lower than that of Kasaba basin during Upper Burdigalian (Karpatian- Ottnangian). This result is completely in agreement with the known paleoecological characteristics of the fauna. The Antalya and Kasaba basins are similar to intermontane molasse basins in the Alps and situated in the same orogenic belt. The all paleogeographic and paleoecological results indicate that, during the evolution of the Tethys, the similar events and Paratethys like environmental conditions were developed. For this reason, the stage names have been used mutually for the investigated basins. The determination of regional stages seems to be a need for the region as having its own special conditions.

INTRODUCTION THE PALEOGEOGRAPHIC AND PALEO- The examined samples have been obta- ECOLOGICAL CHARACTERISTICS OF ined from the Miocene Antalya and Kasaba THE IDENTIFIED MOLLUSCAN FAUNA IN basins located in the east of Western Taurus INVESTIGATED AREAS and west of Central Taurus respectively (Fig. Antalya Miocene basin 1). This study aims to discuss the previously identified and determined age intervals of In this basin, 84 molluscan species were Molluscan species (İslamoğIu, 2001-2002; identified and detailed stratigraphy of the ba- İslamoğIu and Taner, 2002) together with sin has been established (İslamoğIu 2001- their paleogeographic distributions and stra- 2002). In this way, the paleogeographical and tigraphical levels. paleoecological characteristics of the species 12 Yeşim İSLAMOĞLU and Güler TANER

belonging to class Bivalvia and Gastropoda pınar limestone, Altınkaya formation and Ak- identified in the Sevinç conglomerate, Oyma- su formation of the basin are as following:

Fig. 1- Structural units in Antalya and Kasaba basins and in surrounding areas. A: Antalya Miocene basin, B: Kasaba Miocene basin, 1- Plio-Quaternary, 2- Miocene aged molasse basin, 3- Tavas- Burdur post-tectonic molasse basin, 4- Ophiolite nappes, 5- Lycian nappes, 6- Beyşehir -Hoyran - Hadim nappes, 7- Antalya nappes, 8- Bey- dağları autochthon, 9- Anamas- Akseki autochthon, 10- Alanya nappe, 11- Menderes massive (from Şenel, 1997). THE MOLLUSCAN FAUNA AND STRATIGRAPHY OF ANTALYA MIOCENE BASIN 13

The Pecten (Aequipecten) scabrella bol- la gamlitzensis gamlitzensis (Hilber), Irus lenensis (Mayer) yielding Upper Burdigalian (Paphirus) gregarius Partsch, Hydrobia age has been identified in Sevinç conglome- (Hydrobia) frauenfeldi (Homes) like species rate and reflects the Tethys province and nor- are belonging to Central Paratethys (Table 3 mal sea water salinity. a-b). The samples indicating normal sea water salinity are Turritella (Turritella) turris Bas- The Pecten fuschi Fontannes, Anadara terot, Turritella (Archimediella) bicarinata (Anadara) diluvii pertransversa Sacco, Cardi- Eichwald, Triphora adversa miocenica Coss- tamera (Lazariella) striatellata (Sacco), Cardi- mann ve Peyrot, Conus conoponderosus ocardita cf. monilifera (Dujardin), Cardium (Sacco), Polinices (Polinices) redemptus kunstleri Cossmann ve Peyrot, Venus (Ventri- (Michelotti) which are wellknown both in coloidea) multilamella (Lamarck), Codakia le- Tethys and Central Paratethys facies (Table 3 onina (Basterot), Athleta ficulina (Lamarck), a-b and 4 a-b). Most of the mollusc species Tellina (Peronaea) planata Linne are found in in Altınkaya formation are present in both Lo- Upper Burdigalian stage in Oymapınar limes- wer - Middle Miocene stages of Tethys and tone and they are also known to be present in marinal Ottnangian, Karpatian and Badenian Ottnangian and Karpatian stages of Central stages of Central Paratehys. These are Turri- Paratethys. However, the Pecten fuchsi Fon- tella (Turritella) turris Basterot, Tinostoma wo- tannes, Chlamys (Aequipecten) scabrella bol- odi (Homes), Nehtina picta Ferussac, Alvania lenensis (Mayer) are only present in Tethys (Alvania) venus (d'Orbigny), Terebralia biden- (Table 1a-b, 2 a-b and 4 a-b). The all identifi- tata cingulatior Sacco, Terebralia lignitara ed fossil samples in this formation represent (Eichwald), Polinices (Polinices) redemptus the environment having the normal sea water (Michelotti), Natica millepunctata Lamarck of salinity. class Gastropoda and Pelecyora (Cordiopsis) The abundant molluscan fauna yielding islandicoides Lamarck, Gastrana fragilis Lin- Upper Burdigalian - Langhian (Ottnangian - ne, Sanguinolaria (Soletellina) labordei (Bas- Karpatian - Lower Badenian) age and refleo terot), Crassostrea gryphoides (Schlotheim) ting brackish water - marine environment has of class Bivalvia (Table 1 a-b, 2 a-b, 3 a-b and been found in Antalya Basin within the units of 4 a-b). Except these species, the Cerithium Altmkaya formation, the class Gastropoda (Tiaracerithium) pseudotiarella (d'Orbigny) and including Pirenella gamlitzensis gamlitzensis Terebralia subcorrugata d'Orbigny are only (Hilber), Terebralia bidentata cingulatior Sac- found in Lower Miocene in Tethys; whereas co, Terebralia lignitara (Eichwald), Cerithium Hydrobia (Hydrobia) frauenfeldi frauenfeldi (Tiaracerithium) pseudotiarella (d'Orbigny), (Homes), Irus (Paphirus) gregarius Partsch, Nehtina picta (Ferussac), Hydrobia (Hydro- Pirenella gamlitzensis gamlitzensis (Hilber), bia) frauenfeldi (Homes) and Gastrana fragilis Glossus (Cytherocardia) cf. deshayesi (Ku- (Linne), Pelecyora (Cordiopsis) islandicoides tassy) are the species present in Ottnangian - (Lamarck), Irus (Paphirus) gregarius Partscji Sarmatian epochs of Central Paratethys of Bivalvia class have been found (Table 2 a (Table 2 a-b and 3 a-b). Based on this, it is ac- b and 3 a-b). These species adapted an envi- cepted that, it is better to use Upper Burdiga- ronment with relatively lower salinity than that lian together with Ottnangian - Karpatian sta- of normal sea water. Of these fossils, Pirenel- ges for the age of the Altınkaya formation. 14 Yeşim İSLAMOĞLU and Güler TANER THE MOLLUSCAN FAUNA AND STRATIGRAPHY OF ANTALYA MIOCENE BASIN 15 16 Yeşim İSLAMOĞLU and Güler TANER THE MOLLUSCAN FAUNA AND STRATIGRAPHY OF ANTALYA MIOCENE BASIN 17 18 Yeşim İSLAMOĞLU and Güler TANER

Table 3 a- The paleogeographic and stratigraphical distributions of the species of Class Gastropoda identified in Antalya and Kasaba Miocene basins. 1: Hoernes (1856), Papp (1952), Steininger et al. (1978); 2: Strausz (1966), 3: Friedberg (1914 1954-55), 4: Moisescu (1955), Hinculov (1968); 5: Kojumdgieva and Strachimirov (1960); 6: Iliana (1993). THE MOLLUSCAN FAUNA AND STRATIGRAPHY OF ANTALYA MIOCENE BASIN 19

Table 3 b- Continue 3 a- 7: Cossmann-Peyrot (1919 -1924), Vignal (1910); 8: Sacco (1895 -1896), Venzo and Pelosio (1963), Greco (1970); 9: Wenz (1938-44), Malatesta (1960-1974); 10: Erünal-Erentöz (1958); 11: İslamoğlu (2001-2002) and 12: İslamoğlu and Taner (2002). 20 Yeşim İSLAMOĞLU and Güler TANER

Table 4 a- The paleogeographic and stratigraphical distributions of the species of Class Gastropoda identified in Antalya and Kasaba Miocene basins. 1: Hoernes (1856), Steininger et al. (1971); 2: Csepreghy-Meznerics (1954), Strausz (1966"), 3: Kojumdgieva and Strachimirov (1960); 4: Hinculov (1968); 5: Friedberg (1911-28, 1954), 6: Iliana (1993). THE MOLLUSCAN FAUNA AND STRATIGRAPHY OF ANTALYA MIOCENE BASIN 21

Table 4 b- Continue 4 a- 7: Cossmann-Peyrot (1924), Peyrot (1928,1931,1932); 8: Malatesta (1960,1974); 9: Sacco (1891,1893,1904), Moroni (1953), Venzo and Pelosio (1966), Hall (1964), Robba (1968), Davoli (1972-1990); 10 and 11: Malatesta (1960,1974); 12: Erünal-Erentöz (1958); 13: İslamoğ- lu (2001-2002) and 14: İslamoğlu and Taner (2002). 22 Yeşim İSLAMOĞLU and Güler TANER

In Aksu formation, the Gibbula (Gibbula) oporcellus Sacco, Odostomia (Megastomia) maga Linne, Hadriani becki (Michelotti), Mit- conbidea (Brocchi), Gibberulina (Gibberulina) rella (Mitrella) liguloides (Doderlein), Mange- philippi (Monterosato), Gibbula (Gibbula) ma- lia cf. brachystoma (Philippi), Cerithium ap- ga (Linne) and Alvania vehus (d'Orbigny) indi- penninicum dertosulcata Sacco, Odostomia cate high sea water salinity and subtropical (Megastomia) conoidea (Brocchi), Xenophora climatic conditions. Consequently, it can be infundibulum (Brocchi), Arcularia (Arcularia) deduced that, the climatic conditions were ringicula (Bellardi), Charonia stefaninii (Mon- better and warmer in Antalya Miocene basin tarano), Hinia (Uzita) porrecta (Bellardi), relative to Lower and Middle Miocene. Cypraea (Bernaya) fabagina mioporcellus Sacco, Conus conoponderosus (Sacco) of Kasaba Miocene basin class Gastropoda and Megaxinus transversus The total 68 mollusc species have been rotundula Sacco of class Bivalvia are the spe- identified in Kasaba Miocene basin and the cies appeared at the beginning of the Torto- detailed stratigraphy of the basin has been nian only in Tethys (Table 1 a-b, 3 a-b and 4 established (İslamoğIu and Taner, 2002). The a-b). Upper Burdigalian - Langhian (Upper Eggen- Apart from these, the species like Alva- burgian - Karpatian) aged whole mollusc fa- nia (Alvania) curta (Dujardin), Mitra (Mitra) fu- una identifed in Kasaba basin reflects normal siformis Brocchi, Conus mercati Brocchi, Ast- sea water salinity in subtropical climate belt raea (Bolma) rugosa (Linne), Chrysallida and shallow marine environmental conditions (Parthenina) interstincta (Montagu), Linga being different from Antalya Miocene basin. (Linga) columbella strictula (Sacco) have be- The stratigraphic and paleogeographic cha- en appeared since Burdigalian. Of these Ast- racteristics of the fauna are as follows: raea (Bolma) rugosa (Linne), Chrysallida In stratigraphic sections measured within (Parthenina) interstincta (Montagu), Linga Ucarsu formation the identified species which (Linga) columbella strictula (Sacco) are also are Turritella terebralis turritissima Sacco, identified in marinal Lower Badenian stage of Central Paratethys (Table 1 a-b and 3 a-b). Turritella terebralis subagibbosa Sacco, Tur- Although some of the species identified in ritella (Peyrotia) desmarestina Basterot, Cas- this formation have distribution in Lower and sidaria tauropomum (Sacco), Turbonilla (Mor- Middle Miocene of Central Paratethy, they mula) aturensis (Cossmann ve Peyrot), Vexil- can be totally correlated with Tethys in Upper lum (Uromitra) pluricostata percostulata (Sac- Miocene. For this reason, the Lower Tortoni- co) of class Gastropoda and Pecten zizinae an stage has only been used for the Aksu for- Blanckenhorn, Cardium praeaculeatum mation. (Holzl) and Pitar (Paradione) lilacinoides In fauna identified in Aksu formation, the (Schaffer) of class Bivalvia became totally ex- presence of the species like Strombus tinct at the end of Burdigalian (Table 2 a-b, 3 (Strombus) bonellii Brongniart, Strombus co- a-b and 4 a-b). These species are absent in ronatus Defrance, Erato (Erato) laevis elon- Langhian (Lower Badenian) aged Kasaba for- gata Sacco, Cypraea (Bernaya) fabagina mi- mation. THE MOLLUSCAN FAUNA AND STRATIGRAPHY OF ANTALYA MIOCENE BASIN 23

In Ugarsu formation, mostly, the Turritel- Cypraea (Bernaya) fabagina Lamarck, Clava- la terebralis turritissima Sacco, Turritella te- tula asperulata (Lamarck) of class Gastropo- rebralis subagibbosa Sacco, Clavatula (Cla- da and Nemocardium spondyloides hercule- vatula) calcarata francisci (Toula) and Conus um Dollfuss-Cotter-Gomez, of class Bivalvia mercati Brocchi of class Gastropoda and became extinct at the end of Middle Miocene Pecten zizinae Blanckenhorn, Glycymeris (Table 2 a-b, 3 a-b and 4 a-b). (Glycymeris) inflatus (Brocchi) of class Bival- The most of the species identified in Ka- via are found only Tethys (Table 1 a-b, 3 a-b saba formation are present in marinal stages and 4 a-b). However, the Conus (Chelyconus) of Central Paratethys with Tethys fauna simi- puschi Michelotti, Ancilla (Baryspira) glandi- lar in Ugarsu formation. As mentioned above, formis (Lamarck), Turritella (Haustator) tri- except these, the only Cerithium zejsneri cincta (Borson), Cypraea (Bernaya) fabagina (Pusch) and Divaricella ornata subornata Hil- Lamarck, Natica millepunctata Lamarck, Tur- ber type species are found in lower Badenian ritella (Turritella) turns Baste rot, Cypraea stage of Central Paratethys (Table 2 a-b and (Bernaya) fabagina (Lamarck) and Athleta fi- 3 a-b). Based upon these data, the age of the culina (Lamarck) of class Gastropoda and Kasaba formation has been accepted as Anadara (Anadara) diluvii (Lamarck), Langhian (Lower Badenian). Additionally, this Glycymeris (Glycymeris) cor (Lamarck), fauna is typically in marine character and indi- Glycymeris pilosa deshayes/ (Mayer), Callista cates the presence of a stable marine envi- (Callista) chione (Linne) and Nemocardium ronment with normal salinity. spondyloides (Hauer) of class Bivalvia type species are found in some or all marinal sta- THE DISCUSSION OF THE CHRONOSTRA- ges Eggenburgian, Karpatian and Badenian TIGRAPHIC LEVELS AND PALEOGEOG- of both Tethys and Central Paratethys (Table RAPHICAL DISTRIBUTIONS OF THE USED 1 a-b, 2 a-b, 3 a-b and 4 a-b). In addition, a few species belonging to only the Eggenbur- STAGES gian stage of Central Paratethys such as, Pi- In order to discuss and understand better tar (Paradione) lilacinoides (Schaffer) and the paleogeographic interpretations of the Venus (Antigona) burdigalensis producta mollusc fauna present in the basins, it is ne- Schaffer have been also found (Table 1 a-b). cessary to give some knowledge mentioned As far as the paleogeographical characteris- below. tics of the molluscan fauna are considered, it Regional changes in terrain have been is necessary to use the Upper Burdigalian developed in Tethys realm and surrounding stage with Upper Eggenburgian- Karpatian areas since the beginning of Cenozoic due to stages. effect of neotectonism (Steininger et al., In Kasaba formatipn, the species appe- 1985). These changements have caused the ared firstly at the beginning of Middle Mioce- seperation of the Tethys since Paleocene; as ne are Cerithium zejsneri Pusch and Divari- a result of this event, the new marine realms cella ornata subornata Hilber of class Gast- and gateways were developed (Steininger et ropoda. These are the species which belon- al., 1985). The continuation of this event has ging to marinal Lower Badenian stage of been increased since the beginning of Neoge- Central Paratethys (Table 2 a-b and 3 a-b). ne; consequently, the newly formed marine The Turritella (Turritella) turns Baste rot, realms evolved differently and each of them 24 Yeşim İSLAMOĞLU and Güler TANER

became a distinct isolated small basin. At the names were suggested. Especially, before same time, the connection of the marine re- the Central Paratethys concept is established, alm, existed at the south, with (Tethys) Atlan- The Tethys stages were used and later, it was tic, Indo-Pasific and northern inland seas understood that not only the facies and faunal (Central and Eastern Paratethys) was conti- content but also the stratigraphic levels and nued by limited sea ways and later, discon- ages were inconsistent, for this reason, the nected firstly with Paratethys and the other regional new stages have been identified. The oceans (Steininger et al., 1985; Rögl, 1998). stage names previously used in the old litera- ture and correlative regional new stage na- This geodinamic evolution in the region mes are shown in Fig. 2. caused the development of paleobiogeograp- hic and paleogeographic differences in three For example, the new idea and discussi- different regions within the Alpine - Caucasus ons are suggested that the widely used and orogenic belt. These regions are named as; known Aquitanian and Burdigalian stages of Tethys in the south, Central Paratethys for Lower Miocene are not consistent for Tethys. Central Europe and Eastern Paratethys bet- The Carloni et al., (1971) claimed that, the ween eastern Europe and Caucasia (Nevess- Aquitanian and Burdigalian are local facies kaya et al., 1975; Papp, 1981; Steininger and and not to have being a stratotype, also, Ge- Rogl, 1984; Steininger et al., 1985; Rogl, lati and Robba (1975) pointed out that, the 1998). stratotypes in which these stages identified are not belonging to the Mediterranean, ins- It is necessary to research the causes of tead, related to the Atlantic and no marine ga- facies and faunal changes, their relationships teway existed between two oceans during and evolution developed in different regions. For this purpose, the detailed biostratigraphic Early Miocene. They also claimed that, the and chronostratigraphical studies have been type sections of the Oligocene - Miocene is carried out in Tethys, Central Paratethys and somewhat problematic. Based on these, Ge- Eastern Paratethys and the best stratotypes lati and Robba (1975) identified a new stra- representing the regions were identified. The totype including the whole Lower Miocene in new stratotypes have also been suggested Piedmonte basin located at north of Italy in whenever the problems come to existence Tethys realm and suggested a new stage na- correlation. By using the biostratigraphy and me as "Cortemilian". magnetostratigraphy together with radiomet- The Helvetian stage stratotype is in Swit- ric age methods, the correlation tables among zerland in Central Paratethys, known also regions were worked out and the time equiva- western Paratethys. The Helvetian is known lents of stages and their relations were estab- to represented typical mollusc species depic- lished (Cicha et al., 1969; Carloni et al., 1971; ting brackish- marine facies (Rutsch, 1971). Nevesskaya, et al., 1979; Papp, 1981; Ste- The Helvetian stage including endemic fauna ininger and Rögl, 1984; Steininger et al., and developed different facies, was widely 1985). used both in Tethys and Central Paratethys; The regional stage names used in prepa- however, due to correlation problems, it was ration of correlation charts have allowed in- decided not to be used for both realms and vestigators to have different opinions and ma- which stages could be used instead, was the ke discussions. Some of the stage names we- subject of discussion (Steininger and Rögl, re left to use and instead the new stage 1979). THE MOLLUSCAN FAUNA AND STRATIGRAPHY OF ANTALYA MIOCENE BASIN 25 26 Yeşim İSLAMOĞLU and Güler TANER

Before the establishment of Central Pa- In the investigated basins, the most of ratethys concept, the Tethyian stages or local the identified mollusc fauna has wide distribu- stages were used. Throughout the progressi- tion both in Tethys and Central Paratethys. ve studies, it was deduced that, the most of Furthermore, the specie's appeared only in the stage names were not consistent with pa- Tethys or Central Paratethys and the newly leogeographic and paleoecological characte- identified a few species peculiar to the region ristics of the region, and for each stage na- are also present. mes the suitable stages were selected. Con- In Turkey, apart from the studied areas, sequently, it has been decided that, the "Ott- the similar findings have been obtained by ot- nangian" stage is suggested to be used for old Lower Helvetian which was transgressive her investigators. Especially, in West Anatolia and marinal character at the beginning, later and Taurus, the faunal assemblages were de- became regressive and endemic brackish fa- tected reflecting the same environmental con- una in Central Paratethys. For the transgres- ditions similar to Central Paratethys. In con- sive and marine fauna in old Upper Helvetian, test, in northern Anatolia, the Eastern Para- the "Karpatian" stage is used (Steininger et tethys fauna is found. Based upon this: al., 1976; Steininger and Rögl, 1979 and Bukowski (1983), in Rhodos Island, iden- 1984; Nagymarosy and Müller, 1988; Steinin- tified Vivipara clathrala Deshayes, Melania to- ger et al., 1988). urnouari Fuch, Planorbis trassylvanicus Ne- In previous studies in Tethys realm, the umayr, Bythinia meridionalis Freundf. and Helvetian stage of Western Paratethys was Hydrobia ventrosa Montagu like mollusc used for Italy and France countries. However, samples and established the Levantine (Ro- when given up the usage of this stage, the manian) stage. Langhian and Serravalian stages (Middle Oppenheim (1918) referred to Sarmatian Miocene) were instead thought (Cita and - Pontian stages based on the Bithynia pisidi- Blow, 1969; Carloni et al., 1971; Later, it has ca Oppenheim, Vivipara bukowski Oppenhe- been decided that, based on the develop- im, Valvata pisidica Oppenheim and Limna- ments in biostratigraphic correlations and eus meparensis identified around Eflatun - changements in biozones, the Helvetian is corresponding to the Upper Burdigalian (Ste- Bunar (Yenice) at the east of Beyşehir lake. ininger et al., 1976; Steininger and Rögl, A great number of samples of class Bi- 1979; Harzhauzer, 1999, written communica- valvia and Gastropoda identified by Erünal - tion; Robba, 2000, written communication; Erentöz (1958) in Karaman, Adana and Hatay see Fig. 6.2). were also detected in Antalya and Kasaba ba- The Badenian and Sarmatian stage na- sins. The stage names used by Erünal - mes are used for Middle Miocene in Central Erentöz (1958) especially the Helvetian was Paratethys (Fig. 3). The Tortonian of Tethys identified in Switzerland falls into the effective was previously used in both regions for the area of Central Paratethys as mentioned pre- Middle Miocene; later, it is concluded that, the viously. When she interpreted the paleogeog- true Tortonian is correlative of Upper Miocene raphic distribution of identified mollusc fauna and is suitable for Tethys (Nagymarosy and in her study area, she also indicated that, they Müller, 1988; Steininger et al., 1988). were widely distibuted in Vienna basin in THE MOLLUSCAN FAUNA AND STRATIGRAPHY OF ANTALYA MIOCENE BASIN 27 28 Yeşim İSLAMOĞLU and Güler TANER

Central Europe and Polonia. Of the mollusc he also claimed that this genus was reached fauna, the important species are Turritella Jo the region by marine gateways. (Haustator) tricincta (Borson), Turritella (Arc- Gökçen (1979) studied the ostracod fa- himediella) bicarinata Eichwald, Terebralia una in the south of Denizli and north of Muğ- lignitara Eichwald, Xenophora deshayesi la, and based on this, she defined the Lower (MichelottL), Cypraea (Bernaya) fabagina (La- Aquitanian - Burdigalian stages between Ka- marck), Natica millepunctata Lamarck, Galeo- le - Yenişehir and Sarmatian, Pannonian and des cornutus (Agassız), Ancilla (Baryspira) glandiformis (Lamarck), Mitra (Mitra) fusifor- Pontian stages in Göktepe and Yatağan are- mis (Brocchi), Volutilithes (Athleta) ficulina as. She also pointed out that, the Neomonce- (Lamarck), Conus (Chelyconus) puschi Mic- ratina helvetica Oertli and Cyamocytheridea helotti, Anadara (Anadara) fichteli (Desha- reversa (Egger) detected especially around yes), Anadara (Anadara) turonica (Dujardin), Kale area are together with Burdigalian con- Amusium cristatum (Bronn), Pecten (Flabelli- sistent also with Eggenburgian and Ottnangi- pecten) solarium Lamarck, Crassostrea an. gryphoides (Schlotheim), Tellina (Peronaea) These data show us that, the Tethys and planata Linne, Venus (Ventricoloidea) multila- Paratethys stages have been detected in dif- mella (Lamarck) and Pelecyora (Cordiopsis) ferent parts of Anatolia. The mollusc samples isladicoides (Lamarck). that obtained from study area were correlated Taner (1975, 2001), established the by detail examination of stratigraphic levels in Maeotian - Pontian stages in Denizli region Tethys, Central and Eastern Paratethys. As a based on the identified mollusc samples result of this, it can be thought that, the Antal- which are Radix (A.) phrygica Oppenheim, ya and Kasaba basins depicted the evoluti- Pseudocardita phrygica Oppenheim, Dreisse- onary style similar to that of Tethys, since na phrygica Oppenheim, Pseudocardita they are located in Taurids which is situated in bukowskii Oppenheim, Paradacna denizli- the same orogenic belt with Alpine intermon- uense Taner, Prososthenia phrygica phrygica tane basins. Consequently, it is concluded Oppenheim, Pyrgula conica conica Taner and that, the similar environmental conditions in Theodoxus (C.) karakovensis karakovensis the study areas could be developed as that of Taner. Central Paratehys. For this reason, it is deci- Özsayar (1977) identified the mollusc fa- ded that, the time-equivalent stage names of una peculiar to Eastern Paratethys along Tethys and Central Paratethys must be used Black Sea coast and based on this, the used together whenever the correlation is possible. Tarchanian, Tschokrakian, Karagonian and The difficulties and geographic differences Bessarabian in Sinop area and Pontian stage encountered during correlation of stratotypes in Bafra and Trabzon provinces. In addition, in Europe have been also referred by Becker- the author detected the presence of genus Platen (1970) who studied in West Taurus. Velapertina sp., identified by Prof. Dr. Papp For this reason, a need appeared to define and special to Upper Badenian stage plankto- the regional stages peculiar to Turkey in the nic foraminiferas of Central Paratethys, and future. THE MOLLUSCAN FAUNA AND STRATIGRAPHY OF ANTALYA MIOCENE BASIN 29

THE MINERALOGICAL COMPOSITION, Prior to applying analyses the shells are MAJOR AND TRACE ELEMENT VALUES cleaned up, later they are grinded in agate OF THE MOLLUSC SHELLS mortar and prepared to powder. Each sample is cut into halves, one half for detected of mi- Material and method neralogical composition by X-Ray (X-Ray dif- In this study, the mineralogical and ele- feraction) and the other for identification of ment compositions of the shells obtained from major and trace elements by XRF Analyses different locations are defined and it is tried to and Technology Department of MTA. carry out the environmental interpretations on The samples for X-Ray differaction the shells with less effect of diagenesis. For analyses were induced between 2.5-60° environmental interpretations, the known pa- where scanning speed is 8. The obtained mi- leoecological characteristics of the fauna are neral to the lesser one. The calcite coexis ten- considered. ce with aragonite is unclear whether it is Mg- The analyses were carried out on 30 Calcite or not. Hence, the values are conside- mollusc shells in total. These shells are belon- red only as calcite. ging to species identifed in Kasaba and Antal- The major element analyses by XRF ya basins. The Kasaba basin includes Turri- method have been carried out on the samples tella (Haustator) tricincta (Borson), Turritella dried at 105°. terebralis turritissima Sacco, Turritella terebralis subagibbosa Sacco, Turritella (Turritella) Antalya Miocene basin turns Basterot, Turritella (Peyrotia) desmarejs- By evaluating the mineralogical compo- tina Basterot, Turritella (Archimediella) bicari- sition of the shells in the basin, while the nata Eichwald, Ancilla (Baryspira) glandifor- Upper Burdigalian (Ottnangian -Karpatian) mis (Lamarck), Conus antiquus Lamarck and aged marinal shells in Altınkaya formation are Conus conoponderosus (Sacco) of class in calcite or calcite-aragonite composition, the Gastropoda and Pecten (Flabellipecten) sola- Lower Tortonian marine molluscs in Aksu rium Lamarck and Nemocardium spondylo- formation are in aragonite composition (Table ides (Hauer) of class Bivalvia. The Terebralia 5 a-b). lignitara (Eichwald), Terebralia lignitara lignitara (Eichwald), Strombus coronatus Defran- The Crassostrea gryphoides (Schlothe- ce, Cehthium appenninicum dertosulcata im) species of Langihian (Lower Badenian) Sacco, Cerithium (Thericium) europaeum Altınkaya formation adapted to brackish water graciliornata (Sacco), Conus mercati Brocchi environment are calcite in composition with and Conus conoponderosus (Sacco) of class lesser amount of quartz in their body. Due to Gastropoda and Crassostrea gryphoides the effect of burial conditions, the silicification (Schlotheim) and recent shell from Side can be developed in genus and species of beach Glycymeris (Glcymeris) bimaculatus order Ostreina and it takes place as SiO2 (Poli) of class Bivalvia are obtained from quartz mineral within body of crust (Ozhigova, Antalya basin. 1992). 30 Yeşim İSLAMOĞLU and Güler TANER

When the major and trace element valu- tonian aged Aksu formation indicate the values of mollusc shells of Antalya basin are exa- es ranging between 6 and 241 ppm of Mg. A mined; it is shown that the Ca takes the valu- 60 ppm value of Mg has been found in recent es ranging between %35.02 and %38.95 as Glycymeris (Glycymeris) bimaculata (Poli) being the main component of the all shells in from Side beach. This last value is much lo- the region. wer than that of Miocene aged mollusc shells. The anomalous increase in Mg content is In Altınkaya formation, the species rep- known to be related to the diagenesis (Kim et resenting Upper Burdigalian (Ottnangian-Kar- al., 1999). Based on this, it can be interpreted patian) yield 222 ppm Na, whereas the Lang- that, the samples with high value of Mg are hian (Lower Badenian) aged Crassostrea more diagenetic and those with low value me- gryphoides (Schlotheim) type species point a an less diagenetic. lower value of Na (74-148 ppm). The Al and Si values are randomly distri- The Na content of the samples in Lower buted in the whole region. For the Sr, the all Tortonian age Aksu formation is at higher va- Crassost- lues relative to the others and changes bet- Langhian (Lower Badenian) aged ween 222 and 296 ppm. By comparing these rea gryphoides (Schlotheim) species from dif- values with the recent shells, the Na content ferent localities of Altınkaya formation contain of Glycymeris (Glycymeris) bimaculatus (Poli) lower and constant values which is 84 ppm. taken from Side beach depicts a 445 ppm va- The whole formation of this species from cal- lue of Na (Table 5 a-b and 6 a-b). Consequ- citic shells reveals that the original shell com- ently, the sea water salinity is proportional to positon has not changed (Ozhigova, 1992). Na content and it is concluded that the Na The upper Burdigalian (Ottnangian- Karpati- content of the Miocene sea was lower than an) aged aragonitic gastropod shells, taken that of the recent in the region. from under the Crassostrea gryphoides (Schlotheim) level have Sr contents ranging In the case of Mg content of the shells between 253 and 338 ppm in Altınkaya for- (Table 5 a-b); the Cerithium (Thericium) euro- mation. It is known that, the Sr in sea water is paeum graciliornata Sacco has Mg value of proportional to the salinity (Turekian, 1955). 362 ppm in Aşağıyaylabel section and betwe- Consequently, it can be interpreted that, the en 301 and 603 ppm in Hocalarsırtı section, sea water salinity during Langhian (Lower Ba- which both of them are Upper Burdigalian (Ot- denian) was much lower in the region. tangian - Karpatian) in age in Altınkaya formation. The Ostrea lamellosa Brocchi yields a When the 1000 Mg/Ca and 1000 Sr/Ca 241 ppm value of Mg in the Alarahan section ratios of the shells are considered; firstly, the of Upper Burdigalian Oymapınar limestone. recent Glycymeris (Glycymeris) bimaculata The Mg values of Langhian (Lower Badenian) (Poli) found in Side beach processed and the aged Crassostrea gryphoides (Schlotheim) 1000 Sr/Ca= 6.60 and 1000 Mg/Ca= 1.60 ra- species are between 301 and 422 ppm in Al- tios have been obtained. Later, the other data tınkaya formation. The samples in Lower Tor- are correlated with this result. THE MOLLUSCAN FAUNA AND STRATIGRAPHY OF ANTALYA MIOCENE BASIN 31 32 Yeşim İSLAMOĞLU and Güler TANER THE MOLLUSCAN FAUNA AND STRATIGRAPHY OF ANTALYA MIOCENE BASIN 33 34 Yeşim İSLAMOĞLU and Güler TANER THE MOLLUSCAN FAUNA AND STRATIGRAPHY OF ANTALYA MIOCENE BASIN 35

A general evaluation has been carried For the shells of Langhian (Lower Bade- out on the comparison between mineralogical nian) age: compositions and element ratios of the shells 1000 Sr/Ca =2.39- 8.99 obtained from Antalya Miocene basin. As the following; 1000 Mg/Ca = 1.56- 17.18 For aragonitic shells: 1000 Sr/Ca =2.16-9.07 For of Lower Tortonian shells: 1000 Mg/Ca = 7.87-17.21 1000 Sr/Ca =21.9- 9.07 Mg = 60 - 241 ppm 1000 Mg/Ca = 7.87 - 17.21 ratios have been found. Sr= 169-338 ppm Based on this, the 1000 Sr/Ca ratio was much lower than that of the recent, during Up- For calcitic shells: per Burdigalian (Ottnangian- Karpatian) period. However, the 1000 Mg/Ca ratio is higher 1000 Sr/Ca =2.39-8.99 than the recent. By comparing the locations, 1000 Mg/Ca= 1.56-17.18 Cerithium (Thericium) europaeum graciliorna- Mg = 301 - 603 ppm ta (Sacco) in point A10 of Aşağıyaylabel section (Altınkaya formation) and Ostrea lamello- Sr = 84 ppm values have been determi- sa Brocchi in point A4 of Alarahan section ned. (Oymapınar limestone) have close values Based on the results obtained from the which are 224 and 225 ppm respectively. In basin, the all calcitic shells are pelecypods Hocalarsırtı section, the two different samples and the shells with aragonite+ calcitic compo- (Terebralia lignitara Eichwald and Terebralia sition are gastropods. Hence, the aragonitic lignitara lignitara Eichwald) indicate the same shells have lower Mg content. This conclusion 1000 Sr/Ca value (2.16). Although the 1000 is also consistent with the studies Yalçın and Mg/Ca ratios of the same samples are nearly Bozkaya (1995) on recent mollusc shells in proportional to 1000 Sr/Ca, they are not very Bay of İzmit (SE Marmara sea). The 1000 reliable. Sr/Ca ratio is much lower than 1000 Mg/Ca The 1000 Sr/Ca ratio in Langhian (Lower ratio in aragonitic shells. However, in calcitic Badenian) is lower than the recent in same shells, the 1000 Mg/Ca ratio may be the same . samples and is close on much more in other or a little bit more or less than 1000 Sr/Ca ra- samples. The all of the 1000 Mg/Ca ratios are tio. If an evaluation is fullfilled with respect to - much more than recent. A striking result is the ages and localities of the shells; that, in all localities, the shells of Crassostrea For the shells of Upper Burdigalian (Ott- gryphoides (Schlotheim) have 8.4 ppm Sr and nangian- Karpatian) age: 74 ppm Na which are very low. The Lower Tortonian 1000 Sr/Ca ratio is much lower than 1000 Sr/Ca =2.16-2.25 that of recent (2.19-4.82 ppm). The Crassost- 1000 Mg/Ca = 6.18-11.31 rea gryphoides (Schlotheim) species having 36 Yeşim İSLAMOĞLU and Güler TANER

only calcitic shell has the same Sr value, in between % 36.6 and % 38.59. The Na ratio the same age, but in different localities. The withi no difference in Kasaba and Uçarsu for- previous studies carried out on ostreas indica- mations is between 148-222 ppm values. The te that this group yields reliable results in pa- Mg ratios in the samples of the Kasaba basin leoecological interpretations (Ozhigova, are a little bit high relative to those of recent 1992). The data obtained from Crassostrea and in the values of 241-482 ppm in Upper gryphoides (Schlotheim) depicts the environ- Burdigalian (Upper Eggenburgian - Karpati- ment with low salinity and is well consistent an). with its paleoecological characteristics itself. The Langhian (Lower Badenian) aged Kasaba Miocene basin shells, although they are in the same locations, they indicate different compositions. For By considering the mineralogical compo- example, in the Çb2 sample point of Ortabağ sition of the shells; in Ortabağ section of the section, as the Turritella (Turritella) turris Bas- Kasaba formation, the Langhian (Lower Ba- terot is 723 ppm and Turritella (Archimediella) denian) aged Ancilla (Baryspira) glandiformis bicarinata Eichwald is 784 ppm in Mg values, (Lamarck), Conus antiquus Lamarck, Turritel- the Conus antiquus Lamarck has 200 ppm la (Turritella) turn's Baste rot and Nemocardi- and-the Ancilla (Baryspira) glandiformis (La- um spondyloides (Hauer) are aragonite- calci- marck) has 241 ppm values. The similar valu- te in composition, whereas in the same level, es are also present in Boyacıpınar section of the Turritella (Archimediella) bicarinata Eich- the same period. The Ancilla (Baryspira) glan- wald and Pecten (Flabellipecten) solarium La- diformis (Lamarck) and Turritella (Archimedi- marck are calcite- aragonite in composition. ella) bicarinata Eichwald yield the 120 and Similarly, in Boyacıpınar, the Langhian (Lo- 482 ppm values respectively. By comparison wer Badenian) aged Turritella (Haustator) tri- of the mineralogical compositions of the cincta (Borson) is in the composition of ara- shells, it is seen that, the Ancilla (Baryspira) gonite - calcite, while the Turritella (Archime- glandiformis (Lamarck) with low Mg ratio con- diella) bicarinata Eichwald and Conus cono- tent has higher aragonite ratio (Table 6 a-b). ponderosus (Sacco) are in calcite-aragonite This also confirms that, the Mg content in ara- composition (Table 6 a-b). gonitic shells is low as mentioned before. The all Upper Burdigalian (Upper Eggen- There has been no consistency among burgian - Karpatian) aged shells in Uçarsu the Si, Al and Fe ratios, mineralogical compo- formation are composed of two minerals ara- sitions and localities of the shells, similar to gonite calcite or calcite aragonite. The, those in Antalya Miocene basin. However, the changements in aragonite - calcite ratios of Al content of the all shells is nearly equal to the shells reflect the diagenetic effects after the recent, while the Si and Fe contents are a deposition (Kim et al., 1999). It can also be little bit high in values. thought that, in Kasaba basin, the shells part- When a comparison is full filled between ly undergone diagenetic effects. the mineralogical composition and element The major and trace element ratios of the ratios of the shells obtained from Kasaba shells are evaluated as; the Ca ratio changes Miocene basin; THE MOLLUSCAN FAUNA AND STRATIGRAPHY OF ANTALYA MIOCENE BASIN 37

For the shells with aragonite+ calcite Bozkaya, 1995; Yalçın and Taner, 1998). composition: Since it is known that, the Mediterranean has a high salinity relative to the Marmara sea, it 1000 Sr/Ca =6.7-9.0 can be concluded that, the 1000 Sr/Ca ratios 1000 Mg/Ca = 3.1 -11.2 is propositional to the salinity. Mg = 120-723 ppm Sr = 253 - 338 ppm Evaluating the shell localities and ages; For the Upper Burdigalian (Upper Eg- genburgian -Karpatian) aged shells: For the shells having calcite+aragonite composition: 1000 Sr/Ca =6.8- 9 1000 Sr/Ca =4.5-11.1 1000 Mg/Ca = 6.4-12.9 1000 Mg/Ca = 2.1 -12.9 For Langhian (Lower Badenian) aged Mg = 241 - 784 ppm shells: Sr = 169 - 422 ppm values have been 1000 Sr/Ca = 4.5-11.1 determined. 1000 Mg/Ca = 2.1-19.6 values have Based on this, in the shells of aragoni- been found. Based on this, the 1000 Sr/Ca rate+calcite composition, the 1000 Mg/Ca ratio tio in Upper Burdigalian (Upper Eggenburgian is lower than the 1000 Sr/Ca ratio. The same -Karpatian) and Langhian (Lower Badenian) occurence is also valid for the shells having periods is nearly equal or a little bit high calcite+aragonite composition. Except this, (Table 6 a-b). there has not been any clear difference among the all ratios. CONCLUSIONS The shell of the recent pelecypod taken from Side beach (Antalya), indicates 6.61 va- Paleogeographic results lue for 1000 Sr/Ca ratio and 1.56 for 1000 1. The paleogeographic distribution of mol- Mg/Ca ratio. The 1000 Mg/Ca ratio of this ara- lusc fauna puts in evidence that, the Lo- gonitic shells is lower than 1000 Sr/Ca ratio. wer- Middle Miocene age formations in This conclusion also implies that, the aragoni- Antalya and Kasaba basins have correla- tic shells have low Mg content (Yalçın and tive characteristics both with Tethys and Bozkaya, 1995). If the geochemical values of Central Paratethys stages. Hence, the ti- aragonitic pelecypoql in Side beach and the" me equivalent stage names of these two shells with the same composition in İzmit Bay provinces are used together. (SE Marmara sea) are compared, it is found that, the 1000 Sr/Ca ratio in sample of Side is 2. Although some of the samples from studi- 6.6 and that in İzmit. Bay is 3.60-5.72. The ed regions are widely distributed in Eas- 1000 Mg/Ca ratios are 1.6 and 0.86-1.69 for tern Paratethys, it is not advisable to use Side and İzmit Bay respectively (Yalçın and the time equivalent stages of this region. 38 Yeşim İSLAMOĞLU and Güler TANER

3. In both regions, for the Lower- Middle Mi- increase or decrease (Turekian, 1955), it ocene, the Hydrobia (Hydrobia) frauenfel- is concluded that, Antalya Miocene basin di (Homes), Pirenella gamlitzensis gamlit- in this period has a marine realm with zensis (Hilber), Irus (Paphirus) gregarius lower salinity with respect to that of Kasa- Partsch and Glossus (Cytherocardia) cf. ba Miocene basin. The widely distributed deshayesi (Kutassy) type species peculiar brackish water - marine samples in Antal- to the only Central Paratethys were identi- ya Miocene basin also confirm this result. fied. 4. The 1000 Sr/Ca ratios increased a little 4. The Antalya and Kasaba Miocene basins big (2.39-8.99) in Antalya Miocene basin are in the same character of the intermon- during Langhian (Lower Badenian). tane molasse basins in the Alps and loca- However, it is the same in Kasaba ted in the same orogenic belt. Consequ- Miocene basin (4.5-11.1). Consequently, ently, the similar events during Tethyan evolution must have been occured in the although the salinity increased a bit, it is study areas. The faunal development also lower than Kasaba Miocene basin. reveals the environmental conditions simi- 5. During Lower Tortonian, the 1000 Sr/Ca lar to Paratethys, besides the Tethys. For values in Antalya basin ranged between this reason, it is normal that, the special 2.19-9.07. In Kasaba basin, there is no bioprovinces similar to Central Paratethys could be developed in Turkey. In this only marine deposit in this period. Hence, study, although the stage names for the any comparison can not be carried out. basins are used together, it is a need in 6. The Sr trace element concentration of the future to define the regional stages. Crassostrea gryphoides (Schlotheim) which is widely distributed in Antalya Paleoecological results Miocene basin is very low. Its originally 1. The Mg contents of aragonitic shells yield crust composition (calcite) has not been lower values relative to those of calcitic also changed. The shells of this species in ones. different localities indicate the same 2. As a result of geochemical analyses of values. shells, it is concluded that, the Na and Sr Table captions: E: Early, O: Middle, G: Late, trace element concentrations and 1000 Sr/Ca ratios are proportional to the salinity Ol: Oligocene, A: Aquitanian, B: Burdiga- either increase or decrease. lian, L: Langhian, S: Serravalian, T: Torto- nian, Mes: Messinian, PI: Pliocene, 3. Based on the biochemical values obtained P: Pleistocene, Gun: Recent, Eg: Egeri- from mollusc fauna, during Upper Burdi- an, Egb: Eggenburgian, Ott: Ottnangian, galian (Ottnangian- Karpatian) the Sr/Ca ratio in Antalya Miocene basin (2.16-2.25) K: Karpatian, Bd: Badenian, Sr: Sarmati- is lower than that (6.8-9.0) of Kasaba an, Kr: Karagonian, Sak: Sakarulian, Miocene basin. Since the Sr in sea water Tr: Tarchanian, Çk: Tschokrakian, Kon: is proportional to the salinity either Konkian. THE MOLLUSCAN FAUNA AND STRATIGRAPHY OF ANTALYA MIOCENE BASIN 39

ACKNOWLEDGEMENTS Pub. Hungarici, vol.41, fasc.4, 185 P., Budapest. This study is a part of "PhD Thesis" full- Ctyroky, P.; Hölzl, O.; Kokay, J.; Schhckum, W.R.; filled in Geological Engineering of Naturel and Schultz, O., Strauch, F. and Steininger, Applied Science Institute in Ankara Univer- F.,1973, Die Molluskenfaunendes Ottnangi- sity. The authors acknowledged to the Gene- yen, Chronostratigraphie und Neostratoty- pen, Miozan der zentralen Paratethys, M 2, ral Directorate of MTA for field and laboratory OTTNANGIAN, Bratislava. facilities, to TUBITAK authorities to suppor- Davoli, F., 1972, Conidae (Gastropoda), Studi Mo- ting an abroad scholarship Nato A2 provided nografici sulla malacologia Miocenica mo- th for 1 author. denese, Parte I - I molluschi Tortoniani di Monte Gibbo, Paleontog. Italica. 68, 51-143. Manuscript received March 12, 2002 , 1990, La collezione di "Fossili Miocenici di Sagliano" di Lodovico Foresti: Revisione ed illustrazione. Atti.Soc. Nat. e Mat. di Mode- REFERENCES na, 121, 27-109, Modena. Becker-Platen, 1970, Lithostratigraphische Untersc- Deperet, G. and Roman, F., 1902-12, Monographie hungen in Kanozoikum Sud-West Anatoli- des Pectinides Neogenes de I'Europe et ens (Kanozoikum und Braunkohlen der Tur- des regions voisines. Mem. Soc. Geol. Fr., kei, 2): Beih. Geol. Jb., 97, 244 p., Hanno- C.10, No: 26, Paris. ver. Dollfuss, G.F. and Dautzenberg, PH., 1902-1920, Bukowski, V. G. 1983, Die Levantinische Mollusken- Conchyliologie du Miocene Moyen du fauna der Insel Rhodos. Der Denkschriften Bassin de la Loire Mem.Soc.Geol.France der Mathematisch-Naturwissenschaftlichen Paleont.Mem. 27, Paris. classe der Kaiserlichen Akademie der Wis- senschaften. LX Bande. Wien. Dulai, A., 1996, Taxonomic composition and paleoecological features of the Early Bade- Carloni, G.C.; Marks, P.; Rutsch, R.F. and Selli, R., nian (Middle Miocene) bivalve fauna of (Eds.), 1971, Stratotypes of Mediterranean Szob (Börzsöny Mts, Hungary, Ann. His. Tetis Neogene Stages, Proc. Comm.Medit. Neog. Strat. (Bologna 1967), Giorn. Geol., Nat. Mus. Nationalis Hungarici, vol. 88, ser.2, Vol.37, No.2, 266 p. 31-56, Budapest. Cicha, I.; Senes, J. and Tejkal, J.J., 1969, Proposi- Erünal-Erentöz, L., 1958, Mollusques du Neogene tion pour la creation de neostratotypes et des Bassins de Karaman , Adana et Hatay retabhssement d'une Echelle chronostratig- (Turquie), Theses. A la Faculte des Scien- raphique dite ouverte, Giornale di Geologia ces de I'Universite de Paris, Le Grade de (2) 35, fasc.4, s.297-311, Bologna. Docteur es Sciences Naturelles, 232 p., Cita, M.B. and Blow, H., 1969, The biostratigraphy of Ankara. the Langhian, Serravallian and Tortoniah Friedberg, W., 1911-1928, Mollusca Miocenica Polo- stages in the type-sections in Italy. Riv. Ital. niae, Pars:1, Gastropoda et Scaphopoda. Paleont., v.75, n.3, 549-603. Muz. Imenia Dzieduszyckich. Krakow. Cossmann, M. and Peyrot, A., 1914, Conchiologie , 1954-55, Poloniae finitiarumque terrarum Neogenique de I'Aquitaine, t.3, Act. Soc. mollusca Miocenica, t:2-3, Warszawa. linn. Bordeaux. Gelati, R. and Robba, E., 1975, Proposal of a supers- and , 1919-1924, Conchologie Neo tage for the Lower Miocene with type-area genique de I'Aquitaine, C:1-4, Bordeaux. in the Piedmont Basin, VI th Congr. Region. Csepreghy-Meznerics, I., 1954, A Keletcserhati Hel- Commit, on Medit. Neog. Strat., Bratislava, veti es Tortonai Fauna, Ann. Inst. Geol. 209-215. 40 Yeşim İSLAMOĞLU and Güler TANER

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