The Molluscan Fauna and Stratigraphy of Antalya Miocene Basin (West-Central Taurids, Sw Turkey)

Mineral Res. Expl. Bul.. 123-124, 27-58. 2002

THE MOLLUSCAN FAUNA AND STRATIGRAPHY OF ANTALYA MIOCENE BASIN (WEST-CENTRAL TAURIDS, SW TURKEY)

Yeşim İSLAMOGĞU*

ABSTRACT.- This study has been carried out in Miocene units containing molluscan fauna, deposited in Antalya Miocene basin located at Western and Central Taurids. In the circumstances of this study, the eight stratigraphic sections were measured and the stratigraphy of the basin has been re-evaluated, based on the examination of the chronostratigraphic ranges of the collected samples belonging to the molluscan fauna. In this respect, the Lower Miocene Kepez travertine is the lowermost unit and unconformable with the basement, at the southeast of the basin. Succeded up, the Burdigalian Seving conglomerate of alluvial fan - fan delta character overlies this unit. The Upper Burdigalian - Langhian (Karpatian - Lower Badenian) Oymapınar limestone is composed of reefal - massive limestones and conformably overlies the Seving conglomerate. The Sevinc conglomerate and Oymapınar limestone are also unconformably overlying the basement rocks. The Oymapınar limestone is overlain by Çakallar formation (Upper Burdigalian - Lower Langhian) and Geceleme formation (Langhian). Geceleme formation is overlain by Serravalian - Tortonian levels of the Karpuzçay formation. It is the first in this study, that the units exposed in central and northern parts of the basin have been differentiated from the Aksu formation and defined as the Altınkaya formation. The Altınkaya formation is characterized by brackish water - marinal properties and contains Upper Burdigalian - Langhian (Ottnangian - Karpatian - Lower Burdigalian) molluscan fauna. It unconformably overlies the basement rock units and is overlain by Aksu formation. The Altınkaya formation is also laterally transitional with Upper Burdigalian - Langhian levels of the Karpuzçay formation. The Aksu formation widely cropped out widely at western and central parts of Antalya Miocene basin was dated as Lower Tortonian due to its molluscan fauna. However, the overall age of the formation was accepted as Serravalian - Tortonian.

INTRODUCTION gic, stratigraphic and tectonic point of view and different ideas have been suggested (Al- The Antalya Miocene basin is located at tmli, 1945; Blumenthal, 1951; Özer at al., east of Western Taurids and west of Central 1974; Öztümer, 1974; Dumont and Kerey, Taurids in the area among Antalya, Alanya 1975a and b; Monod, 1977; Akbulut, 1980; and Isparta provinces (Fig. 1). In this study, Akoz, 1981; Akay and Uysal, 1984; Akay et the Miocene units in the basin have been in- al., 1985; Şenel et al., 1992, 1996 and 1998; vestigated and eight stratigraphic sections ha- Naz et al., 1991 and 1992; Tuzcu et al., 1994; ve been measured with compilation of samp- Flecker et al., 1995; Erk et al., 1995; Karabı- les collected from levels rich in molluscan fa- yıkoğlu et al., 1996 and 1997; Atabey, 1998; una. The paleogeographic properties and Karabıyıkoğlu et al., 2000). taxonomies of molluscan fauna in measured sections were studied in detail (İslamoğlu, Such a paleontological and stratigraphic 2001). study based on the molluscan fauna in the

The Miocene sediment fill in the region Antalya Miocene basin was firstly carried out has been the subject of many studies since and by using the obtained data, it is tried to 1940's from the sedimentologic, paleontolo- make a contribution to the basin stratigraphy. 28 Yeşim İSLAMOĞLU THE MOLLUSCAN FAUNA AND STRATIGRAPHY OF ANTALYA MIOCENE 29

GEOLOGY OF THE BASEMENT ROCKS platform type deposits (Brunn et al., 1971; Monod, 1977; Şenel et al., 1992; 1996). The The Neogene marinal deposits cover wi- Antalya nappes were also defined as "Antalya de area in the region where the autochthono- Unit" and "Antalya complex" by Özgül (1976) us and allocthonous rock units of Precambri- and Woodcock and Robertson (1977) respec- an - Quaternary time interval are exposed. tively. In the region, the autochthonous rock The Alanya nappe, overlying the Antalya units are Beydağları and Anamas - Akseki au- nappes, includes Mahmutlar and Yumrudağ tochthone whereas the allocthonous were de- and Sugozu units undergone greenschist and fined as Antalya nappe and Beysehir-Hoyran- blueschist facies metamorphism respectively Hadim nappes (Brunn et al., 1971, 1973; Du- (Özgül, 1984). Özgül (1976) defined the Alan- mont and Kerey, 1975a; Dumont, 1976; Mo- ya nappe as "Antalya unit". nod, 1977; Poisson, 1977; Akbulut, 1977 and 1980; Waldron, 1982; Akay and Uysal, 1984; Özgül (1976) distinguished three tecto- Akay et al., 1985; Şenel et al., 1992, 1996; nic units namely; Aladağ unit, Bozkır unit and Şenel, 1997a, b). Bolkar unit based upon sequential between Lycian nappes and Beyşehir-Hoyran-Hadim The Beydağları autochthone is located at nappes, Şenel (1997 a,b,c) classified the west of Antalya Miocene basin and generally Lycian nappes into many structural units as represented by Moesozoic platform carbona- Tavas nappe, Bodrum nappe, Marmaris ophi- tes. The Anamas-Akseki autochthone is ob- olite nappe, Domuzdağ nappe and Gülbahar served at east and north of Antalya basin and nappe. consists of Mesozoic - Lower Tertiary carbo- The Neogene deposits in the Antalya ba- nates with minor amount of clastic rocks. The sin have been investigated by many researc- Beydağları and Anamas-Akseki autochthones hers (Monod, 1977; Poisson, 1977; Dumont were combined and defined as Geyikdağ unit and Kerey, 1975a and b; Akay and Uysal, by Özgül (1976). 1984; Akay et al., 1985; Şenel et al., 1991, In the region, the Antalya nappes empla- 1992, 1996; Naz et al., 1991 and 1992; Flec- ced from the south, during Early Paleocene ker et al., 1995; Şenel and Bölükbaşı, 1997; (Danian) and they include Upper Triassic Karabıyıkoğlu et al., 2000). The region has platform, Jurassic - Cretaceous slope-basin undergone the effect of Kırkkavak fault (Du- type deposits of Çataltepe nappe, Permian- mont and Kerey, 1975a) and Aksu thrust (Po- Lower Triassic platform, Middle Triassic-Up- isson, 1977) which are coeval with the sedi- per Cretaceous basin type deposits with do- mentation. For this reason, some of the rese- minant basic volcanism of Alakırçay nappe- archers preferred to investigate the region un- Tekirova ophiolite nappe and Tahtalıdağ nap- der the three subbasin areas namely; N-S pe composed of Cambrian-Upper Cretaceous . trending Aksu and Köprüçay subbasins and 30 Yeşim İSLAMOĞLU

NW-SE trending Manavgat subbasin (Flecker LOCATIONS OF MEASURED STRATIG- et al., 1995; Robertson et al., 1996). RAPHIC SECTIONS

Generally, at east and southeast of the In the region, the Miocene units conta- basin, the Kepez travertine (Lower Miocene), ining molluscan fauna (Seving conglomerate, the Seving conglomerate (Burdigalian), the Oymapınar limestone, Altınkaya formation Oymapınar limestone (Upper Burdigalian- and Aksu formation) have been investigated Langhian), the Çakallar formation (Upper Bur- in detail, and eight section were measured digalian-Lower Langhian) and the Geceleme (Fig. 1). Measured sections and their locati- formation (Langhian) are cropped out. The Al- ons are as follows. tınkaya formation (Upper Burdigalian-Lower Langhian) is exposed at central, northern and The Alarahan measured stratigraphic sec- southern parts of the basin. The Karpuzçay tion (Fig. 1, AA') formation (Upper Burdigalian-Tortonian) is This section was measured in NE-SW di- observed in the whole basin, whereas the Ak- rection at southeast of Antalya Miocene basin su formation (Serravalian-Tortonian) is crop- (Alanya 027d2 quadrangle) at eastern slope ped out at central and western parts of it. of the Alara stream. It has a 190 m total thick- The other units in the region are the Lo- ness, starting at X1 86400, Y1 62600 and fi- wer Pliocene the Gebiz, the Eskiköy and the nishing at X2 86350, Y2 62400 coordinates. Yenimahalle formations, the Upper Pliocene Lower part of the section (170 m.) is repre- Alakilise formation, the Pleistocene Belkıs sented by the Seving conglomerate, whereas conglomerate and the Quaternary Antalya tra- the rest 20 m is the Oymapınar limestone vertine and alluvions (Poisson, 1977; Akay (Fig. 2). and Uysal, 1984; Akay et al., 1985). The Oymapınar measured section (Fig. 1, There has been a compression - extenti- BB') on type tectonic regime prevailed since This section is located at O27a1 quad- Miocene in the region. The products of the compressional regime are the empiacement rangle and was measured along Manavgat of Lycian nappes from northwest to southeast, stream toward southwest, at Oymapınar Dam NE-SW trending Aksu thrust and Kırkkavak and is situated approximately 3 km to the fault which is right-lateral strikeslip fault with north of Oymapınar village. It is about 95 m reverse slip component (Dumont and Kerey, thick and starting at X1 69150, Y1 85450 and 1975a; Poisson, 1977; Akay and Uysal, 1988; finishing at X2 68950, Y2 85975 coordinates. Şenel et al., 1992). Antalya graben has deve- Throughout the section, the basal 55 m part is loped by the E-W and later N-S trending belonging to Oymapınar limestone and the compressions since Late Pliocene (Akay and overlying 40 m thick upper part is represented Uysal, 1988). by the Geceleme formation (Fig. 3). THE MOLLUSCAN FAUNA AND STRATIGRAPHY OF ANTALYA MIOCENE 31

Fig. 2- The Alarahan stratigraphic section measured in the Seving conglomerate and the Oymapınar limestone (AA') 32 Yeşim İSLAMOĞLU

Fig. 3- The Oymapınar stratigraphic section measured in the teh Oymapınar limestone (BB') THE MOLLUSCAN FAUNA AND STRATIGRAPHY OF ANTALYA MIOCENE 33

The Radioring measured stratigraphic asured from southeast to northwest. The co- section (Fig. 1, CC') ordinates are starting at X1 40020, Y1 90020 and finishing at X2 40125, Y2 90000. It is only This section is located at Antalya O26a2 represented by 40 thick the Oymapınar limes- quadrangle, 4.5 km northwest of Tasagil and tone (Fig. 4) 1 km south of Radioring station ancl was me-

Fig. 4- The Radioring stratigraphic section measured in the Oymapınar limestone (CC') 34 Yeşim İSLAMOĞLU

The Ballıbucak measured stratigraphic 29425 and finishes at X2 33800, Y2 29000 section (Fig. 1, DD') coordinates. The basal 86 m part of 101m total thickness is characterized by the Oymapı- The section is located at Isparta N26a4 nar limestone. Unconformably overlying this quadrangle, approximately 700 m to the sout- is the 15 m thick conglomerates, probably heast of Ballıbucak village and was measured . belonging to Aksu formation (Fig. 5). in NW-SE direction. It starts at X1 33165, Y1

Fig. 5- The Ballıbucak stratigraphic section measured in the Oymapınar limestone and the Aksu formation (DD') THE MOLLUSCAN FAUNA AND STRATIGRAPHY OF ANTALYA MIOCENE 35

The Altınkaya measured stratigraphic sec- 2.5 km from north of Beşkonak village in tion (Fig. 1, EE') northwest direction to the antique Zelga theatre (Altınkaya village). The section starts at X1 The Altınkaya measured section is loca- 39250, Y1 15400 and finishes at X2 33825, ted at Isparta N26d2 quadrangle. The section Y2 22200 and it is completely represented by is 750 m in total thickness and was measured the Altınkaya formation (Fig. 6).

Fig. 6- The Altınkaya stratigraphic section measured in the Altınkaya formation (EE') 36 Yeşim İSLAMOĞLU

The Asağıyaylabel measured stratigraphic province. It is approximately 54 m in thickness section (Fig. 1, FF') and starts at X1 49400, Y1 57175 and finis- This section is located at M26c4 quad- hes at X2 49875, Y2 57275 coordinates. The rangle and was measured in northeast direc- whole section is characterized by the Altınka- ya formation (Fig. 7). tion 1.5 km to the southwest Aşağıyaylabel

Fig. 7- The Aşağıyaylabel stratigraphic section measured in the Altınkaya formation (FF') THE MOLLUSCAN FAUNA AND STRATIGRAPHY OF ANTALYA MIOCENE 37

The Hocalarsırtı measured stratigraphic vince. The starting and finishing coordinates section (Fig. 1, GG') are X1 49250, Y1 45800 and X2 49750, Y2 45550 respectively. The thickness of the sec- This section is located at Isparta N26b2 tion is about 36 m and it belongs completely quadrangle, approximately 1 km northwest of to the Altınkaya formation (Fig. 8). Hocalarsırtı and 1 km south of Karakaya pro-

Fig. 8- The Hocalarsırtı stratigraphic section measured in the Altınkaya formation (GG') 38 Yeşim İSLAMOĞLU

The Kargı measured stratigraphic section around Kargı Tunnel. It is 56.5 m in total thick- (Fig. 1,HH') ness and starting at X1 06150, Y1 27350 and finishing with X2 06275, Y2 27850 coordina- This section is located at Isparta N25b4 tes. The section was completely measured quadrangle, 12 km to the south of Kargı and within Aksu formation (Fig. 9). was measured from southwest to northeast

Fig. 9- The Kargı stratigraphic section measured in the Aksu formation (HH') THE MOLLUSCAN FAUNA AND STRATIGRAPHY OF ANTALYA MIOCENE 39

THE STRATIGRAPHY OF THE ANTALYA name Sevinç conglomerate for the unit. Akay MIOCENE BASIN and Uysal (1984) and Akay et al., (1985) considered the unit together with Aksu formation. For the better understanding the stratigraphic relationships in the basin, the other Mi- Type section locality.- The type section is ocene units in the region have been also in- located around Sevinç village (Antalya O27a vestigated together with the studied formati- quadrangle). ons. These units are Kepez Travertine, Se- Lower-Upper boundary relations.- The ving conglomerate, Altınkaya formation, Oy- formation is observed at south and southeas- mapınar limestone, Çakallar formation, Gece- tern parts of the basin. It unconformably over- leme formation, Karpuzçay formation and Ak- lies the basement rock units and is confor- su formation. mably overlain by the Oymapınar limestone. The Kepez travertine Lithology.- The formation is dominantly Definition and nomenclature- It was first- represented by unbedded or cross-lenticular ly named by Monod (1977). stratified, continental and marinal conglomerates of different size. In some levels, it inclu- Type section locality.- It was defined at des yellow, reddish brown colored sandstone 300 m east of Kepez village (Antalya O27a1). and mudstone on small reefal limestone len- Lower-Upper boundary relations.- It un- ses. Sandstone and mudstone levels pinch conformably overlies Alanya massif and is out laterally. The marinal conglomerate is in- overlain by Upper Burdigalian deposits. tercalated with reefal limestone in Alarahan section representing marine level of the for- Lithology.- It is compposed of brown co- mation. lored, massive calcium carbonate with soluti- on cavity and plant fragments. Thickness and Distribution.- It is about 600 m thick (Şenel et al., 1992) and it pinches Thickness and distribution.- The unit is out laterally. appoximately 20 m thick and pinches out laterally. Fossil Content and age.- No fossil record was encountered to give an age data within Fossil content and age.- It contains leave terrestrial level of the formation. Late Burdiga- and plant fragments and rare green algae lian age has been suggested from the Alara- (Charophyte) (Monod, 1977). No age assign- han section representing marine levels. It is ment was estimated these fossils. It is thought concluded that due to unsuitable environmen- to be Lower Miocene based on stratigraphic tal conditions, the molluscan fauna could not relations. find opportunity to develope in diversity. For Depositional environment.- It reflects a this reason, only the Chlamys (Aequipecten) brackish water environment. scabrella bollenensis (Mayer) and.Osfrea lamellosa Brocchi characterizing the Late Bur- The Sevinç conglomerate digalian were found and for this part of the for- Definition and nomenclature.- Monod mation this age has been accepted. Also in (1977) assigned the unit as Tepekli detritics. the same level, the presence of the benthic Later, Gutnic et al., (1979) defined it as Se- foraminfera such as Borelis cf. melo Fichtel vinç conglomerate in their geological map. and Moll, Amphistegina sp., Peneroplis sp., Şenel et al., (1992, 1998) also adopted the- Operculina sp., Textulariidae (identified by 40 Yeşim İSLAMOĞLU

E. Sirel) and planktonic foraminifera Globige- cated 2.5 km to the northwest of Yaka village rinoides trilobus (Reuss) and Globigerinoides and Hocalarsırtı section (Isparta N26b1) situ- Disphericus Todd (identified by A. Hakyemez) ated at Hocalarsırtı ridge 1 km to the south of confirm this ageassigment. The age of the for- . Karakaya. The formation is also observed mation has been accepted as Burdigalian. along the road continued from Ballıbucak vil- Depositional Environment.- The conti- lage towards east (Köprüçay) (Isparta N26a4) nental parts of the formation indicate alluvial and along the road between Kesme and Ye- fan (Şenel et al., 1992, 1996), whereas the şilbağ village and north of Yeşilbağ village (Is- marinal levels reflect shallow marine environ- parta M26c4). ment. Karabıyıkoğlu et al., (1996, 1997, 2000) Lower-Upper boundary relations.- The pointed out that, the deposits indicate facies formation unconformably overlies the Antalya characteristics of alluvial fan-fan delta envi- nappes, Beydağları-Karacahisar autochthone ronment. and Anamas-Akseki autochthone at northeastern parts of the basin. At central parts of the Altınkaya formation basin, it is laterally interfingering with turbiditic Definition an nomenclature.- The all ba- deposits of the Karpuzçay formation. This bo- sal conglomerates developed during different undary relationship is best observed in Köprü- stages of Miocene in Antalya Miocene basin lü Canyon. The Aksu formation unconfor- were considered under the name of Aksu formably overlies the Altınkaya formation (Brunn mation and have been dated as Oligocene- etal, 1971). Tortonian by Akay and Uysal (1984) and Akay Lithology.- The dominant lithology in the et al., (1985). Şenel et al., (1992, 1997b, formation is the marinal conglomerates. In so- 1998) considered the continental conglome- me levels, the sandstone, shale, claystone rates, developed at the base of Upper Burdi- and sometimes reefal limestones are also galian - Langhian units, as the Sevinç conglo- present. The conglomerates are generally merates and Tortonian conglomerates as the sandy conglomerate and pebbly sandstone in Aksu formation. They also named the conglo- types and they are dark gray colored, welllithi- merates deposited during Late Burdigalian- Langhian time interval at northeastern part of fied, carbonate cemented and the pebbles are the basin as Aksu formation. Dumont (1976) radiolarite, chert and limestone in origine. In considered the same unit as the Kesme cong- Aşağıyaylabel section, the formation transg- lomerates. In this study, this unit not differen- ressively overlies the Anamas-Akseki au- tiated from Aksu formation will be considered tochthone and starts with marinal conglome- as Altınkaya formation. rates at the base and succeded up by yellow colored silty fine-grained sandstones, transiti- Type section locality.- It is not possible to onal to reefs. Upwards, the marinal units with observe the whole formation in one locality. brackish water levels intercalate once more The type section locality has been chosen and the sequence ends regressively. The se- along the road continues towards Altınkaya quential development like Aşağıyaylabel sec- village (historical Selge city and theatre) loca- tion was also observed in Hocalarsırtı section. ted at northwest of Beşkonak. In this case, the thickness of coral reefs and Reference section localities.- These are intercalated underlying conglomerates can Ute Asağıyaylabel section (Isparta M26c4) lo- not be measured due to unsuitable topograp- THE MOLLUSCAN FAUNA AND STRATIGRAPHY OF ANTALYA MIOCENE 41

hic conditions. Also their boundary relation es upward with 80 cm thick greenish gray with basement rocks were not observed. The claystone, 40 cm thick matrix-supported observable lowermost part of the section conglomerates, 70 cm thick fine-grained starts with 1 m thick marinal conglomerates, sandstone with clay intercalation, 2.2 m thick overlain by the 22 m thick sandstone, gre- green-blue colored fine grained clayey sands- enish gray colored claystone. The sandstone tone and 3 m thick green-blue colored clays- beds are 10-30 cm in thickness and become tones with thin coal seams. At uppermost more thicker at upper part. The 80 cm thick, part, the 2 m thick matrix-supported conglo- small pebbly fine-grained sandstone bed with merates were observed. scored base, overlies overlying this level. The The thin coal seams developed within sequence continues with 2 m thick greenish the formation are similar to the levels in the gray colored claystone. As it is explained be- Altınkaya and Hocalarsırtı sections. low, the section is rich in molluscan fauna rep- Thickness and distribution.- It is about resenting brackish water-marine conditions 600 m, although the thickness changes late- with nearly the same salinity of marine water. rally. The H1 sample is rich in molluscan fauna Fossil content and age.- The moluscan representing brackish water - marine environ- fauna, found within sections measured from ment in this unit. It yields Tinostoma woodi different localities of Altınkaya formation, indi- (Homes), Pirenella gamlitzensis gamlitzensis cate generally Upper Burdigalian - Langhian (Hilber), Terebralia bidentata cingulatior Sac- (Ottnangian-Karpatian-Lower Badenian) age co, Terebralia lignitarum (Eichwald), Terebra- also supported by the other faunas. lia lignitarum lignitarum (Eichwald), Terebralia The molluscan fauna hasn't been found subcorrugata d'Orbigny and Cerithium at lowermost part of Altınkaya section. Howe- (Ptychocerithium) turhtoplicatum Sacco of ver, in the sandstone-marl intercalations of class Gastropoda; Gastrana fragilis (Linne), this level, the nannoplankton flora such as Sanguinolaria (Soletellina) labordei (Baste- Coccolithus pelagicus (Wallich), Sphenolithus rot), Pelecyora (Cordiopsis) islandicoides conicus Bukry, Cyclicargolithus abisectus Lamarck, Pelecyora (Cordiopsis) polytropa (Muller), Calcidiscus leptoporus (Murray- suborbicularis (Goldfuss) and Irus (Paphirus) Blackman), Dictyococcites productus (Kampt- gregarius Partsch from class Bivalvia. Based ner), Dictyococcites bisectus (Hay-Mohler- on these molluscan fauna, this part of the Wade), Reticuloenestra umblica (Levin) and section represents the stage of Upper Coronocyclus nitescens (Kamptner) were de- Burdigalian (Karpation) (Table 1a, 1c). The tected. This flora indicate and give the Lower accumulation of thick and coarse shell frag- Miocene age (identified by H. Karakullukçu). ments (20-35 cm) of Crassostrea gryphoides In the same unit, rare planktonic foraminifera (Schlotheim) bearing fine-grained siltstones was found such as Globigerinoides bispheri- conformably overly this unit. With this level, cus Todd which is known to be appeared in the Langhian (Early Badenian) starts and it Early Burdigalian (identified by A. Hakyemez). can be also correlated with A14 sample num- For this part of the section mentioned above, oer of Aşağıyaylabel and S3-S4-S5 sample althought there is no presence of the mollus- numbers of Altınkaya measured sections. can fauna, considering its stratigraphic positi- This level is succeded up by 2-4 m thick fine- on and the presence of nannoplankton as- grained pebbly coarse sandstones. It continu- semblage and planktonic foraminifer fauna, 42 Yeşim İSLAMOĞLU

its age was accepted as Upper Burdigalian (sample A4), the Tarbellastraea reussiana (Ottnangian-Karpatian). After a 5 m thick co- (Milne Edwards and J. Haime) and Favites vered interval, 50 cm thick ctaystones with neglegta (Michelotti) corals were found (iden- thin coal seams were observed. Upward, yel- tified by S. Babayiğit). The sequence continu- low colored, silty fine grained sandstone (S3) es with 60 cm thick clayey limestone and 5 m containing 70-80 cm thick accumulations of thick limestone including Porites sp frag- the Crassostrea gryphoides (Schlotheim) of ments. In this level a sample as A6 many class Bivalvia are present. For this level, the Gastropoda representing low-salinity marine age of the sequence was accepted as Lang- environment as Neritine picta (Ferussac), nian (Lower Badenian) based on the presen- Hydrobia (Hydrobia) frauenfeldi frauenfeldi ce of the Crassostrea gryphoides (Schlothe- (Hoernes) and Tinostoma woodi (Hoernes) im). Overlying this level, the section continues were found. In the sample A7 taken from 3 m with nearly 280 m thick marine conglomerates thick clayey limestone, Bivalvia as Ostrea la- and ends with 6 m thick coral reefs observed mellosa Brocchi, corals as Siderastraea cre- around antique theatre. Within the S6 sample nulata (Goldfuss) Porites sp. (identified by S. number of coral reefs as Ostrea lamellosa Babayiğit) and ostracoda as Bairdia sp. (iden- Brocchi, Spondylus crassicosta ornatulina tified by M. Duru) were found. Sacco and Venus (Venus) excentrica Agassız After 2 m thick cover, light greenish gray were identified. This fauna also indicate the colored, 2 m thick fine grained pebbly, silty Langhian (Lower Badenian) age. At the lower- clay overlies the unferlying levels. In the most part of the Aşağıyaylabel section, the sample A8, the corals as Siderastraea crenu- identified Gastropods are Turritella (Turhtella) lata (Goldfuss), Sedirastraea miocenica rricarinata (Brocchi), Turritella (Archimediella) (Osasco) and Porites collegniana (Michelin) bicarinata Eichwald, Chrysallida (Parthenina) were found (identified by S. Babayiğit). The mterstincta (Montagu) and Cerithium (Tiara- level of sample A9 taken for nannoplankton is cerithium) pseudotiarella D'Orbigny which the 70 cm thic and is composed of greenish gray last one became extinct at the end of Burdiga- lian. This unit also includes benthic foramini- colored, parallel laminated clay stone conta- fera as Borelis sp., Elphidium sp., Miliolidae ining no nannoplanktons. The section conti- (identified by E. Sirel) and ostracoda as Auri- nues with light yellow colored, 60 cm thick cla- la) cicatricosa (Reuss) survived in neritic envi- yey siltstone. Sample A10 taken from this le- ronment and widely distributed in Middle-Up- vel yielded following marine Gastropod fauna per Miocene (identified by M. Duru). The yel- are Alvania ispartaensis n.sp., Alvania (Alva- low colored silty sandstones are transitional to nia) curta (Dujardin), Alvania (Alvania) venus 6 m thick and 40 m wide reefal limestones. d'Orbigny), Triphora adversa miocenica Sample A2 collected from this level contains Cossmann ve Peyrot, Turritella (Turritella) tri- Heliastraea sp., Stylophora reussina (Monta- carinata (Brocchi), Turritella (Zaria) spirata rano-Galitelli) like coral fauna (identified by S. (Brocchi), Cerithium (Thericium) vulgatum mi- Babayiğit). Also in sample A2a, the benthic ocenicum (Vignal), Cerithium (Thericium) eu- foraminifera (A3) as Borelis melo (Fichtel and ropaeum graciliornata (Sacco), Cerithium Moll) and Borelis curdica (Reichel) (identified (Ptychocerithium) turritoplicatum Sacco, Co- by E. Sirel), indicate the Upper Burdigalian- nus conoponderosus (Sacco) and Conus stri- Tortonian age and marine environment with atulus Brocchi. The sample A11 taken from low salinity. In the overlying reefal limestones greenish gray colored 1.6 m thick clays with THE MOLLUSCAN FAUNA AND STRATIGRAPHY OF ANTALYA MIOCENE 43

thin clayey limestone intercalation also yielded section has been accepted as Langhian (Lo- Gastropoda as Neritina picta (Ferussac), wer Badenian) based on the molluscan fauna. Hydrobia (Hydrobia) frauenfeldi frauenfeldi The sample H1 in Hocalarsırtı section is (Hoernes) characterizing brackish water- rich in moluscan fauna which represents the marine environment. No fauna was found in low salinity marine environment. The identifi- yellowish colored 10 cm thick carbonate ed Gastropods are Tinostoma woodi (Hor- cemented sandstone (A12 sample). nes), Pirenella gamlitzensis gamlitzensis (Hil- Towards the upper part of the section is ber), Terebralia bidentata cingulatior Sacco, represented by greenish gray colored, 1.1 m Terebralia lignitarum (Eichwald), Terebralia thick, thin laminated claystones and continues lignitarum lignutarum (Eichwald), Terebralia with yellow colored, 10 cm thick, carbonate subcorrugata d'Orbigny and Cerithium cemented sandstone. The greenish gray colo- (Ptychocerithium) turritoplicatum Sacco. The red 4 m thick claystones with increasing Bivalves are Gastrana fragilis (Linne), Sangu- sandstone intercalations are succeded up by inolaria (Soletellina) labordei (Basterot), Pe- yellow colored, parallel lamimated 2.5 m thick lecyora (Cordiopsis) islandicoides Lamarck, coarse-grained pebbly sandstones with sco- Pelecyora (Cordiopsis) polytropa suborbicula- red bases. Within the 1 m thick greenish gray ris (Goldfuss) and Irus (Paphirus) gregahus claystone the identified Gastropods are Neri- Partsch. Based on the mentioned molluscan tina picta (Ferussac), Terebralia sp. and Val- fauna, the age of the section at this level was vata sp. (sample A13) which also characteri- assigned as Upper Burdigalian (Karpatian) zing the low salinity marine conditions. The (Table 1a-b-c). The Langhian (Lower Badeni- section continues with yellow colored, carbo- an) starts with the Crassostrea giyphoides nated, sandy siltstone. In thp 1 m interval of (Schlotheim) found as accumulation of thick yellow colored silty sandstone, the Gastropo- and coarse shell fragments (20-35 cm) overl- da fauna as Turritella (Turritella) thcarinata tri- ying the basal level. This level can be correla- carinata (Brocchi), Turritella (Turritella) turris ted with other measured sections in the basin, Basterot and Polinices (Polinices) redemptus such as, sample A14 of Aşağıyaylabel and (Michelotti) indicating the marinal conditions sample S3, S4 and S5 of Altınkaya measured were found (A14). This part of the section was stratigraphic sections. dated as Upper Burdigalian (Ottnangian-Kar- Depositional environment.- The Altınka- patian) based on this fauna (Table 1). ya formation contains molluscan fauna which From this level upward, the sequence generally indicates the low salinity brackish includes Bivalvia as Crassostrea giyphoides water-marine environments. Especially, in (Schlotheim) which can survive in very low Hocalarsırtı and Aşağıyaylabel sections the salinity environments. The other species are euryhaline mollusc species survive in low sa- the Ostrea lamellosa Brocchi and Pycnodon- linity environment were detected in greenish te germanitala (De Gregoria) which their shell gray colored claystones. In this sections, also fragments accumulated in 70 cm thick siltsto- in the Altınkaya section, the accumulation of ne and adopted themselves to salinity chan- shell fragments of the Crassostrea giypho- ges in environment. Uppermost part of the se- ides (Schlotheim) were detected which deve- quence is characterized by 5 m thick marinal loped in much lower salinity environments conglomerates. The age of this part of the (Cox et al., 1969). These levels are intercala- 44 Yeşim İSLAMOĞLU

ted with marinal units. The intercalations of by Monod (1977). It was previously named as molluscan fauna representing low salinity ma- Burdigalian limestone by Altınlı (1943) and rine environment and small-scale coral reefs Miocene limestone facies by Blumenthal indicate tidal changes in sea level throughout (1951). Later, Derman (1977) and Aköz the time. This change is especially well-obser- (1981) used the name as Sakseydi limestone ved in Aşağıyaylabel section. The benthic fo- and Naz et al., (1992) considered it under the raminifera encountered within sandy limesto- name of Oymapınar formation. Akay and Uy- nes of this section are Borelis melo Fichtel sal (1984), Akay et al. (1985) and Şenel et al., and Moll and Miliofidae representing back re- (1992, 1996) adopted and used the same na- ef-lagoon environmental conditions (identified me as Oymapınar limestone. by E. Sirel). Type-section locality.- It is located at slo- In the formation, similar to the Altınkaya pe of Manavgat stream, 3 km north of Oyma- section, the nannoplanktons and planktonic pınar. foraminifera implying the deeper and more Reference sections.- Two reference sec- saline environmental conditions were found. tions sections are observed; one is located at As it is seen from the Altınkaya and Aşağıyay- 4.5 km northwest of Taşağıl, the Radioring label sections the presences of algae and and the other is situated about 700 m southe- small patchy reefs indicates the marine envi- ast of Ballıbucak village, the Ballıbucak secti- ronment. on. The geochemical analyses were carried Lower-Upper boundary relations.- This out on shell fragments of molluscs found in unit unconformably overlies the Alanya nap- Hocalarsırtı, Aşağıyaylabel and Altınkaya pe, Antalya nappes and Anamas-Akseki au- sections to interprete the paleoecological con- tochthone and conformable over the Sevinç ditons. These analyses also imply the presen- conglomerate. The Oymapınar limestone is ce of cold and low saline marine water condi- conformably overlain by the Çakallar formati- tions (İslamoğlu, 2001). The faunal data from on at southeast of the basin and Geceleme the formation also support this idea. Although formation in Oymapınar section. It is uncon- the euryhaline molluscs are abundant, the formably overlain by the Aksu formation in stenohaline nannoplanktons and planktonic Ballıbucak section. foraminifera are not abundant and diverse in the section (Flecker et al. 1995 and Hakyemez, Lithology.- The Oymapınar limestone is 2001, personal communication). It is obser- composed of medium-thick bedded, polyge- ved that, the types and number of diversity nic base conglomerate, sandstone, white- are less and the wall structures of the plank- gray colored hard, sandy limestone, algal li- tonic foraminifera were destroyed (Hakye- mestone, massive limestone, coral-algae re- mez, personal communication). This is interp- efal limestone and mudstone. It sometimes reted that, the environmental salinity and tem- starts with conglomerate or sandstones and perature conditions were not suitable for the continues with reefal limestone and with mas- surviving of planktonic foraminifera. sive limestones. The sequence in Oymapınar section transgressively overlies the Alanya The Oymapınar limestone nappes and it starts at the base with 20 m Definition and nomenclature.- Oymapı- thick, red colored poorly sorted and angular nar limestone as a formation was first given conglomerates (Fig. 3). The limestone brecci- THE MOLLUSCAN FAUNA AND STRATIGRAPHY OF ANTALYA MIOCENE 45

as are exposed following the conglomerates The sequence continuing with green colored, at the slope face to measured section locality. 50 cm thick clays with coal seams, is later These breccias indicate the tectonic activity transitional to light colored, 3 m thick massive which is known to be developed at the begin- sandy limestones. The sample O3 from this ning of the Miocene in the region (Akay et al., level contains Pecten fuschi Fontannes, 1985; Şenel et al., 1992, 1996). The terrestri- Chlamys (Aequipecten) scabrella bollenensis al conglomerates are followed by greenish (Mayer). Venus (Ventricoloidea) multilamella yellow colored, small pebbly 1.55 m thick (Lamarck) characterizing also marine envi- sandstones. These are succeded up by green ronment. Overlying this level, is the 27 m colored, 60 cm thick claystones and greenish thick, sometimes claystone intercalated with yellow, 1.8 m thick, semi-lithified siltstones. hard, massive algal limestones. Sample O4 in In Alarahan section, the topmost 10 m is this unit includes planktonic foraminifera Ca- represented by white-gray colored very hard, tapsydrax sp., Globigerinoides trilobus (Re- massive, algae limestones which are the Oy- uss) representing Burdigalian age (identified mapınar limestone (Fig. 2). by A. Hakyemez). Based on these data, it is In Radioring section, the Oymapınar li- accepted that this part of the sequence repre- mestone overlies conformably the 5 m thick sents the Upper Burdigalian (Karpatian) stage marinal conglomerates and continues with 2 (Table 1). m thick, algae, distributed pebbly, sandy li- At the locality of Oymapınar section, the mestone (Fig. 4). olistoliths derived from coral reefs of the Oy- In Ballıbucak section, the sequence aga- mapınar limestone are found in Geceleme for- in starts transgressively and at the base it mation. The thin sections prepared from the contains thick, massive, sandy, poorly sorted, samples of this olistolits indicate Upper Burdi- grain-supported conglomerates. It continues galian - Tortonian age based on the benthic with 3 m thick, small pebbly, bioclastic limes- foraminifera suchs as Borelis melo (Fichtel tone containing coral and mollusc fragments. and Moll), Borelis cf. curdica (Reichel), Amp- In sample B1 of this level, the Ostrea sp. was histeginasp., Planorbulinella sp., Lepidocycli- found. Upward, the sequence continues with na sp., Operculina sp., Miliolidae, Rotaliidae, 10 m thick sandy limestone and marl alterna- Victoriellidae (identified by E. Sirel). The fa- tion. una also confirms the Upper Burdigalian (Kar- patian-Lower Badenian) age formation the Thickness and distribution.- Although the Oymapınar limestone in this section. thickness is changeable, it reaches up to 100 In Alarahan section, the uppermost parts m. of the formation were dated as Langhian ba- Fossil content and age.- The molluscan sed on planktonic foraminifera. These levels fauna identified in the Oymapınar limestone indicate that the environment was deeper indicate generally Upper Burdigalian-Langhi- Gastropod and Bivalve fauna were not detec- an (Karpatian-Lower Badenian) age (Table ted there. However, there was abundance of 1). The Bivalve as Pitar (Pitar) rudis (Poli) and planktonic foraminifera, the sample A5 inclu- Gastropod as Terebralia sp. found in sample des Praeorbulina glomerosa glomerosa O2 reveal the shallow marine environment. (Blow), Praeorbulina glomerosa curva (Blow) 46 Yeşim İSLAMOĞLU

and Praeorbulina sicana de Stefani which ne). These fauna represent marine environ- characterizing the transition to Langhian ment and indicate Upper Burdigalian (Karpa- (identified A. Hakyemez). The Praeorbulina tian) age. They include both Mediteranean sp. appeared at the beginning of the Middle Tethys and Central Paratethys species. For Miocene and indicates a great distribution this reason, the age of the section was esti- both Mediterranean Tethys Langhian and mated as Upper Burdigalian (Karpatian) ba- Central Paratethys Lower Badenian (Steinin- sed on the molluscan fauna (Table 1). ger and Rogl, 1984; Rogl, 1998). Although it In Ballıbucak section, within sample B2, was not found in Alarahan section, the pre- the Bivalves and Gastropods characterizing sence of turbiditic deposits of Serravalian and marine environment were found. The Bivalves Tortonian in the region has been determined are Anadara (Anadara) diluvii (Lamarck), in the other studies (Öztümer, 1974; Akay ve Chlamys (Aequipecten) scabrella bollenensis Uysal, 1984; Akay ve dig., 1985; Naz ve di- (Mayer), Codakia leonina (Basterot), Acant- ğerleri, 1991, 1992; Şenel, 1996). The samp- hocardia (Acanthocardia) turonica (Mayer), le R1 in Radioring section is taken from 2 m Tellina (Peronaea) planata Linne, Megaxinus thick algae pebbly, sandy limestone and bent- bellardianus (Mayer) whereas the Gastropod hie foraminifera assigning to Upper Burdigali- is-Athleta ficulina (Lamarck). At the basal part an-Tortonian age were found in this level. of the 15 m thick massive algae-coral reefal li- These are Borelis cf. melo (Fichtel and Moll). mestone Miliolidae was obtained (Sample Borelis curdica (Reichel), Planorbulinella sp., B3). After this level, again at the lower part of Textularia sp., Amphistegina sp. (identified by the 15m thick limestones, the Heterostegina E. Sirel). 22 m Thick coral and algae reefal li- sp., Miliolidae type benthic foraminifera were mestone overlies this level. The sample R2 obtained and algal abundance increase to- also includes benthic foraminfera as Borelis wards up the section. The sequence foramini- cf. melo (Fichtel and Moll), Amphistegina sp., fera were obtained and algal abundance inc- Textularia sp., Operculina sp., Archaias ? sp., rease towards up the section. The sequence Miliolidae (identified by E. Sirel) Later, it is 10 continues with 3 m thick marls and 20 m thick m thick, white colored limestone with rodolit- reefal limestone where the algae and corals hes (identified by. N. Atabey) and the section become abundant. The age of the this part of ends with 1 m thick yellow colored sandstone. the section was accepted as Upper Burdigali- In sample R3 of this level, the following mol- an (Karpatian) based on the molluscan fauna luscan fauna were found; Anadara (Anadara) (Table 1). The 15 m thick conglomerates un- diluvii pertransversa Sacco, Chlamys (Aequ- conformably overlie the limestone levels. The- ipecten) scabrella bollenensis (Mayer), Telli- se conglomerates are conglomerate could be na (Peronaea) planata Linne, Venus (Ventri- suggested as Tortonian due to its stratigraphi- coloidea) multilamella (Lamarck), Carditame- cal position. It can be assumed that this for- ra (Lazariella) striatellata (Sacco), Cardiocar- mation formed in transgressive and reefal dita cf. monilifera (Dujardin), Acanthocardia conditions. (Acarthocardia) turonica (Mayer), Cardium kunstleri Cossmann ve Peyrot, Tellina (Pero- Depositional environment.- The formati- nidia) planata Linne, Venus (Ventricoloidea) on is generally reflecting transgressive and multilamella (Lamarck), Dosinia lupinus (Lin- reefal characteristics. THE MOLLUSCAN FAUNA AND STRATIGRAPHY OF ANTALYA MIOCENE 47 48 Yeşim İSLAMOĞLU THE MOLLUSCAN FAUNA AND STRATIGRAPHY OF ANTALYA MIOCENE 49 50 Yeşim İSLAMOĞLU

The Çakallar formation Lower-Upper boundary relations.- Gece- leme formation crops out only in the southe- Definition and nomenclature.- Akay and ast part of the basin and it lies conformably Uysal (1984) and Akay et al., (1985) defined between Oymapınar limestone and çarpuz- this unit which is composed of breccia limes- cay formation. At southeast of the basin, it is tone. It is onlyobserved at southeast part of transitionally overlying the Çakallar formation. Antalya Miocene basin. Lithology.- The formation is generally Type section locality.- This unit is crop- composed of marls and clayey limestones. ped out at eastern part of the basin and its The thinmedium bedded, light gray, greenish type locality is at the eastern slope of Alara gray, green, dark colored clayey - sandy li- stream to the west of Çakallar. mestone, claystone and siltstone levels are Lower-Upper boundary relations.- It con- also observed. In the Oymapınar section, the formably overlies Oymapınar limestone with a Geceleme formation is represented by 1.3 m sharp contact relation. thick, light gray colored marls and continues Lithology.- It is brecciated and represen- with 30 m thick, sandstone intercalated marl. ted by beige-dirty yellow colored, clayey li- It also contains limestone blocks derived from mestone-limestone alternations. Oymapınar limestone. Thickness and distribution.- The unit is Thickness and distribution.- The thick- about 80 m thick and displays a lenticular ge- ness of the unit was measured as 410 m by ometry. Akay etal., (1985). Fossil content and age.- The identified Fossil content and age.- No age data has fossils are the Bivalves and Gastropods. The been found in the unit. Since it is overlying the age of the formation was accepted as Langhi- Upper Burdigalian Oymapınar limestone and an based on the microfossil assemblage. In underlying the Geceleme formation, its age Oymapınar section, the sample O5 yields He- was accepted as Upper Burdigalian-Lower licosphaera kamptneri Hay-Mohler, Cyclicar- Langhian. golithus abisectus (Muller), Calcidiscus lepto- Depositional environment.- It reflects the porus (Murray-Blackman), Dictyococites pro- slope environmental conditions. ductus (Kamptner), Dictyococites bisect us (Hay-Mohler-Wade), Sphenolithus hetero- The Geceleme formation morphus Deflandre, Coccolithus pelagicus Definition and nomenclature.- The unit (Wallich) and Pontosphaera sp. like nannop- was firstly named as Geceleme marls by Blu- lanktons of biozones NN5 (Langhian-Lower menthal (1951), Monod (1977), Akay and Uy- Serravalian) (identified by H. Karakullukçu sal, (1984); Akay et al., (1985); Şenel et al., and E. Erkan) and planktonic foraminifera (1992); Naz et al., (1992) adopted the same Praeorbulina glomerosa glomerosa (Blow) name. characterizing Langhian age (identified by A. Hakyemez). After 1.2 m thick sandstone level, Type section locality.- The type locality of the 2 m thick marls are observed. In this level, the unit is located at 1 km north of Gençler vil- again Helicosphaera kamptneri Hay-Mohler, lage. Sphenolithus heteromorphus Deflandre, Reference section.- It is partly observed Sphenolithus conicus Bukry, Sphenolithus in Oymapınar section. compactus Backman, Dictyococites produc- THE MOLLUSCAN FAUNA AND STRATIGRAPHY OF ANTALYA MIOCENE 51

tus (Kamptner), Dictyococcites antarcticus Thickness and distribution.- It has a vari- Haq, Coccolithus pelagicus (Wallich7, Bra- able thickness throughout the basin. It was arudosphaera bigelowi (Gran-Braarud). Dis- measured as 2050 m between Kızıldağ-Kara- coasfersp. corresponding to NN5 biozone of bekir. nannoplankton flora are present (Langhian- Fossil content and age.- It was not studi- Lower Serravalian) (identified by H. Karakul- ed in detail because of absence of molluscan lukçu, E. Erkan). Based on these data of the fauna. Based on its planktonic foraminifera age was accepted as Langhian. and nannoplankton contents, its age was ac- Depositional environment.- The presen- cepted as Upper Burdigalian-Tortonian. ce of abundant planktonic foraminifera and Depositional environment.- The presen- nannoplankton flora, reveals relatively deep ce of synsedimentary fold and slump structu- marine environment. res implies turbiditic characteristics.

The Karpuzçay formation The Aksu formation Definition and nomenclature.- Previously Definition and nomenclature.- In the regi- defined units such as flysch and conglomera- on, the Tortonian molassic conglomerates te (Altınlı, 1943), partly Beşkonak formation has been considered as Aksu conglomerate (Eroskay, 1968), Manavgat molasse (Monod, by Poisson (1977) and Aksuçayı formation by 1977) Kargı molasse (Poisson, 1977) have Akbulut (1977). Akay and Uysal (1984) and been combined under the name Karpuzçay Akay et al. (1985) defined the unit as Aksu formation, since they mapped the conglome- formation by Akay and Uysal (1984), Akay et rates over and under the unconformity plane al., (1985) which is best observed along the below Langhian age. However, they were Karpuzçay stream. unable to separate these conglomerates. Naz Type section locality.- The type section et al., (1992) defined this unit as the Aksu of the formation strats at 2 km west of Genç- member of Karpuzçay formation. Şenel et al., ler village and continues along the ridge loca- (1992, 19976, 1997c) mapped and defined ted between two branches of Karpuzçay stre- the Tortonian rock units as Aksu formation. In am. this study based on the Poisson (1977) and Akbulut (1977) definitions, the name Aksu for- Lower-Upper boundary relations.- The mation is adopted, since the type section of unit is widely cropped out in all parts, of the ba- molassic deposits is located along Aksu stre- sin. It conformably overlies Oymapınar limes- am. Due to stratigraphic and faunal environ- tone and Geceleme formation at central and mental differences of the unit, the "Aksu for- southeastern part of the basin respectively. At mation" definition applied for whole basin by the west of the basin, it is overlain by Aksu Akay and Uysal (1984) and Akay et al., (1985) formation, in other parts it is, either unconfor- should be separated and the "Aksu formation" tnably overlain by Pliocene rock units or expo- definition must be used for Serravalian-Torto- sed as recent erosional surface. nian molassic deposits which are exposed at Lithology.- It is cdmposed of gray, green west of the basin. greenish gray, beige, dirty yellow colored, Type section locality.- The type section thinmedium-thick-bedded sandstone, conglo- of the formation is best observed at junction of merate, siltstone, claystone and detritic limes- Sinne stream with Aksu stream in Eskiköy vil- tones. lage (Akay et al., 1985). 52 Yeşim İSLAMOĞLU

Reference section.- It is also observed in , philippi (Monterosato), Conus conopondero- Kargı section. Sus (Sacco), Conus mercati Brocchi, Conus (Conolithus) dujardini Deshayes and Terebra- Lower-Upper boundary relations.- The lia sp., Cerithium sp. The following level is the Aksu formation unconformably overlies the 64 cm thick gray colored mudstone in which basement at the locality 5 km to the south- Cerithium sp. was obtained (K5). west of Kargı tunnel. It is conformably overlying the Karpuzçay formation. Its relation with Overlying this level is the gray colored. Altınkaya formation has not been differenti- 17 cm thick mudstone with, laminated coal se- ated yet. In the region, the presence of a un- am. In this level (sample K6), Gastropods as conformity is known between Lower-Middle Alvania (Alvania) curta (Dujardin), Chrysallida Miocene and Tortonian (Brunn et al., 1971). (Parthenina) interstincta (Montagu), Odosto- Lithology.- It is generally composed of al- mia (Megastomia) conoidea (Brocchi), Valva- ternations of red, reddish brown, yellowish ta sp., Cerithium sp. Alvania (Alvania) curta green colored, thick bedded, molassic sands- (Dujardin), Chrysallida (Parthenina) interstinc- tone and conglomerates. At some levels, the ta (Montagu), Odostomia (Megastomia) cono- dark gray, brown colored marls and sandsto- idea (Brocchi), Valvata sp., and Cerithium sp. nes, gray colored limestones, algae and coral were determined. reef limestones and locally very thin coal se- After 7 cm thick, white colored clay level, ams are also present. the Cerithium sp.was found (K7) within 60 cm The reddish brown colored conglomera- thick, gray colored mudstones with coal se- te-sandstone alternation forming the lower am. In the overlying 30 cm thick fine-grained part of the formation is considerably thick and sandstone, the Chrysallida (Parthenina) in- observed along the road arrived Kargı. It was terstincta (Montagu), Cerithium sp. of class not measured as no fossil record was obta- Gastropoda and Tellina (Peronaea) planata ined in this unit. Linne of class Bivalvia were identified (K8). The Kargı section starts at the base with The sample K9 was taken from the level 3 m thick altenations of conglomerate, sands- which is represented by 4 cm thick, white co- tone and mudstone. No fossils was observed lored lenticular claystone followed by 5.5 m from this level (sample K1). Over this level, thick, coarse grained pebbly sandstones. The me 11 m thick, massive, gray colored, algae (K9) sample yields Astraea (Bolma) rugosa and coral reefal limestone succeds. The (Linne), Cypraea (Adusta) subamygdalum sample K2 taken from this unit yields Tortoni- d'Orbigny, Conus conoponderosus (Sacco), an age based on the Molluscan fauna as Po- Conus (Conolithus) dujardini Deshayes of ntes lobatosepta (Chevalier), Tarbellastraea class Gastropoda and Tellina (Peronaea) pla- siciliae (Chevalier), Tarbellastraea reussiana nata Linne of class Bivalvia. The gray colored, (Milne-Edwards and J. Haime), Siderastraea massive, algae and coral reefal limestones crenulata (Goldfuss), Tarbellastraea sp., Aqu- 4.5 m thickness overly the conglomerates. itanastraea sp. and in the K3 sample taken The sample K10 and K11 were collected from from uppermost of reefal limestone, continues this level and they contain the corals, as Pori- with 30 cm thick yellow colored sandstone. In tes lobatosepta (Chevalier), Tarbellastraea si- the sample K4 of this level, the Gastropods ciliae (Chevalier), Favites neglegta (Michelot- are represented by Cypraea (Bernaya) faba- ti), Aquinastraea sp., Porites sp. implying Tor- gina (Lamarck), Gibberulina (Gibberulina) tonian age (determined by S. Babayiğit). THE MOLLUSCAN FAUNA AND STRATIGRAPHY OF ANTALYA MIOCENE 53

The brown-colored, 2.5 m thick mudsto- The section upward with increasing bed ne overlies the reefal limestone. Many gastro- thickness of 2 m thick sandstone - mudstone pods and bivalvia were obtained from sample intercalations. This level is overlain by yellow K12 taken from mud stone level. Gastropods colored 15 cm thick, pebbly coarse-grained are Astraea (Bolma) rugosa (Linne). Tinosto- sandstone, gray colored 15 cm thick, fine-gra- ma woodi (Homes), Alvania (Alvania) curia ined sandstone and 8 cm claystone. The (Dujardin), Alvania (Alvania) venus (d'Or- sample K 15 from the mudstone of 7 m thick bigny), Alvania tanerae n. sp., Turritella (Za- sandstone-mudstone alternation includes ria) spirata (Brocchi), Turritella (Archimediel- Gastropoda as Conus mercati Brocchi ve Su- rdi bicarinata (Eichwald), Chrysallida (Parthe- bula (Oxymeris) plicaria (Basterot). The 20 nina) interstincta (Montagu), Erato (Erato) la- cm thick sandstone and 2 m thick pebbly co- evis elongata Sacco, Natica millepunctata La- arse-grained thick sandstone overlies the for- marck, Arcularia (Arcularia) ringicula (Bellar- mer level. The sample K16 collected from di), Mangelia brachystoma (Philippi), Conus pebbly sandstone contains Xenophora infun- conoponderosus (Sacco), Conus mercati dibulum Brocchi, Strombus (Strombus) bonel- Brocchi and Cerithium appenninicum derto- /ii Brongniart, Strombus coronatus Defrance, sulcata Sacco whereas. The Bivalves are Galeodes cornutus (Agassız), Latirus (Dolic- Anadara (Anadara) diluvii (Lamarck), holatirus) dispar(Peyrot), Mitra (Mitra) fusifor- Cniamys (Aequipecten) scabrella bollenensis mis (Brocchi), Athleta ficulina (Limarcks), Co- (Mayer), Parvilucina (Microloripes) dentatus nus conoponderosus (Sacco), Conus striatu- ( Defrance), Loripes (Lonpes) dujardini (Des- lus Brocchi and Cerithium appenninicum der- hayes) and Laevicardium (Laevicardium) ob- tosulcata Sacco of class Gastropoda and longum (Chemnitz) (Table 1),. Also in the sa- Anadara (Anadara) diluvii (Lamarck), Linga me level (K12), the Rotaliidae type benchic (Linga) columbella (Lamarck), Megaxinus bel- foraminifera (determined by. E. Sirel) and lardianus (Mayer), Megaxinus (Megaxinus) Ostracoda as Bairdia sp. were determined ellipticus (Borson), Megaxinus (Megaxinus) (identified by M. Duru). transversus (Bronn) and Nemocardium spondyloides (Hauer) of class Bivalvia. Above this level, the brown-colored, 2.5 m thick, fine sadstone intercalated mudstone The level of sample K 17 is represented is present. In the 12 cm thick mudstone level, by the 50 cm thick gray colored mudstone and the sample K13 includes Gastropoda as Gib- rich in molluscan fauna. In this sample, gast- bula (Gibbula) magus (Linne), Astraea (Bol- ropods ane Gibbula (Gibbula) magus (Linne), ma) rugosa (Linne), Cerithium appenninicum Astraea (Bolma) rugosa (Linne), Turritella dertosulcata Sacco. Strombus (Strombus) bo- (Archimediella) bicarinata (Eichwald), Cerithi- ne//ii Brongniart Strombus cononatus Defran- um appenninicum dertosulcata Sacco, Strom- ce, Mitiella (Mitrella) liguloides (Doderlein), bus coronatus Defrance, Strombus coronatus Conus conoponderosus (Sacco), Conus stri- compressonana Sacco, Strombus (Strombus) atulus Brocchi. Conus striatulus Brocchi. Co- bonelli Brongniart, Erato (Erato) laevis elon- nus (Conolithus) dujardini Deshayes and Bi- gata Sacco, Cypraea (Bernaya) fabagina mi- vaivia as Anadara (Anadara) diluvii (Lamarck)-- oporcellus Sacco, Natica millepunctata La- and Parvilucina (Microlonpes) dentaius (Def- marck, Charonia stefaninii (Montarano), Mit- rance). rella (Mitrella) liguloides (Doderlein), Hinia 54 Yeşim İSLAMOĞLU

(Uzita) porrecta (Bellardi), Athleta ficulina (La- Odostomia (Megastomia) conoidea (Brocchi), marck), Voluta erentoezae n. sp., Conus co- Arcularia (Arcularia) ringicula (Bellardi), Man- noponderosus (Sacco), Conus (Chelyconus) gelia brachystoma (Philippi), Cerithium ap- fuscocingulatus Bronn, Conus mercati turricu- penninicum dertosulcata Sacco, Gibbula la Brocchi, Conus striatulus Brocchi, Conus (Gibbula) magus (Linne) and Charonia stefa- (Conolithus) dujardini Deshayes. Within this ninii (Montarano) indicate the Tortonian age. sample some Bivalvia as Anadara (Anadara) However, the typical molluscan fauna repre- diluvii (Lamarck), Linga (Linga) columbella senting Upper Tortonian (Robba, 1970) which (Lamarck), Parvilucina (Microloripes) denta- are Parvamussium (Parvamussium) duode- tus (Defrance), Megaxinus bellardianus (Ma- cimlamellatum (Bronn), Polinices (Lunatia) yer) and Megaxinus (Megaxinus) ellipticus catena helicina (Brocchi), Amycyclina semist- (Borson) were also determined. riata dertonensis (Bellardi), Hinia (Hinia) turbinella turbinella (Brocchi), Turricula (Knefastia) The sequence continues upward whith bellardii bellardi (Desmoulins), Gemmusa gray colored, 30 cm thick sandstone and dark (Gemmula) rotata rotata (Brocchi) and Gem- gray colored, 3.8 m mudstone with coal seam. mula (Gemmula) rotata coronata (Münster in In the sample K 18 taken from this level, the Goldfus) have not been found in this unit. For Strombus coronatus Defrance, Strombus this reason, the levels containing mollusc fa- (Strombus) bonellii Brongniart, Murex (Pse- una in Kargı section of the Aksu formation udomurex) becki Michelotti, Hinia (Uzita) por- was accepted as Lower Tortonian. recta (Bellardi), Conus conoponderosus (Sac- Corals as Porites lobatosepta (Chevali- co), Conus mercati Brocchi belonging to class er), Favites neglegta (Michelotti), Tarbellast- Gastropoda were identified. At the uppermost raea siciliae (Chevalier) Tarbellastraea reus- part, the section is represented by 75 cm thick siana (Milne-Edwards ve J. Haime) and Side- conglomerate, gray colored, mudstone inter- rastraea crenulata (Goldfuss) (determined by calated, thick bedded. 4 m thick sandstone, by S. Babayiğit) obtained from Kargı section brown colored 3 m thick mudstone. 30 cm also confirm the Tortonian age. thick sandstone and 4 m thick mudstone. The section is laterally transitional to sandstones Based on this idea, the age of the hund- and conglomerates towards the northwest red meter thick conglomerates underlying part. conformably the Kargı section of the Aksu formation should be stratigraphically Serrevalian Thickness and distribution.- The total in age. For this reason, overall age of the for- thickness of the formation was not measured. mation was accepted as Serravalian - Torto- However, it is known to be reached up to 450 nian. m in thickness (Akay et al., 1985). Depositional environment.- The formati- Fossil content and age.- In the formation, on represents the continental and shallow the molluscan fauna reveals Lower Tortonian marine environments. The marine environ- age and implies marine suptropic environment indicates shallow shelf-deep shelf repe- ment. The previously identified nannoplank- tition and the great abundance of molluscan ton flora submitted by Akay et al., (1985) is al- fauna was present in shallow shelf implying so confirmed this age assignment. warm and normal salinity marine environment In this unit, the molluscan fauna Gibberu- (suptropic climate). Coral reefs were develo- hna (Gibberulina) philippi (Monterosato), ped during deepening of environment. This THE MOLLUSCAN FAUNA AND STRATIGRAPHY OF ANTALYA MIOCENE 55

environmental change can be observed in was firstly named as the Altınkaya formation Kargı section (Fig. 9). in this study. The Altınkaya formation uncon- CONCLUSION AND DISCUSSION formably overlies the basement units. It is also interfingering with turbiditic deposits of The stratigraphical study related to the Karpuzçay formation outcropping at central molluscan fauna in the Antalya Miocene basin parts. It is unconformably overlain by Aksu was firstly established in this study. The stra- formation. This unit was previously investiga- tigraphy of the basin has re-evaluated by ted under the name Aksu formation. The pre- using all fossil records. vious researchers assigned Upper Burdigali- The oldest unit in the basin is the Kepez an - Langhian age which also support the age travertine. It stratigraphically underlies the data obtained during this study (Akay and Uy- Upper Burdigalian rock units (the Sevinç sal, 1984; Akay et al., 1985 and Tuzcu et al., conglomerate and the Oymapınar limestone). 1994). Since the unit is terrestrial in origine and has The other investigated unit in the basin is no reliable age data, the stage name was not the Oymapınar limestone. Its age was previ- used and its age was fixed as Lower Miocene. ously claimed to be Lower Langhian (Akay Another unit in the basin is the Sevinç and Uysal, 1984; Akay et al., 1985; Şenel et conglomerate cropping out at south and sout- al., 1992. 1996). This age has been modified heastern parts of the basin. This unit was con- as Upper Burdigalian - Langhian (Karpatian- sidered as Tepekli conglomerates by Monod Lower Badenian). The identified benthic and (1977). later it was mapped and defined as planktonic foraminifera and corals also con- Sevinç conglomerate by Gutnic et al. (1979). firm this age assignment. As it is pointed out by Şenel et al. (1992, The planktonic foraminifera and nannop- 1998), this unit is not only in continental cha- lankton obtained from the Geceleme formati- racteristics, but also includes marine levels. on which conformably overlies the Upper Bur- This evidence is also confirmed by other rese- digalian levels of the Oymapınar limestone, archers such as Monod (1977), Akay and Uy- also confirmed with age evidences of Öztü- sal (1984), Akay et al. (1985), Karabıyıkoğlu mer (1974), Akay and Uysal (1984), Akay et et al. (1996, 1997. 2000). The marine levels of al. (1985), Nazetal. (1991, 1992), Seneletal. the Sevinç conglomerate was dated as Upper (1991, 1992, 1996, 1998) and Karabıyıkoğlu Burdigalian. By considering the continental le- et al. (2000). vels of the formation, as a whole, its age was accepted as Burdigalian. The Çakallar formation conformably overlies the Oymapınar limestone and under- The Aksu formation was previously ge- lies the Geceleme formation and is observed nerallized to the whole basin by Akay and Uy- only at southeastern part of the basin. Altho- sal (1984) and Akay et al. (1985). In this case, ught it is brecciated and has no fossil record, clue to stratigraphic, faunal and environmental its age was accepted as Upper Burdigalian- differences, it has been thought that, it should Lower Langhian. oe differentiated. For this reason, the units exposed at central and northern parts of the ba- In this study, no detailed study was carri- sin and Upper Burdigalian-Langhian (Ottnan- ed out in widely exposed at west of the basin gıan-Karpatian-Lower Badenian) and conta- and the previously suggested Aksu formation ining brackish water-marine molluscan fauna- for the whole basin by Akay et Uysal (1984) 56 Yeşim İSLAMOĞLU

and Akay et al. (1985) has been modified. Akay, E.: Uysal, S.; Poisson, A.; Cravette, Y. and The levels of the formation containing mollus- Muller, C.. 1985. Antalya Neojen havzasının can fauna was dated as Lower Tortonian. The stratigrafisi. T.J.K. Bull., 28, 105-109. lower parts composed of alternations of thick . ; 1988. Orta Torosların Post-Eosen conglomerate and sandstone levels are tho- tektoniği. MTA Bull, 108, 57-68. ught to be Serravalian in age. Based on this Akbulut, A.. 1977, Etude geologique d'une partie du data, the age of the Aksu formation was Tarus occidental sud'Eğirdir (Turquie) These 3. Cycle Univ. Paris-Sud-Orsay. 203, (unpub- accepted as Serravalian- Tortonian but not lished). Tortonian as the previous investigators , 1980, Eğirdir gölü güneyinde Çandır (Sütçü- suggested (Akbulut, 1977: 1980; Şenel et al., ler, Isparta) yöresindeki Batı Torosların jeoloji- 1997 a,b,c; Şenel et al.. 1991, 1992, 1996. si, T.J.K. Bull., 23. 1, 1-10. 1998). Aköz, 6., 1981, Oymapınar tip stratigrafik kesitinin Nannoplanktonlarla biyostratigrafik inceleme- ACKNOWLEDGEMENTS si. TPAO Research Center Rep. No 399. This study is a part of the "Ph. Thesis" Altınlı, E., 1943, Antalya bölgesinin jeolojisi MTA Rep. fullfilled in, Institute of Natural and Applied No 858-59 (unpublished). Science, in Geological Engineering Depart- ———, 1945, Antalya bölgesinin tektonik etüdü, ment, Ankara University. The author is grate- İst.Üniv. Fen Fak. Mecm. Serie B, 10, p. 1. ful to General Directorate of Mineral Research Atabey, N., 1998, Batı Toroslar kuşağı Miyosen kırmı- and Exploration (MTA) for providing field and zı alglerinin paleoekolojisi ve çökelme ortam- laboratory facilities, TUBITAK authorities for ları. Proceeding of the 51 th Turkish Geol. Cong. Abstracts, 58. providing NATO A2 research scholarship, to Güler Taner (supervisor), Dr. Mustafa Şenel Blumenthal. M.M., 1951. Batı Toroslarda Alanya ard ülkesinde jeolojik araştırmalar, MTA publ., Se- and Ergun Akay for fruitful suggestions during rie D. No. 5. 134 p., Ankara. this study, Dr. Margit Bohn-Havas for provi- Brunn, J.H.; Dumont, J.F.; Graciansky, P. Ch. De; ding study in Hungary Natural History Muse- Gutnic, M.; Juteau, Th.; Marcoux. J.; Monod. um and Hungary Geology Institute, Dr. Ortwin O. and Poisson, A., 1971, Outline of the Ge- Schultz for using opportiunities in Austrian ology of the Western Taurids, Geology and Natural History Museum and, to Dr. Alfred History of Turkey, Petroleum Exploration Soci- Dulai tor using his special collection in Hun- ety of Libya, Tripoli. gary Natural History Museum and Dr. Ercu- , Argynadis, l; Marcoux, J.: Poisson, A. and ment Sirel (A.U.M.F.), Aynur Hakyemez Ricou. I.E., 1973, Antalya ofiyolit naplarmin (MTA), Sedef Babayiğit (MTA), Hatice Kara- orijin lehine ve aleyhine kanıtlar. Proceedings of 50 th annual of Republic of T.C. kullukçu (MTA), Emin Erkan (MTA) ve Dr. Mehmet Duru (MTA) for paleontological Cox, R.; Newell, N.D.; Boy, D.W.; Branson, C.C.; Ca- sey, R.; Chavan, A.; Coogan, A.M.; Dechase- determination. aux, C.; Fleming, C.A.; Haas, F.; Hertlein. Manuscript received November 15. 2001 L.G.; Kauffman, E.G.; McAlester, A.L.; Moore, R.C.; Nuttall, C.P.; Perkins, B.F.; Smith, L.A.; Soot-Ryen, T.: Stenzel, H.B.: Trueman, E.R.: REFERENCES Turner, R.D. and Wein, J,, 1969. Treatise on Akay. E. and Uysal. S., 1984, Orta Torosların batısın- Invertebrate Paleontology, Part N, vol. 1-2. daki (Antalya) Neojen çökellerinin stratigrafisi. Mollusca 6, Bivalvia, (Ed R.C. Moore) The Ge- sedimantolojisi ve yapısal jeolojisi. MTA Rep. ol. Soc. of America. Inc. and the University of No 7799 (unpublished). Kansas. THE MOLLUSCAN FAUNA AND STRATIGRAPHY OF ANTALYA MIOCENE 57

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