Sülfür Throughout Geological Time in Balkan Peninsula**

Mineral Res. Expl. Bul.. 123-124. 1-12, 2002

SÜLFÜR THROUGHOUT GEOLOGİCAL TIME IN BALKAN PENINSULA**

Radule POPOVİC*

ABSTRACT.- During investigations for a long time it has been remarked that the oldest metallogenic epochs in Balkan Peninsula include a limited number of, occurrences with sülfür as one of the chief chemical elements. Thus it could be said that in these epochs the deposits with sulphur compounds either have not been formed or in some cases there were only rare showings. So, for instance with the Grenvilian epoch, according to date knowledge, only one occurrence in Pelagonids (Nezilovo) could be associated. In the Baikalian metallogenic epoch, characterized by formation of greenschists in western Macedonian only traces of sulfide mineralizations, then one deposit of lead, zinc and copper sulfides, as well as one pyrite impregnation in the larger Popcevo - Dojran area (eastern Macedonia), exhibiting sülfür content less than 0,11% are present. In contrast to Pelagonian-Rhodopean massif, in the Green complex (Vlasina) of eastern Serbia numerous deposits and occurrences of pyrite and lead, zinc and copper sulfides are present, indicating a more remarkable sülfür yield in this district during Baikalian metallogenic epoch. Thanks to this fact it could be estimated this epoch to be much more enriched in sülfür in Balkan Peninsula, compared with the Grenvilian epoch. In the next epochs (Caledonian and Hercynian) the sülfür yield had become more and more intensive. This is especially related to the phytlitic volcanogenic-sedimentary origin formation of western Macedonian. in which fifteen deposits and occurrences of lead. zinc, copper and molybdenum sulfides have been registered, indicating numerous richer and poorer, certainly irregular pyrite impregnations. Compared with all previous epochs, the Alpine (early and late) time is characterized by great number of deposits of lead, zinc, copper, iron, arsenic, mercury sulfides and other metals, then by sulphates in sedimentary complexes, thus geochemically very sharply differing Alpine time from all previous epochs. On the basis of these facts, one could ascertain that the Cretaceous-Tertiary period could geochemically be characterized as the Sulphur Epoch. Judging by all these facts this is only the feature of Balkan Peninsula, but is probably of Global importance (phenomena).

Key words: Sülfür, epoch, sulfates, green complex, phyllitic formation, Cretaceous - Tertiary, intrusive-volcanogenic complex, Balkan Peninsula.

İNTRODUCTİON arsenic and other metals, as well as sulphate deposits. This appearance has induced certa- During geological investigations lasting in curiosity, resulting in some attempts this several years in the territories of Macedonian, phenomenon to be deciphered. In that sense Serbia, Bosnia-and-Herzegoniva, Montenegro some investigations were undertaken, but and Turkey, as well as the visits to other regi- these couldn't be studious and more universal ons in Balkan Peninsula, it was noticed that because of limited financial support and other sulfide deposits are very rare in the oldest for- circumstances. In that way, ideas presented mations of these regions, and going throughout in this paper are based upon incomplete evi- time they are more and more freguent so that dences, although sufficient, according to our in the Cretaceous and Tertiary time there. opinion, the problem to be opened and some occur numerous smaller or larger suifide de- distinct observations to be presented. posits of iron, copper, lead, zinc, antimony,

Geoinstitute, Rovinjska 12, 11000 Belgrade, Yugoslavia ** The paper has been realised under the Project 07M04 funded by Ministry of Science of Serbia. *** Translated from Serbian by Antonije Antonovic 2 Radule POPOVlC

SHORT REVIEW OF GEOLOGİCAL EVO- crust and initially it was a part of Bohemian or LUTİON OF BALKAN PENINSULA Middle European massif (Popovic, 1988), be- In aim the phenomenon of geochemical ing formed 700 million or more years ago (Ba- evolution of sülfür to be perceived in the best logh et al., 1994), and the other, Green or Vla- way, it is necessary to present in brief some sina complex respectively, according to all its newer comprehensions on geotectonical evo- features is restricted to the ocean type of the earth crust. This part had originated in the lution and some magmatic events related to certain geochemical processes. area Paleoasiatic ocean (as named by Zo- nensain et. al., 1976), nearly in the same time According to knowledges to date the ol- as the Gneiss complex. The Vrvi Kobila struc- dest formations in the Balkans occur in the ture, şeparating these two complexes, as far eastern part of the Pelagonian-Rhodopean as concerned all facts represents a rudiment massif or in Rhodopeans, including highly of a Collision structure, one part of it being ori- metamorphosed rocks constituting the geo- ginated between Paleoasiatic ocean and tectonical block, which is confined, according Middle European continent. to all features, to continental type of the earth crust. Numerous characteristics of Pelagonian- By separation of Mediterranean subcon- Rhodopean massif have indicated that its ori- tinent from the Gondwana, and Morava mas- gin and evolution during longer span of geolo- sif from the Middle European continent (Popo- gic time cannot coincide with formation and vic, 1998), and their motion in later times, they evolution of the Morava massif* and other were included into the contemporaneous geotectonical mosaic of Balkan Peninsula. crystalline complexes in Balkan Peninsula. Just during the younger Paleozoic and in Such a dynamic evolution of geotectoni- Mesozoic time the Pelagonian-Rhodopean cal blocks of the Balkans, as well as geotec- block entered along with other geotectonical tonic processes, which have been developed blocks, a part of the unique assemblages of during the younger Paleozoic, Mesozoic and Balkan Peninsula. Cenozoic (including the modern time as well) or after creation of the contemporaneous Bal- According to available data the Pelagoni- kan Peninsula respectively, have been ac- an-Rhodopean massif originated 2.5 billion companied by corresponding magmatism, years ago, being in that time a part of the which played an impressive role in geoche- Gondwana supercontinent. From the other si- mistry of individual elements in the same de, it is considered (Popovic, 1991, 1995, area, one of these being sulphur. 1998) that the Morava massif (crystalline complexes in the Juzna Morava and Velika GEOCHEMİCAL EVOLUTİON OF SÜLFÜR Morava valleys) is composed of two complex- IN BALKAN PENINSULA es formed in various geotectonical settings. It is under discussion, accordingly, the Gneiss Taking into consideration the indepen- complex and the Green-or Vlasina complex dent pre-Mesozoic evolution of individual respectively. The Gneiss complex exhibits geotectonical settings of their origin, being properties of continental type of the earth specific for each of individual blocks in a

The Serbo-Macedonian mass is divided into Pelagonian-Rhodopean and Morava massifs (Popovic. 1991) SULFUR THROUGHOUT GEOLOGICAL TIME IN BALKAN PENINSULA 3

corresponding way, one of the features, besi- In the next, Baikalian epoch the green de other individualities, is the sülfür as a che- schists had been formed, whose protoliths are mical element, exhibiting his own geochemi- confined to the rocks originated in the area of cal and metallogenic evolution. In the same oceanic type of the earth crust. Formations of time this is a common feature of all unified this complex occur in the Pelagonian-Rhodo- geotectonical blocks in frames of Balkan pean and Morava massifs, then in western Peninsula during Mesozoic and especially Serbia, Zagrebacka Gora and elsewhere. Cenozoic time. In greenschists of western Macedonia, These Studies are based first of all on re- as a part of Pelagonian-Rhodopean massif, latively limited and non-systematic investigati- trending form Sar Planina, across Kicevo, De- ons of sülfür contents, in conditions of defici- mir Hisar and Pelister, Continuing further to ency of detailed Studies on distribution of this Greece, some low order, until recently not in- element throughout metallogenic epochs in vestigated sulfide mineralization have been Balkan Peninsula, concerning the Proterozoic registered. In contrast to them, in the district complexes of Pelagonian-Rhodopean massif occurring between Strumica and Dorjan in (Macedonia), then Drina, Ivanjica and Jadar eastern Macedonia occur much larger con- metamorphics (western Serbia), area of southern Serbia, the Vlasina or Green complex of centrations of iron, lead, zinc and copper sul- eastern Serbia. These facts are supported by fides. This has particularly been manifested presence of numerous sulfide and sulfate de- by the lead-zinc deposits near Dojran, with in- posits originated during Mesozoic and Ceno- dicated ore reserves of about 25 million tons zoic epochs, in which the sülfür percentage averaging 3.8% lead-and-zinc and 0.1% cop- varies mostly from 1 % to 20%. per. The chief minerals in this deposit are pyrite, galena, sphalerite, chalcopyrite, arse- In the oldest petrogenetic complexes in nopyrite, marcasite, enargite, pyrrhotite and Balkan Peninsula (Pelagonian-Rhodopean others. Although the lead-zinc and copper massif) are not known some more important contents are low, it is stili to be ascertained, occurrences of sulfides and other sülfür com- according to frequency of all sulfides, inclu- pounds, thus the pre-Grenvilian epochs could ding the pyrite impregnations in concentrati- be considered as depleted in this element. ons of 0.3% covering a large area of greensc- Just in the Grenvilian epoch in Pelagonides hists, that in the mean sülfür content in these (Nezilovo at Mt. Babuna) some smaller sulfide occurrences are preserit, which could be as- schists is higher than the mean value in basic sumed as the first traces of increased sülfür magmatic rocks (0.03% after Vinograd ov, concentrations in the area of Balkan Peninsu- 1962). The investigations in the district betwe- la. The Origin of this sülfür cannot be discus- en Strumica and Dojran (Popovic, 1993) exhi- sed since these investigations have not been . bited the sülfür content (according to 100 completed, and from the other side the occur- analyzed samples) in greenschist from rence itself had several times undergone the 0.042% to 0.11%, evidently speaking about hydrothermal, tectonical and all other geologi- sülfür increase from about 1.5 to 4 times (ave- cal transformations, which affected this part of raging about 2 times) compared with basic Pelagonides throughout the geological time. magmatic rocks. 4 Radule POPOVİC

In contrast to Pelgonian-Rhodopean accompanied by chalcopyrite. sphalerite, ga- massif, where in greenschists took place rela- lena and others. The most important sulfide tively limited concentrations of sülfür compo- occurrences and deposits appear near Golu- unds in the same rocks of the Vlasina comp- bac, at Veliki Bubanj and Mali Bubanj nearby lex or the Morava massif respectively, which Petrovac na Mlavi, then occurrences near extends from Carpathians in Romania. Conti- Aleksinac and at Bukovik and Rozanj, in the nuing across eastern and SE Serbia, to NE iarger area of the Crna Trava and Blagodat Macedonia and further throughout Bulgaria. (Ljubata) district, near Trgoviste etc. (Fig. 1). The sulfide mineralizations are widespread in Considering the length and width of the gre- the whole area. They were formed during Ba- enschist zone with sulfide impregnations and ikalian tectono-magmatic cycle in the area of higher concentrations in form of deposits, and oceanic type of the earth crust. These are according to investigations to date (drilling), most commonly poor or rich sulfide impregnati- extending more than 200 m depth, the sülfür ons as well as smaller or iarger suifide ore mean content in greenschist could be estima- deposits in which the pyrite is predominant, ted at about 0.08%, which is about 3 times SULFUR THROUGHOUT GEOLOGİCAL TIME IN BALKAN PENINSULA 5

higher than the average (clarke) content in na river region, Polimlje, SE Bosnia, eastern basic magmatic rocks after Vinogradov Serbia ete.), but essentially not changing the (1962). Taking this information into considera- impression on the sülfür content in general. tion, including also the mentioned sulfide de- The Alpine (early and later) time has be- posits only in the area of eastern Serbia, it co- en defined, after Haq and Eysinga (1987), as uld be concluded that this tract of land is very early, middle and Late one, including the who- promising for discovery of lead, zinc, copper le Mesozoic and Cenozoic era. When consi- and most probably gold deposits, the last dered the distribution of intrusive-volcanic ones otherwise coinciding with the Green complex accompanied by sulfide ore deposits complex of this region. and occurrences, in such cases in the Bal- The Caledonian and Hercynian metallo- kans have existed vast areas occupied by genic epochs in Macedonia or in Pelagonian- these complexes (Fig. 2). In addition of wi- Rhodopean massif respectively are characte- despread anhydrite and gypsum sedimentary rized by relatively higher sulfide concentrati- deposits in Dinarids and in other areas of the ons, most commonly represented by pyrite, Balkans it could be comprised that during the galena, sphalerite, chalcopyrite, molybdenite, Mesozoic and Cenozoic took place remarkab- and lesser arsenopyrite, pyrrhotite, marcasite, le sülfür enrichment. Considering only sulfide antimonite and others, bearing in mind that ore deposits one could say that 90% of Pb, higher concentrations could be consıdered as Zn, Cu, Mo etc. deposits in Balkan Peninsula ore deposits and occurrences. In western Ma- originated in that period. In lack of other in- cedonia following occurrences and deposits vestigations (on sülfür contents and distributi- of sulfide mineralizations are known: molyb- on) this is the most important criterion for denurn - Strelci (near Kicevo) and Vrutok (ne- estimation of the sulfur yield throughout ar Gostivar), copper, zinc and iron at Beriko- Mesozoic and Cenozoic time in the Balkan vo, copper at Padaliste, lead and zinc near Peninsula. If compared with older epochs an Kolari, copper near Judovo, lead and zinc at evident difference is remarkable, not only in Openica, as well as numerous pyrite concent- freguency of deposits, but in the total reser- rations in the Phyllite compiex of volcanic-se- ves of Pb, Zn, Cu and other sulfides as well. dimentary Origin. On the basis of distribution If the pyrite impregnations in rocks are added, and local sampling, it could be estimated that locally being the genuine pyrite ore deposits the average sülfür content varies in the pyhlli- with reserves of several million tons, conside- tic formation complex from 0.014% to 0.37% ring gypsum and anhydrite in Sediments, rela- (according to only 50 analyses of rocks of this tively simple and real estimations are achi- formation), thus evidentfy indicating the incre- evable, but it should be noticed that during Al- ased content of this element, denoting that pine time the sülfür yield was not Uniform. Na- both Caledonian and Hercynian epochs are mely, in the Mesozoic the largest sülfür con- markedly enriched in sülfür, compared with centrations are related to anhydrite and gyp- previous epochs. especially in amount of sul- sum, lesser to sulfide deposite. From the ot- fide deposits and occurrences (about 15). Si- her side. at the end of Mesozoic and Cenozo- milar features as in mentioned two epochs ic epochs extremely great number of the Fe. are in other parts of Balkan Peninsula. aitho- Pb, Zn, Cu and other metals took place. Ta- ugh in some districts the sulfide concentrati- king into account the roughly calculated ore ons in the Phyllitoid complex are lower than in reserves of all sulfides in the area of the for- western Macedonia (as for instance in the Dri- mer SFR Yugoslavia, quantities are greater 6 Radule POPOVlC

than 2 billion tons. The calculated sulfur gra- Some of these volcanoes have extruded, for de has exhibited more than 5%, from that extample, 50 tons of sülfür per year or more, amount minimum 0.5% sulfur is restricted to and the others extruded during a single day disseminations in dacite-andesitic rocks, thus 100 tons of sulfur or more, as emanations. indicating the huge sülfür quantities. Similar The best illustration for it is the Mount St. He- situation is in the other Balkan areas, particu- lena volcano, which emitted from June, 6-22, larly in Rumania and Bulgaria. However, it 1980 between 950 and 1300 tons SO2, inclu- should not be neglected that during these ti- ding periodical 15 minutes paroxysms emit- me s the active subaerial volcanoes had emit- ting 40 tons SO2 or recalculated at 3800 tons ted also great amounts of sulfur, as it could be SO2 per 24 hours (Lipman, Donald, 1980). compared with contemporaneous volcanoes.

All the presented data are in favour of higher, compared with the mean (clarke) valu- the fact that in the intrusive-volcanic complex es in similar or same magmatic rocks (Vinog- of Balkan Peninsula during Alpine epoch in- radov, 1962), and 10-15 times higher in rela- tensive enrichment in sulfur took place. Ac- tion to the older metallogenic epochs. These cording to roughly estimated sulfur amounts are features distinguishing the Mesozoic-Ce- in rocks (complexes) it has averaged about nozoic time as an extraordinary geochemical 1 %. Such a content of this element is 30 times appearance. SULFUR THROUGHOUT GEOLOGİCAL TIME IN BALKAN PENINSULA 7

ORİGİN OF SULFUR IN THE BALKAN Balkans has indirectly suggested the assump- PENINSULA DURING THE ALPİNE TIME tion that this process resulted from subducti- If compared number of sulfide ore depo- on of the ophiolitic belt and Inner Dinarids be- sits and disseminated sulfides of iron, copper, low the continent (in this case these are the lead, zinc, arsenic, and others, as well as va- Morava and Pelagonian-Rhodopean massifs rious sulfates originated in sedimentary or Serbo-Macedonian mass, after Grubic complexes in the Balkans during Mesozoic (1974b), Jankovic and Petkovic (1974). Such an unilateral explanation is hard to be accep- and Cenozoic periods with the same or similar complexes of Paleozoic or older time, ted if considered only one segment (Inner Di- enormous differences are evident. This is par- narids and ophiolites of the Vardar zone), be- ticularly characteristically for the period of the cause a simple explanation is that the tract of latest Mesozoic and Tertiary or better to say subduction is not remarkable compared with the whole Cenozoic time. In that way the Up- the span of time of its activity. per Cretaceous, Paleogene, Neogene, and In fact, the numerous sulfur emanations Quaternary times should be defined as the and pyritizations (Vranje Spa, Sijarina Spa Sülfür Epoch in the Balkan Peninsula. But this etc.) speak that ophiolites and Inner Dinarids, phenomenon has opened numerous prob- sometimes being active segments of subduc- ems, among them the most important being tion of the earth crust, ended this activity, but origin of sülfür. This is not all an Uniform and that the sülfür yield has continued. This fact is unilateral problem, especially bearing in mind of primordial importance for these tracts. If to limited amounts of direct geochemical and these considerations is added the fact that other informations and that this phenomenon sülfür in the area Carpatho-Balcanids is also was not to date in focus of corresponding abundant, but not being related to the same Studies. geological processes of tectono-magrnatic If this complicated problem would be activation, an-other problem has been opened: of what kind and which mechanisms we- open to be solved, especially in frames of ac- re producing sulfur in that area; And then ap- tual knowledge, it is necessary to start from Alpine geotectonical events in Balkan Penin- pears a common problem of the total sulfur yi- sula. In that regard the most important prob- eld. This problem or huge guantity of the sül- lem to be analyzed is the so called Tertiary für introduced during Alpine time is not restric- tectonomagmatic activation. The authors of ted only to Balkan Peninsula but has continu- this concept (Grubic, 1974b; Jankovic and ed from one side to the Aegea, Asia Minör Petrovic, 1974), although being seriously oc- and further to the east and, and from the other cupied by problem of geotectonical events side, across the Carpathians to middle Euro- and related metallogenic manifestations cha- pe as well. racterising the mentioned activation, have not The conception of the authors for the been occupied neither by the problem of sul-- Tertiary tectono-magmatic activation uncle- fur origin nor by its enormous yield and depo- arly has defined the causes and direct factors sition in the intrusive-volcanic complexes of of the tectono-magmatic activation. Only Ka- that period. However, the concept of origin-of. ramata (1983), Grubic (1974) and partly large intrusive-volcanic complexes in the pro- Auboin, Blanchet (1981) have been more cess of tectonic-magmatic activation in the concrete in that sense, especially Karamata 8 Radule POPOVlC

(Fig. 3), who has analyzed, throughout geoc- the Pelagonian-Rhodopean massive or the hemical features, the direct relation of ophioli- Serbo-Macedonian mass respectively, and in tic complexes with Tertiary dacite-andesitic frames of the Drina-lvanjica block and Vardar volcanites in the tract of Tertiary tectono-mag- zone or the ophiolitic zone respectively. This matic activation. Namely, he has observed, model is acceptable if it would be taken into from one side, the Inner Dinarids including so consideration that subduction of the menti- called Drina-lvanjica block and ophiolites of oned blocks is a conseguence of another sub- the Vardar zone, being subducted as a who- duction, much more widespread, being stili le, and from the other side, the Outer Dina- active in the present days. Thsi is subduction rids, which also had parallel entered into the of the Mediterranean bottom or African conti- process, leading to distinct magmatic proces- nent respectively, which also contains high ses, being reflected to the earth surface: eit- sulfates concentrations, beneath the Europe, her at the border of Morava massif or inside i.e. Balkan Peninsula in our case.

In such circumstances one could suppo- The subducting evidently commenced se that formerly deposited sulfur (in form of with ophiolites of the Vardar zone and meta- gypsum and anhydrite) in Dinarids could be morphites of Inner Dinarids below the Morava the chief source of sulfur that area. So called massif (in the southern part of the Balkans, tectonomagmatic activation is not autochto- beneath the eastern segment of the Pelagoni- nous in this case, but had resulted from a an-Rhodopeans or Rhodopean massive in complex spacious and longtherm process ha- this case), accompanied by another subducti- ving lasted from jurassic time (Auboin, Blanc- on related to the western ophiolitic zone and het, 1981, Fig. 4). Outer Dinarids beneath Inner Dinarids (as SULFUR THROUGHOUT GEOLOGICAL TIME IN BALKAN PENINSULA 9

reported by Karamata, 1983), and further in geodynamic processes of such complexity, the district of Hellenic trench initiated by and retaining only at so called Tertiary tecto- subduction of the Tethyan ocean bottom or no-magmatic activation or at the magmatism remains of the oceanic crust and African introducing large sulfur amounts into Balkan continent beneath the Europe or Balkan Peninsula, that the zone of Tertiary intrusive- Peninsula in such a case (Underhill, 1989). All volcanic complex stretches across the Bal- these very intricated processes had initiated a kans in the northwest-southeast direction, vigorous magmatism, partly reflected as so cutting all older structures and the Vardar called Tertiary tectono-magmatic activation zone as well, as formerly reported by numero- (Grubic, 1974b; Jankovic and Petkovic, 1974), us authors. This zone strikes in length of se- accompanied by corresponding geochemical veral hundred kilometres and probably across masifestations. One could say, neglecting ot- the Aegean sea continues to Asia Minor, thus her phenomena, which otherwise follow all measuring more than 2000 km in total length.

Differing from the zone of tectono-mag- occur extremely spacious intrusive-volcanic matic activation, in Rumania, eastern Serbia complexes, with high concentrations of (iron, and Bulgaria the Carpatho-Balkanids are pre- copper, lead, zinc etc.) sulfides, lesser sulfa- sent, also characterized by abundant intruzi- tes. This region evidently has similar, not only ve-volcanic complexes with the outstanding petrogenic but also geochemical characteris- sülfür enrichment. We don't enter now in tics of sulfur, as the trans-Balkan intrusive- their origin since various opinions have exis- volcanic complexes (the zone of Tertiary tected. Some authors such as Grubic (1974a) tono-magmatic activation). have proceeded from rifting, the others, Bog- For geochemical Studies of the sülfür ex- danov (1977) for instance, have taken into ac- cess during the Cretaceous-Tertiary period, a count the subdictioh of Moesian plate bellow partial assistance may offer the tests of the the Balkans, the third ones - Vukasinovic, sülfür isotopic composition, as reported by Antonovic (1989) have considered impacts as Putnik (1981) in the zone of Diabase-Chert a cause etc. The fact is that in this belt also Formation in western Serbia, then by Alek- 10 Radule POPOVİC

sandrov (1992), Efremov (1993) and Serafi- which took place in the tract of formation of movski (1993) for districts of the Lece massif the magma melt and the yield of sülfür from and in deposits of NE Macedonia, as well as sedimentary rocks during subduction, introdu- former Studies by Drovenik et al. (1975) in sul- cjng it into the magmatic melt, show much fide deposits of N.E Serbia. Their interpretati- more complicated processes of the sülfür iso- ons of the sülfür isotopic composition are rat- tope fractionation. In that manner, sülfür from her Uniform, although with some reserves. the upper mantle, then from the subducted Certainly, numerous measurements of 34S ha- Sediments and from lovver parts of the earth ve varied around values linked to magmato- crust represent the reaj primitive sources of genic sulfur, which most of authors have rela- sülfür. All these processes have together con- ted to the upper mantle. However, when the ditioned the high heterogenity of the sülfür cited results presented by them are observed, isotopic composition in individual sulfide ore it is to be noticed that most of these could not deposits in Balkan Peninsula. This phenome- be connected with the mentioned concept. non has especially been focused by Drovenik et They actually have not an obvious explanati- al. (1974/75) in an attempt to find out a satis- on for the isotope values higher than +7 %0 factory solution considering the horizontal zo- and lesser than -7%0. So for example for the nality around the magmatic body, while other Markov Karnen in NE Serbia Drovenik et al. authors have mostly neglected this phenome- (1974/75) have cited the 34S values starting non. It is possible that Sediments in Dinarids from -20%o., which is evidently characterized or from another geotectonic block, then the for enrichment in the light sülfür isotope. Simi- bottom of Mediterranean sea, and African lar results have been obtained for the ore de- plate would not be the primary source at least posits of NE Macedonia as well. Such appe- of one part of sülfür in sulfide deposits and arances would be rather interpreted as a con- impregnations occurring in the zone of tecto- sequence of various Origin of the primitive sül- no-magmatic activation? Wen the Carpatho- für. One could, namely, suppose that one part Balkan arc in question, it is hard to favour eit- of sülfür has originated from the upper mant- her the subduction process, although Bogda- le, but for the other part would be rather assu- nov (1977) postulated this way, or other pla- med to originate from the former Sediments netary geotectonical process, as reported by entering during subduction in the zone of Grubic (1974a) and Vukasinovic, Antonovic magma generation, as well as from lovver (1989). In all such cases the Sediments or parts of the continental crust, affected by par- continental crust in this district respectively tial melting. Such a 34S fractionation from the occur as primordial source of one part of sül- melt created in the mentioned manner depen- für, entering into composition of sulfide depo- ded on physical-chemical conditions, pH va- sits in Carpatho-Balkanids. lue, transport length, thermodynamical and If duration of the subduction process, other terms. then the phase of magmatic melt, introduction it has been considered that such factors of sülfür into Cretaceous-Tertiary intrusive- would improve the fractionation of heavy iso- volcanic complexes, and certainly continuati- topes, but in the case of light isotopes the on of its yield till the present days would be ta- ımproving would be partial. But results repor- ken into consideration, it is evident that this is ted by the mentioned authors could not be included in a relatively longterm process, ha- simplified as they did. Intricated processes, ving lasted for about 140 million years. SULFUR THROUGHOUT GEOLOGİCAL TIME IN BALKAN PENINSULA 11

If this period would be better focused one Mediterranean. Faculty of Mining and should get to the judgement that this geoche- Geology, Belgrade. UNESCO Correlation, mical feature of the Balkan Peninsula is not of Project no 3, Ed S. Jankovic, pp 493-504. Belgrade. a local importance. Contrary, it could be said that in guestion is a global phenomenon, Decker, E. R.: Wright, L. T. and Stauffer, H. R., 1987. which in the best way reflects distribution of Volcanism in Hawaii. US Geological Survey the Cretaceous-Tertiary sulfide deposits aro- Professional Paper 135, v 1. p 8391. Was- und the Pacific, in Mediterranean regions and hington. ın districts with contemporaneous active vol- Drovenik, M.; Lekovsek, H. and Pezidc. J., 1974-75. canoes. This is related to the so called cir- Izotopski sastav sumpora u rudnim lezistima cumpacific fire belt, then to the middle- sout- Timocke eruptivne oblasti. Rudarsko-meta- hern and SW Pacific, middle America, Medi- lurski zbornik, knj 4, str 320-62. Ljubljana. terranean, southern and SE Asia, Malaya arc- Efremov, I, 1993, Osnovne geohemijske magmatske hipelago, middle oceanic rifts (in Atlantic, Indi- i metalogenetske karakteristike u Kratovskoz- an ocean etc.). All together it has led to an letovskoj oblasti. Doktorsk disertajica. Rudars- unigue conclusion that the Cretaceous-Terti- ko-geoloski fakultet, daktilografisano, str 282, ary period could be announced as the Epoch Stip. of Sülfür from the geochemical point of view, Grubic, A., 1974a, Istocna Srbija u svetlosti nove glo- not only for Balkan Peninsula but in larger balne tektonike i odras takvog modela na tu- sense as well, representing a global geoche- macejne tektonike severne grane Alpida. Me- mical epoch. talogenija i koncepcija geotektonskog razvoja Jugoslavije. Posveceno Prof Dr. B. Milovano- Manuscript received April 4, 2001 vic'u. Rudarsko-geoloski fakultet, Katedra za Ekonomsku Geologiju, str 153-80. Beograd.

. 1974b, Srpska-Makedonska mineragenetska REFERENCES provincija u svetlosti neoalpske aktivizacije. Aleksandrov. M, 1992, Metalogenetske karakteristike Metalogenija i koncepcija geotektonskog raz- polimetalicnog rudnog polja Sase-lstocna Ma- voja Jugoslavije. Posveceno Prof. Dr. B. Mila- kedonija. Rudarsko-geol. Doktorska clisertaci- vanovicu. Rudarsko-geoloski fakultet, Katedra ja. Rudarsko-geoloski fakultet daktılografisa- za Ekonomsku Geologiju. str 261-63. Beograd. no, str 264. Beograd. Haq U. Bilal and Van B. Eysinga, V. F., 1987, Geolo- Auboin. J. and Blanchet. R., 1981, Subduction and gical Time Table. Elsevier, Amsterdam, Net- tectonics: Discussion on the results of the herland. IPOD Programme in active margins. Oceano- Jankovic, S. and Petkovic, M., 1974, Metalogenija i logica Acta. Collogium C 3. Geology of Conti- koncepcija geotektonskog razvoja Jugoslavi- nental Margins, 25th IGC, pp 283-94. Paris je. Posvec'eno Prof. Dr B. Milovanovicu. Ru- Balogh. Kad.; Svingor. E and Cevtkovic. V.. 1994. darsko-geoloski fakultet, Katedra za Eko- Ages and intensities of metamorphic proces- nomsku Geologiju, str 369-98. Beograd. ses in the Batocina area, Serbo-Macedonian Karamata. S., 1983, Sadrzaji nekih mikroelemenata u Massif. Acta Mineralogica-Petrographica. tercijarnim magmatitima istocnog dela Jugos- Szeged, XXXV, pp 81-94. Segedin. lovije u zavisnosti od njihovog geotektonskog Bogdanov. B., 1977. Metallogeny of Sredna Gora Zo- polo/aja. Glas CCCXXXV SANU. Odelenje ne in the context of plate tectonics. Metallo- prirodno-matematickih nauka. knj 49, str 39- geny and plate tectonics in the northeastern 54. Beograd. 12 Radule POPOVİC

Lipman, W. P. and Mullineaux. R. R.. 1981, The 1980 Putnik, S., 1981, Metalogenija bakra dijabaz-roznac- Eruptions of Mount St. Helens. Geological ke formacije. Posebna izdanja Geoinstituta, Survey Professional Paper 1250, str 844. knj 6. str 117. Beograd. Washington Serafimovski, T., 1993, Strükturno-metalogenetski Popovic, R., 1991, Şrpsko-Makedonska masa ili Pe- karakteristiki na zonata Lece-Halkidiki Tipovi lagonsko-Rodopski i Moravski Masiv. Radovi na naogalista i reonizacija. Rudosko-geoloski Geoinstituta, knj 25, str 7-20. Beograd. fakultet, Posebno izdanie br 2, str 328. Stip.

. 1993, Geochemical and Metallogenic Evoluti- Underhill, R. J., 1989, Late Cenozoic Deformation of on of Ore Mineralizations of Southern Part of Hellenids Foreland, western Greece. Bulletin Balkan Peninsula in Pre-Alpine Age. Proce- of the Geological Survey of America, v 101, no edings of the 29th IGC. Resource Geology 5, pp 613-34. Boulder, Colorado, USA, Special Issue, no 15, pp 331-41. Tokyo, Ja- Vinogradov. A. P., 1962, Srednee soderzanie hi- pan. miceşkih elementov v glavnih tipah izverzenih . 1995, Geohemijska i rnetalogenetska evoluci- gornih porod Zemnoy kori. Geohimiya, no 7. ja moravskog masiva u premezojskom vreme- str 555-71. Moskova. nu. Radovi Geoinstituta, knj 31, str 267-84. Vukasinovic, S. and Antonovic, A., 1989. The Funda- Beograd. mental Magmatogenic-Minerogenic Structu- th . 1998, Palinspasticka rekonstrukcija geotek- res in Yugoslavia. 28 IGC, Abstracts, v 3 of tonskih dogdjaja mediteranskog podrucja kroz 3, str. 3-312-3-313. Washington DC, USA. geolosko vreme. Radovi Geoinstituta, knj 35, Zonensain, L. P.; Kuzmin, l. M. and Moralev, M. V., str 91-98. Beograd. 1976, Globalnaya tektonika, magmatizm i metalogeniya. Izd. "Nedra", str 231. Moskva. Mineral Res. Expl. Bul. 123-124, 13-19, 2002

GEOLOGY AND ORİGİN OF THE PYROPHYLLITE - DEPOSİTS IN THE PÜTÜRGE MASSIF (MALATYA - EASTERN TURKEY)

Ali UYGUN* and Enis SOLAKOĞLU*

ABSTRACT.- The pyrophyllite deposits of Pütürge massif (Malatya - Eastern Turkey) have been increasingly used in last years for white cement Production because of their low iron and chromium content. Around 25 pyrophyllite occurrences are explored along a nearly 15 km's long belt south of Pütürge, where 10 guarries are opened. The co-existence of high-AI pyrophyllite and kyanite indicate that the pyrophyllites were formed during a retrograde greenschist metamorphic phase, which the massif had experienced. Five different types of pyrophyllite are identified; pyrophyllite with high Al content. pyrophyllite with sericite, pyrophyllite with high silica modüle, pyrophyllite with low silica modüle and pyrophyllite with low alkaline content respectively. In this study, mineralogical and geochemical properties of these pyrophyllites are described.

Key Words: Pyrophyllite, Pütürge massif, mineralogy, genesis, geochemistry.

İNTRODUCTİON According to the US Geological Survey statistics (Harben, 1999), undifferentiated The first Identification of pyrophyllite world talc and pyrophyllite Production is about (AI O .4SiO2.H O) in Turkey rests up to be- 2 3 2 2.2 Mt's per year, China's Production exclu- ginning of 1970's. As it resembles talc, ded. Turkey is one of the 10 pyrophyllite pro- pyrophyllites were mined for a while as talc in ducing countries and is at the fifth rank after limited amounts. In 1976, pyrophyllite was Japan, South Korea, Brazil and India. In Far mentioned in the Turkish Mining Law. Up to East, rocks with mixed composition of 1990's the annual Production was around 2- pyrophyllite, sericite, kaolinite and quartz are 3000 typ (tones per year) and used in refrac- termed as "roseki". However, in Brazil, the tory industry. Starting with this date it has be- blend of pyrophyllite, sericite, diasporite, kya- come an important row material since ÇİMSA nite and quartz is termed as "agalmatolite". In Cement industry Comp., has started to use South Africa, the mixture of pyrophyllite, chlo- pyrophyllite instead of kaolin in white cement ritoid, rutile and epidote is termed as "won- Production. Recently, it has been consumed derstone" (Harben, 1999). in the rate of 100-120.000 tpy. In this study, the authors present their By using the Pütürge pyrophyllite with its own data and observations on the genesis, low iron and chromium content, the whiteness properties and geological setting of pyrophyl- of the cement produced by ÇİMSA has reac- lite occurences, gained during their study within hed to 90, termed as "Süper white". Today, it last 10 years in Malatya - Pütürge region. takes place within the best guality cements in Evaluations are based on a Series of Europe. By the capacity of 1 Mt per year, the geochemical and mineralogical investigations factory of ÇİMSA-Mersin has reached to the in the laboratories, besides the photogeology, position of world's largest white cement pro- geological mapping and drilling with coring or ducer. by reverse circulation. 14 Ali UYGUN and Enis SOLAKOĞLU

GEOLOGY AND DISTRIBUTION OF southern arm following the Keşen hill, Köse- PÜTÜRGE PYROPHYLLITES mustafa hill, Hopan ridge, Cünütü hill. The Within the first investigations in the regi- northern one follows the line of Kütüreş hill, on, Danış (1978) mentioned that the pyrophyl- Güreş hill, west of Tümbelek hill and east of " Şiro stream. The position of the pyrophyllite lite-bearing schists were located between qu- occurrences and main fault systems around artz-sericite-schists and tourmaline-schists. Pütürge are presented in figüre 1. The quarri- Cornish (1983) reported the presence of 3 es opened on these occurrences within last types of pyrophyllites, which were formed as 10 years are as follows: a result of hydrothermal alteration of dacitic tuffs. Presence of pyrophyllite in Pütürge 1-) Karataş hill - İmrün quarry massif was reported by in Yazgan (1984) and 2-) Keşen hill in the explanations of the Malatya İ-27 sheet of 1/100.000 scaled geological map Series of 3-) Ümik hill Turkey (MTA, 1986) as "the pyrophyllite, kya- 4-) Aytez hill nite. diaspore assemblage is tormed within 5-) 1407 m. hill the shear-zones in tourmaline-rich orthogne- ısses. According to Erdem and Bingöl (1977), 6-) West Vaktık hill pyrophyllite developed along a main shear- 7-) East Vaktık hill zone between the Lovver and Upper units of Pütürge massif. 8-) Kösemustafa hill The Pütürge massif, composed of augen 9-) Güreş hill gneisses, amphibolite - prasnite, mica schists 10-) Mukul hill with pelitic origin, orthogneisses and marbles, radiometric ages of 70 - 85 Ma (MTA, 1986) Pyrophyllite occurrences are of lensoidal were obtained from the metamorphic rocks. from with different sizes. At the bottom of the Widespread amphibolites and augen gneis- lenses, 2-mica orthogneisses or schists are ses forming the core of the massif outcrop in usually observed. Schists with muscovites or the area between Babik stream and Tepehan sericites are observed as wall rocks. Ouartzi- at the southern of the massif (Fig. 1). At the tes observed together with pyrophyllites are southern part of Pütürge where pyrophyllites mostly quartz-dykes. No stratigraphic relati- are frequently observed, orthogenesises and onship between these quartzites and rare to- mica schists dominate, however meta-carbo- urmaline-schists with pyrophyllite could be nates take place mostly at the northern part of encountered. Pütürge (MTA, 1986). Although the pyrophyllite occurrences in The pyrophyllite occurrences ın Pütürge Vaktık hill and Keşen hill are related to shear massif are aligned along a 10 km long belt, zones, there are also pyrophyllite occurren- trending about N 60° W starting from around ces without any relationship with tectonic zo- Karataş hill at 6 Km's SE of Pütürge at the nes (e.g. Ümik hill and Sınık hill). This situati- eastern tip through south of Yıldırım hill, Ke- on relates pyrophyllite-formation with retrog- şan hill, north of Babik, Ümik hill, Şahantaşı rade metarmorphism rather than to a structu- hill, Sınık hill, Aytez hill, and Vaktık hill. To the ral control, as it will be explained in the next west of Vaktık hill the belt is branched, with a chapter. GEOLOGY AND ORIGIN OF THE PYROPHYLLITE IN THE PÜTÜRGE MASSIF 15 16 Ali UYGUN and Enis SOLAKOĞLU

Length of the pyrophyllite lenses reach XRD studies. The electron microprobe analy- up to 600m in Vaktık hill, and 400m's in Keşen ses have shown that the kyanites contain 60 - hill and widths of the lenses range between 62 % AI2O3 (Uygun, 1995). Our suggestion 20 - 50 m's. Depths are around 20 - 30 m's that pyrophyllites were formed by retrograde maximum. The maximum thickness of metamorphism is evidenced by the replace- pyrophyllites cut in bore-holes is 39 m's in ment of the kyanite porphyroblasts by Ümik hill section. pyrophyllite observed on the microphotograph MINERALOGY AND GEOCHEMISTRY OF (Fig. 2). PYROPHYLLITE OCCURRENCES Pyrophyllite occurences are usually divided in to two groups (Carnish, 1983). In the pyrophyllite occurrences in Pütür- ge, pyrophyllite and quartz are main observed a- By loss of alkalies and iron of acidic minerals. Kyanite, muscovite, sericite, illite, volcanic rocks by the effect of hydrothermal kaolinite, dickite and alunite are the accom- fluids along the fault zones. The main examp- panying minerals at some places. Pyrophylli- les to this first group are the pyrophyllites de- te is mainly gray or greenish gray or greenish rived from porphyries and liparites in Japan, white in color and oily and dull in appearance. from quartz porphyry and trachyandesite in Its association with fine-grained quartz gives South Korea, from rhyolitic volcanics in North a resistant appearence to the rock. Carolina in USA, and from rhyolitic pyroclas- tics in Australia. Theoretically the AI2O3 content in pure

pyrophyllite, is about 28.3%. AI2O3 contents b- Podiform pyrophyllites of metamorp- around 30.52% from trenches of western Vak- hic origin where metamorphosed volcanic tuff tık hill, are found out to be due to the presen- and ashes are associated with schists, as tho- ce o kyanite determined by microscope and se in Brazil. GEOLOGY AND ORIGIN OF THE PYROPHYLLITE IN THE PÜTÜRGE MASSIF 17

Especially, the presence of kyanite to- Muscovite and sericite as other acces- gether with pyrophyllites is critical for the me- sory minerals observed form more prominent tamorphic origin of Pütürge pyrophyllites. The zones in different outcrops. For example, presence of two successive metamorphic marginal zones with muscovite (Keşen hill qu- phases in Pütürge massif, one in prograding arry), and with sericite have developed (Ümik amphibolite facies and the other one in retrog- hill and 1407m. hill). In these areas, they also rading green schist facies were reported by include illite as determined by XRD studies. Yazgan (1984) and MTA (1986). So, it is in- Kaolinite and dickite are comparably rare terpreted that kyanite was developed from and they are most probably mineralisations tuffs with high Al content or kaolinites in gra- developed along hyrothermally activity zones nites or their volcanic equivalents in the prog- or in secondary shear zones. This kind of ressive stage and replaced by pyrophyllites in kaolinite alterations with small dimensions are the retrograde stage. observed within very young shear systems Bucher and Frey (1994) reported that associated with the east Anatolian Fault kaolinite in the temperatures above 300°C and passing through Şiro stream at 10 Km's west kyanite+quartz at temperatures of 400°C and of Puturge.

<4 Kbar Pwater reacts to form pyrophyllites. As- Main characteristics of the Pütürge sociation of quartz either with pyrophyllites or pyrophyllites is the whiteness of their firing co- with kyanite, and even presence of silicarich lour due to their iron content below % 0.2 in rocks together with pyrophyllites implies that average. Moreover, for the importance of whi- transformations in this stage were below te cement production, chromium with values 400°C. less then 100 ppm, and Mn with less 10 ppm are far below the critical limits. Measured SO On the other hand, the distribution of 3 values, which are secondary in origin, reach pyrophyllite occurrences in the massif indica- to maximum % 4.8 in alunitisations observed te that their formation can not be simply exp- in east Vaktık hill and Sınık hill quarries. TiO lained by their association with shear zones, 2 present in average of % 0.5 ratio in pyrophyl- but supports our suggestion for retrograde lites is related with minerals like rutile of sphe- metamorphism. Besides, pyrophyllites do not ne. show any oriented fabrics nor foliation, which could have been the case if formed in a she- 5 types of ores have been identified ar zone. Moreover, their distribution in the (Table 1) in Pütürge massif according to XRD, massif also seem not, to be restricted to the microscopy and XRF analysis in based on contact between the lower and upper units as samples obtained from field work, drilling and proposed by Erdem and Bingöl (1997). production: 18 Ali UYGUN and Enis SOLAKOĞLU

A) High Al-Pyrophyllites.- Al2O3 content are ores that can be directly used in white ce- in this type are above 28%. They are rich in ment production. kyanite. AI O content in these ores in west 2 3 D) Pyrophyllites with sericites.- Vaktık hill and in Ümik hill reaches up to 38% Pyrophyllites with sericite including some al- at some samples. Here 40% of the rock is ma-

kalies (in average 2 - 4% K2O) are observed de up of kyanite. AI2O3 contents even reac- hing up to 40.1% are found in core samples of in Keşen hill quarry, Ümik hill and in 1407 m. Aytez hill. hill. They have schistose appearance and include primary feldspars.

B) Low silica Pyrophyllites.- AI2O3 content of this type changes between 20 - 35%. E) Low alkali Pyrophyllites.- This type of The silica module reaches to about 2.5 - 3. In ores observed in eastern Vaktık hill can be these pyrophyllites, cut in limited amounts in differentiated from high silica pyrophyllites the borings of Ümik hill, Şahantaşı hill, and with their very low alkaline content (max. 1407 m. hill, kyanite is nearly not recorded. 0.5%).

C) High silica Pyrophyilites.- These The melting point of pyrophyllite, which is types are pyrophyllites are originally with qu- actually a refractory mineral, is given as 1200°C. In mixtures such as "algaimatolite" artz and have AI2O3 with values ranging between 15 - 18%. In these types of ores obser- and "wonderstone", it is given as 1530°C and ved in some places such as Karataş hill-imrün even as 1630°C. However, easy participation quarry, Keşen hill and 1407 m. hill, silica mo- of Puturge pyrophyllites in reactions, in kiln dule (SM) is observed to be around 4-5. They temperatures are reasoned by presence of GEOLOGY AND ORIGIN OF THE PYROPHYLLITE IN THE PÜTÜRGE MASSIF 19

either low temperature quartz or fluxes such The 5 different groups of Pütürge as F and B. The F content of pyrophyllites pyrophyllites with their outstanding mineralo- used for fiberglass production is found to be gical and geochemical properties, if elabora- around 1500 ppm, which might be controlled ted in to economically more valuable products by coexisting apatite. in ceramics, refractory, fiberglass, fillings, paper, and plastic industry will have high impor- Abundance of boron in pyrophyllites as- tance for economy of the country in the futu- sociated with granitic gneisses depends on re. presence of tourmaline and even dumortierite

(AI7 [O3/BO3/(SiO4)3]). This paragenesis is ob- Manuscript received May 21, 2001 served in misroscopic investigations (Cemal Göncüoğlu. personal communications) of some Pütürge samples. Especially, in the Hollan REFERENCES dere occurrences, pyrophyllites with tourmaline are observed. Bucher, K. and Frey.. M., 1994, Petrogenesis of Me- tamorphic Rocks. Berlin, pp. 318. CONCLUSIONS Cornish. B.E., 1983, Pyrophyllite. In: Industrial Mine- Around 25 pyrophyllite occurrences have rals and Rocks, V. 2, AIME, New York. been detected in a 15 km long, E-W trending Danış, M., 1978, Malatya-Pütürge-Babik çevresinde- belt in the Pütürge massif. The massif was ki pirofillit zuhurlan, MTA Rap. 6477 (Unpub- subjected to two successive phases of meta- lished). morphism; an earlier progressive one within the amphibolite facies and a retrogressive Erdem, E. and Bingöl, A.F., 1997, Pütürge (Malatya) one in green schist facies, respectively. Mine- Masifi'ndeki gnayslarm petrografik ve petrolo- jik özellikleri. Selçuk Üniv. Müh. Mim. Fak. 20. ralogical and geochemical data indicate that Yıl Jeol. Semp. Bild. 217-227. originally high-alumina tuffs, clays or kaolinites gave way in the first phase to the formati- Harben. P.W.. 1999, The Industrial Minerals Hand- on of kyanite and in retrograde conditions, book. 3. Edit. London, pp. 296. kyanite - pyrophyllite transformations were re- MTA, 1986. 1 /100.000 Ölçekli Türkiye Jeoloji Haritası alized. Serisi. Malatya I-27 paftası. Ankara.

The Pütürge pyrophyllites are incre- Uygun, A.. 1995. Çimsa-Malatya-Pütürge AR-59827 asingiy used in white cement production be- ve ÖlR-4002 nolu ruhsat sahaları Jeolojik cause of their low iron and chromium content. etüdü: Geosan Rap. 786, (Unpublished). Due to these properties it is used for the pro- Yazgan, E., 1984, Geodynamic evolution of the Eas- duction of the best quality European white ce- tern Taurus region. In: Tekeli, O. and Gön- ment in ÇİMSA-Mersin, termed as "Super cüoğlu. M.C., (Eds) Geol. of the Taurus Belt White" that has "whiteness" around 90. Proc. 199-208, MTA, Ankara. Mineral Res. Expl. Bul.. 123-124. 21-26. 2002

A PELAGIC PALAEOCENE SEOUENCE IN THE BİGA PENINSULA NORTHWEST TURKEY

M. Burak YIKILMAZ*, Aral l. OKAY1* and İzver ÖZKAR**

ABSTRACT.- A sequence of pelagic limestone, calciturbidite, debris flow, greywacke, basalt and limestone blocks. up to several hundred metres across, occur west of the town of Biga in northwest Turkey. The pelagic limestones in this seguence, named as the Ballıkaya formation, comprise pelagic foraminifera of Palaeocene age. Neritic limestone of Mid-Eocene age lies unconformably over the Ballıkaya formation. The age and the sedimentary environment of the Ballıkaya formation indicate the presence of a tectonically active deep sea environment in northwest Turkey during the Palaeocene, and constrain the main Alpide deformation in northwest Turkey to the Late Palaeocene - Early Eocene interval.

İNTRODUCTİON The Sakarya zone consists of Late Triassic Late Cretaceous and Palaeocene are subduction-accretion units, collectively na- critical tectonic periods in Anatolia. Subducti- med as the Karakaya complex, unconfor- on, ophiolite obduction, regional metamorp- mably overlain by a Jurassic-Cretaceous se- hism and Aipide deformation occurred or star- dimentary sequence. Rocks of the Karakaya ted during this time span. Upper Cretaceous- complex crop out widely in the eastern part of Palaeocene stratigraphy has, therefore, a the Biga peninsula (Bingöl et al., 1975; Okay special importance in Turkey. However, et al., 1991). These rocks are unconformably Upper Cretaceous-Palaeocene outcrops ha- overlain by the Liassic Bayırköy formation and ve not been described over a very large regi- the Middle-Upper Jurassic Bilecek limestone. on extending from Bursa westwards to the Cretaceous rocks generally do not crop out in Aegean Sea, and information of the palaeo- the Biga peninsula and farther east, probably geographic and tectonic evolution of north- due to erosional removal during the Tertiary. west Turkey during the Late Cretaceous and In the Biga peninsula the Jurassic Bileck li- Palaeocene is very limited. In this context the mestone is unconformably overlain by the Up- discovery of a Palaeocene seguence in the per Oligocene-Miocene Volcanic and volcano- Biga peninsula in the immediate vicinity of the clastic rocks. An exception to this situation is town of Biga is of special importance for the observed west of Balya, where a sequence of tectonics of northwest Turkey. This paper Bilecik limestone, 800 m thick, is overlain un- describes the Palaeocene sequence in Biga conformably by thinly to medium bedded pe- and discusses its significance for the tecto- lagic shaley limestones. The pelagic limesto- nics of western Anatolia. nes are only 30 m thick, and are in turn unconformably overlain by the Neogene Volca- GEOLOGİCAL SETTING nic rocks. They contain the foraminifera Bone- The eastern part of the peninsula be- tocardiella conoidea, characteristic for the Al- longs to the Sakarya zone of the Pondides. bian to Cenomanian period (Okay et al,

* istanbul Teknik Üniversitesi, Avrasya Yer Bilimleri Enstitüsü, Ayazağa 80626, istanbul. ** istanbul Üniversitesi, Mühendislik Fakültesi, Jeoloji Mühendisliği Bölümü, Avcılar, İstanbul. 1 Corresponding author. 22 M. Burak YIKILMAZ; Aral l. OKAY and Izver ÖZKAR

1991). Similar pink pelagic limestone seguen- limestone blocks have been described in the- ces with Hedbergella sp. form small outcrops se ophiolitic melanges, which mark the wes- west of Gönen, around the margins of the tern boundary of the Sakarya zone (Brink- Hamdibey-Kalkım Neogene basin and north mann et al., 1977; Okay et al., 1991). of Balya. In these regions the stratigraphic po- The Palaeocene seguence described in sition of these Cretaceous limestones is not this paper occurs immediately west of the clear. Upper Cretaceous ophiolitic melanges town of Biga and forms an outcrop, two kilo- crop out in the centre of the Biga peninsula along a zone extending from Küçükkuyu to metres wide, surrounded by the Neogene vol- Karabiga (Fig. 1). Upper Cretaceous pelagic canic rocks and Eocene sandstones. A PELAGIC PALAEOCENE SEOUENCE IN THE BlGA PENINSULA 23

GEOLOGY OF THE WEST BİGA REGİON res across. Lithologically these limestone In the area studied, southwest of the blocks resemble the Jurassic Bilecik limesto- town of Biga, the Palaeocene Ballıkaya for- ne, which outcrops around Balya and Gönen. mation is the lowest exposed unit (Fig. 2). It is The limestone blocks in the Ballıkaya formati- overlain unconformably by the Eocene limes- on constitute the hills west of Biga. The mat- tone, sandstone and shale. The Palaeocene rix to the blocks, which crops out in the val- and Eocene seguence is cut by a Neogene leys, consists of pelagic limestone, calciturbi- microgranodiorite and is overlain unconfor- dite, debris and grain flows, greywacke and mably by the Neogene acidic tuffs. basalt. In the previous Studies, the matrix was not recognized and the region was ascribed to the Bilecik limestone (Okay et al., 1991). Pelagic limestones and the intercalated calciturbidites are best observed on the Ballı- kaya hill west of Biga. Similar outcrops of pelagic limestone also occur southwest of the village of Havdan (Fig. 3). The pelagic limestones are red, violet, thinly to medium bedded micrites with radiolaria and foraminifera (Pla- te 1 - fig. 2). The micrites are intercalated with pink, red and white calciturbidites and calcirudites. The limestone clasts in the calciturbidites and calcirudites are poorly sorted (0.5-25 cm) and medium to poorly rounded (Plate 1 - fig. 1). Red, brown debris flows with a volcanogenic matrix are observed on the Ahlatlı hill southwest of Biga. The debris flows comprise poorly sorted (1-75 cm) limestone and Ballıkaya formation mudstone clasts and are intercalated with, grey, laminated mudstones and silstones. The Ballıkaya formation, first described Greyish green greywacke and spilitic basalt in this study, consists of pelagic limestone, forms rare outcrops in the Ballıkaya formation calciturbidite, debris an grain flows, greywac- east of Havdan. ke and basalt and large number of neritic limestone blocks of various sizes. The name of The Ballıkaya formation is dated through the abundant pelagic foraminifera in the red the formation comes from the Ballıkaya hill, pelagic limestones. Three samples of micritic 500 m west of the town of Biga, where the limestone around the Ballıkaya hill (sample best and most representative outcrops are lo- numbers 146A, B, 163A) contain radiolaria cated (Fig. 3). The geographic coordinates of and the foilowing foraminifera characteristic the type section are north 40°13'25" and east for the Early Palaeocene (Danian) Morozovel- 27° 14'15". la pseudobulloides (Plummer), M. uncinata Most of the Ballıkaya formation consists (Bolli), M. cf. trinidadensis (Bolli), Morozovella of grey, pale grey, thickly bedded to massive sp., Planorotalites compressa (Plummer), limestone blocks up to several hundred met- Planorotalites sp., Globigerina triloculinoides 24 M. Burak YIKILMAZ; Aral l. OKAY and İzver ÖZKAR

Plummer, Globigerina sp., Racemiquembeli- other regions Eocene sandstones and shales na sp., Bolivina sp. (Plate 1 - fig. 3). Another lie directly over the Ballıkaya formation witho- specimen of micrite from the same region ut the intervening Soğucak limestone (Fig. 3). (number 160) contains Morozovella velasco- West of Biga the Soğucak limestone has a ensis (Bolli), Planorotalites sp. and Radiolaria thickness of about ten meters and is overlain indicative for the Late Palaeocene (Thaneti- by the sandstones and shales of the Ceylan an) (Plate 1 - figs. 4 and 5). Another micrite formation. The contact between the Soğucak sample collected from southwest of the villa- limestone and the Ceylan formation could not ge of Havdan (sample number 93) contains be observed in the field. Planorotalites compresssa (Plummer), Plano- The Soğucak limestone west of Biga rotalites sp., P. Morozovella sp., Globoconusa contains abundant nummulites and other Globotruncanita stuarti sp., cf. (d'Lapparent), benthic foraminifera. Samples of the Soğucak Globotruncanita Abathomphalus sp., sp. (Pla- limestone from this region contain Nummuli- te 1 - fig. 6). These foraminifera indicate latest tes beaumonti d'Archiac and Haime, Nummu- Maastrichtian and earliest Palaeocene. The lites spp., Discocyclina sp., Asterocyclina sp., Globotruncana forms in the sample are pro- Operculina sp., Quinqeuloculina sp., Rotali- bably reworked from the Upper Cretaceous li- idae, Rupertidae, Anomalina sp., and indicate mestones. The foraminifera in the pelagic li- a Middle Eocene (Lutetian) for the Soğucak limestones indicate a Palaeocene age (Dani- mestone. an-Thanetian) for the Ballıkaya formation. Ceylan formation The presence of large number of limestone blocks in the Ballıkaya formation, as well Eocene sandstone, siltstone, mudstone as the scarcity of bedding, make the estimati- and microconglomerate form a belt around on of its thickness difficult. However, a mini- the Ballıkaya formation west of Biga (Fig. 3). mum thickness of two hundred metres can be This Clastic sedimentary unit has been named estimated for the Ballıkaya formation. In the as the Ceylan formation following the stratig- area of study the base of the Ballıkaya forma- raphic nomenclature in the Thrace basin and tion is not observed, it is overlain unconfor- the Biga peninsula (Siyako et al., 1989). The mably by the Soğucak limestone of Middle dominant lithology of the Ceylan formation in Eocene age. the area of study is medium bedded, fine- grained yollowish brown sandstones. Locally Soğucak limestone siltstone, mudstone and microconglomerate beds are intercalated with the sandstones. The neritic limestones, that lie unconfor- Outcrops of the Ceylan sandstones are very mably over the Ballıkaya formation, are called rare in the area studied. In Thrace, the Ceylan Soğucak limestone following the stratigraphic formation is known to consist of siliciclastic nomenclature in the Thrace basin and in the turbidites. Biga peninsula. (Siyako et al., 1989). The So- ğucak limestone is made up of yellowish, No fossils have been found in the Ceylan thickly bedded to massive reefal limestones formation in the area studied. However, its with abundant nummulites, corals and algae. stratigraphic position above the Lutetian So- In the study are the Soğucak limestone is only ğucak Limestone, as well as palaeontological observed on the Ballıkaya hill west of Biga data from other parts of the Biga peninsula (Fig. 3). In this locality limestones with abun- (Siyako et al., 1989) indicate a Mid-to Late dant nummulites lie unconformably over the Eocene age for the Ceylan formation west of limestone blocks of the Ballıkaya formation. In Biga. A PELAGIC PALAEOCENE SEQUENCE IN THE BlGA PENINSULA 25 26 M. Burak YIKILMAZ: Aral I. OKAY and İzver ÖZKAR

Neogene rocks in northwestern Turkey during this period. This deep marine environment could be rela- A small microgranodiorite cuts the Ballı- ted to the Intra-Pontide ocean. The Alpide de- kava and Ceylan formations in the southwest. The microgranodiorite consists mainly ot qu- formation and uplift in trtis region, probably related to the closure of the Intra-Pontide oce- artz and plagioclase with minor amounts of bi- oiite and amphibole. Extensive zoning in the an, in constrained in northwest Turkey to the late Palaeocene-Early Eocene. plagioclase crystals in microgranodiorite indicates a shallow intrusion. ACKNOWLEDGEMENTS On the main road between Biga and We thank Sefer Örçen for the palaeonto- Çan, white acitic tuffs lie unconformably over logical determination of the nummulites in the the Ceylan formation. The microgranodiorite Eocene limestones. and the acidic tuff are products of the extensi- Manuscript received May 22, 2001 ve late Oligocene-Early Miocene calc-alkaline magmatism in northwest Turkey.

DISCUSSIONS AND CONCLUSIONS REFERENCES A Palaeocene sequence of pelagic li- Bingöl, E.: Akyürek, B. and Korkmazer, B., 1975, Bi- mestone, calciturbidite, debris and grain ga yarımadasının jeolojisi ve Karakaya For- flows, greywacke, basalt and large number of masyonunun bazı özellikleri. Cumhuriyetin 50. limestone blocks crops out west of the town of Yılı Yerbilimleri Kong. Tebliğleri, MTA Enstitü- Biga. This sequence is unconformably overla- sü, 70-77. m by the Soğucak Limestone of Middle Eoce- Brinkmann. R.: Gümüş, H.; Plumhoff. F. and Salah. ne age. A.A.. 1977, Höhere Oberkreide in Nordwest- Anatolien und Thrakien. N. Jb. Geol. Paleont. Palaeocene outcrops in the northwes- Abh.. 154, 1-20. tern Turkey are scarce. Upper Cretaceous- Okay, A.l.and Tansel, L, 1994, New data on the Palaeocene limestones have been described upper age of the Intra-Pontide ocean from form the northern margin of the Gelibolu pe- north of Şarköy (Thrace). MTA Bull, 114, 23- ninsula under the name of Lört formation 26. (Önal, 1986). Blocks of Upper Cretaceous ; Siyako, M. and Burkan, K.A., 1991, Geology (Maastrichtian) and Lower to mid-Palaeocene and tectonic evolution of the Biga Peninsula. (Danian and Montian) pelagic limestone, to- Special Issue on Tectonics (ed. J.F. Dewey), gether with blocks of serpentinite, metadiaba- Bulletin of the Technical University of İstanbul, se, reefal Upper Eocene limestone blocks ha- 44. 191-255. ve been described as olistoliths in an Upper Önal, M., 1986, Gelibolu yarımadası orta bölümünün Eocene Clastic seguence north of Şarköy sedimanter fasiyeleri ve tektonik evrimi, KB (Okay and Tansel, 1994). The Lört limestone Anadolu. Türkiye. Jeoloji Mühendisliği, 29, 37- could also be a large block in the Eocene se- 46. guence. Siyako, M.; Burkan, K.A. and Okay, A.l, 1989, Biga The Palaeocene rocks in Biga, Gelibolu ve Gelibolu yarımadalarının Tersiyer jeolojisi and Şarköy indicate the presence of a tectoni- ve hidrokarbon olanakları. Türkiye Petrol Je- cally active, deep sea to oceanic environment ologları Derneği Bült., 1, 183-199. PLATE PLATE-I Fig. 1- Field photograph of the calcirudites in the Palaeocene Ballıkaya formation, Ballıkaya hill, west of Biga. Fig. 2- Microphoto of a typical pelagic micrite in the Palaeocene Ballıkaya formation with radiolaria and foraminifera (Morozovella pseudobulloides (Plummer)), sample number 163A, the long edge of the photo is 2 mm, Fig. 3- Morozovella pseudobulloides (Plummer), sample 163A, Ballıkaya formation, Danian, long edge 0.41 mm. Fig. 4- Morozovella sp., sample 160, Ballıkaya formation, Palaeocene, long edge 0.82 mm. Fig. 5- Morozovella velascoensis (Bolli), sample 160, Ballıkaya formasyonu, Thanetian, long edge 0.41 mm. Fig. 6- Planorotalites compresssa (Plummer), sample 93 Ballıkaya formation, Danian; long edge 0.41 mm. M. Burak YIKILMAZ; I. ,OKAY ve İzver ÖZKAR PLATE- I 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 solution 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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Robertson, A.H.F.; Collins, A.; Flecker, R.; Glover, C.; Eğirdir-Yenişarbademli- Gebiz ve Geriş-Köp- Pickett, E.; Ustaömer, T. and Dixon, 1996, Ba- rülü (Isparta-Antalya) arasında kalan alanın ti Türkiye'nin Üst Paleozoyikten günümüze Jeolojisi, MTA-TPAO Rep. No 3132, 559 p. tektonik evrimi, Proceedings of 49 th Turkish (unpublished). Geol. Cong., Abstracts, 9-14. Şenel, M.; Gedik, I.; Dalkılıç, N.; Serdaroğlu, M.; Bil- Rögl, F., 1998, Paleogeographic considerations for gin, A.Z.; Uğuz, M.F.; Bölükbaşı, A.S.; Korucu, Mediterranean Tethys and Paratethys M. and Özgül, N., 1996, Isparta büklümü do- Seaways (Oligocene to Miocene), Ann. ğusunda otokton ve allokton birimlerin stratig- Naturhist. Mus. Wien, 99/A, 279-310. rafisi (Batı Toroslar), MTA Bull., 118, 111-160. Steininger, F.F. and Rögl, F., 1984, Paleogeography . and Bölükbaşı, A.S., 1997, 1100 000 ölçekli and palinspastic reconstruction of the Türkiye Jeoloji Haritaları, Fethiye M-9 Geolo- Neogene of Mediterranean Tethys and gical Dep., Ankara. Paratethys. In: Dixon, J.E. and Robertson, , Dalkılıç, H.; Gedik, I.; Serdaroğlu, M.: Metin, A.H.F. (editors): The Geological Evolution of S.: Esentürk, K.; Bölükbaşı, A.S. and Özgül, the Eastern Mediterranean Tethys, 659-668 (Blackwell) Oxford-London - Edinburgh. N., 1998, Orta Toroslarda Güzelsu koridoru ve kuzeyinin Jeolojisi, MTA Bull., 120, 171-198. Senel. M., 1997a. 1250 000 ölçekli Türkiye Jeoloji Haritaları. Fethiye paftası, No 2, MTA, Geolo- Tuzcu, S.; Karabıyıkoğlu, M. and İslamoğlu, Y., 1994, gical Dep., Ankara. Batı Toroslar Miyosen Mercan resifleri Bile- , 1997b. 1250 000 ölçekli Türkiye Jeoloji Hari- şimleri, fasiyes özellikleri ve ortamsal konum- taları. Antalya paftası, No 3. MTA Geological ları, Proceedings of 47 th Turkish Geol. Cong., Dep., Ankara. Abstracts, p. 16. , 1997c. 1250 000 ölçekli Türkiye Jeoloji Hari- Waldron, J.W.F. 1982, Antalya Karmaşığı kuzeydoğu taları, Isparta paftası, No 4, MTA Geological uzanımının Isparta bölgesindeki stratigrafisi Dep., Ankara. ve sedimenter evrimi MTA Bull., 97-98, 1-20. . Bilgin, A.Z.; Dalkılıç, H.; Gedik, I.; Serdaroğ- Woodcock, N.H. and Robertson, A.H.F., 1977, Impre- lu. M.: Uğuz, F. and Korucu. M., 1991, Eğirdir- cate thrust belt tectonics and sedimentation as Sütcüler- Yenişarbademli arası ve yakın dola- a guide to emplacement of part of the Antalya yının (Batı Toroslar) Jeolojisi. MTA Geological Complex, SW Turkey Int. sixth coll. on the Dep Rep. No 365 (unpublished). Geology of the Aegean region (Edt.) İzdar, E., , Dalkılıç, H.: Gedik, I.; Serdaroğlu, M.: Bölük- ve Nakoman, E., İzmir, Piri Reis Int. Cont. başı, S.; Metin, S.: Esentürk, K.; Bilgin, A.Z.; Series Publ., 2, 661-670. Uğuz, F.; Korucu, M. and Özgül, N., 1992, Mineral Res. Expl. Bul.. 123-124. 59-65. 2002

THE FORMATION OF FISSURE RIDGE TYPE LAMINATED TRAVERTINE-TUFA DEPOSITS MICROSCOPICAL CHARACTERISTICS AND DIAGENESIS, KIRŞEHİR CENTRAL ANATOLIA

Eşref ATABEY*

ABSTRACT.- At Kırşehir center, in Kuşdili and Kayabaşı, along NE-SW directed extensional fracture, there is a fissure ridge type-travertine-tufa deposits. Travertine-tufa ridge is appoximately 800 m in length and 10-30 m in width. The hot-water saturated with calcium bicarbonate and minerals are enhensed from fissures and have caused to deposit yellow orange, brown and cream colored travertine in the walls of fissures as well as along the both sides. On the walls of the fissure, parallel to the fissure, compact and hard, laminated and thin bedded travertine crusts were deposited. However, in the both sides of the ridge, consistent with the slopes, the bedded crusts being porous, spongy tufas were deposites as well. Milimeter and Centimeter sized microscopic structures, similar to shrubs, are commonly found in this hot water originated travertine-tufas. These are; 1-Dendritic structures and, 2-Crystal bunches. Dendritic structures own micritic aggregate, shrub bunch, reed bunch and small twig shapes. There are calcite crystallisations among the twigs. But the crystal bunches are knife-shaped, large crystals and fibrous ray crystal structures. Dendritic structures have developed in the laminated crust and microterrace pools, located on both slopes of the fissure. On the other hand, the crystal bunches are common on the parallel- laminated crusts deposited an developed chemically. Super crystals were developed on the prismatic crystals, that were also developed along c-axes of the fibrous crystals.

INTRODUCTION 1984; Pedley, 1990; Ford and Pedley, 1996; Pentecost, 1990; Evams, 1999; Chafetz and Travertines are calcium carbonate preci- Guidry, 1999; Guo and Riding, 1994, 1998). pitations developed from organic and inorga- In Türkiye, such a study like occurrence, age, nic processes in karstic, hydrothermal microorganism effects and depositional kine- springs, small rivers and swamps. They are tics of travertines have been concentrated on spongy, compact and indicate crystal structu- Pamukkale (Denizli) travertines (Pentecost et res in different colors. They are named as cal- al., 1997; Altunel and Hancock, 1993; Ekmek- citic tufa, calc tufa, sinter crust and plant tufa. çi et al., 1995; Altunel, 1996). Moreover, the However, there are characteristic features characteristics of within-travertine pisolites in which make differency between tufa and tra- Mut (İçel) and petrography of travertines in Sı- vertine. Pedley (1990) used to define the tufa cakçermik (Sivas) areas were conducted by as high porous, spongy, paper-leaved and Atabey (2002) and Tekin et al., (2000) res- woody texture cool-fresh water carbonate de- pectively. The tufa deposits are subdivided in- posits. In contrast, He defined the travertine to two classes, namely, autochthonous-and as extremely well-lithified, spari calcite textu- clastic-originated by Pedley (1990). Chafetz red, diagenetic old calcerous tufa deposit. and Folk (1984) distinguished five classes of The research works have been carried travertine accumulations. These are, 1-Lake out about the classification formational envi- deposits, 2-Mounds and cones, 3-Terraced ronment, origin and diagenesis of the traverti- mounds, 4-Fissure ridges, 5-Waterfall depo- ne and tufas (Julia, 1983; Chafetz and Folk, sits. 60 Eşref ATABEY

The fissure ridge-type travertine of this crystal bunches. The purpose of this study is classification is found in Kırşehir (Fig. 1 and to present the properties, formation and di- Plate-l, fig. 1). The formation of fissure ridge- agenesis of these structures and their role in type travertine has previously been investiga- the formation of travertihe-tufa deposition. In consistency with the purpose of study, systematic samples were collected from different parts of travertine-tufa mass, in the order from fissure ridge outward. These samples have been examined under Polarization Mic- roscope and Scanning Electron Microscope (SEM), including x-ray analysis. The drilling locations have been correlated to establish the relationship between spring water and travertine deposit. GENERAL GEOLOGY Fissure ridge-type travertine accumulated at intersection points of the northeast-southwest and eastwest trending faults in southern part of Kırşehir massif. The Kırşehir metamorphic rock units consisting of Paleozoic age marble and schists are exposed at north, east and southwest of Kırşehir (Fig. 3). At southwest of Kırşehir, the Late Cretaceous Ba- ranadağ granodiorite and Early Eocene conglomerate, sandstone and limestone of Baraklı formation are exposed (Kara, 1991) in the ted at Pamukkale (Altunel, 1996). In Kırşehir, at Kuşdili and Kaya- başı localities, fissure ridge-type travertine deposits formed along a N-S directed fracture (Fig. 2). For the purpose of hot water sup- ply, the drilling facilities by MTA have been carried out and the characteristics of the hot water were given (Özmutaf and Didik, 1992; Didik and Tekin, 1995). Based upon the microscopic characteristics of the samples taken from the travertines, it is observed that the structures are of two types, dendritic shape and THE FORMATION OF FISSURE RIDGE TYPE LAMINATED TRAVERTINE-TUFA 61

area to the west of Kılıçözü stream. These morphic unit as source rock are changed. At units are overlain by Late Miocene-Pliocene number 1, the travertine is 46 m and late Mi- Kızılırmak formation, composed of conglome- ocene-Pliocene unit is 175 m in thickness. rate, sandstone, mudstone and tuffite (Fig. 2 These thickness values are 28 m and 20 m at and 3) (Kara, 1991). The alluvium sediments number 6, 22 m and 26 m at number 7, 38 m are present along Kılıçözü stream. Travertine and 15 m at number 5, 18 m and 55 m at is Quaternary ?-Recent in age, overlying the number 4, 10 m and 118 m at 3, and 10 m and Kızılırmak formation and it is formed around 87 m at drilling number 8, respectively. Con- the fault located along Kılıçözü stream. As it is sequently, it is deduced that, a downthrown shown on the drillings facilitied by MTA (inturn block side is present between 1 and 6, and 4 1, 6, 7, 5, 4, 3 and 8 numbered drillings), the and 3, whereas at 6, 7, 5 and 4, the meta- thickness of travertine and late Miocene-Pli- morphic basement was uplifted. ocene unit, consequently depth to the meta- 62 Eşref ATABEY

CHARACTERISTICS OF TRAVERTINE-TU- ging from 3 mm to 3-4 cm and characterized FA DEPOSITS 6y dark color, mottled and micritic aggregate- shaped (Plate-ll, fig. 2), herbage-shaped (Pla- The ridge-type travertine-tufa deposits te-ll, fig. 3), asicular redd-shaped (Plate-ll, fig. are located in Kuşdili and Kayabaşı districts at 4), woody plant overgrowth on crust surface Kırşehir center along a northeast-southwest and small twig-shaped (Plate-ll, fig. 5). The trending fissure fracture. The ridge is approxi- dendrites similar to reed, feather shaped ones mately 800 m in length, 10-30 m in width and have been interpreted by Weijermers et al. 2-4 m in height. The travertine-tufa rocks due (1986) that were originated from Bryum cf. to the effect of mineral-saturated hot ground- (algae) in Spain travertines. In interareas of water are reddish, brown, yellow, blue, green, dendrites there is light-colored spari-calcite, in orange, beige, white and blackish in color other areas, they are yellow and brown-colo- (Plate-l, fig. 1). There is a fissure at the cen- red due to limonitization, iron and phosphate ter of travertine ridge and parallel to this fissu- content. In the dendrites of short herbage re, laminated, thin-bedded, hard and compact bunch, the micritic aggregate-shaped ones crystalline crusts are present (Plate-l, figs. 2, are in medium-coarse grained calcite crystall, 3). At both slopes of fissure microterrace po- whereas the woody, tree twig-shaped ones ols tufas are deposited. Within the tufas, ro- are overgrowth on laminated crust surface und, ellipsoidal and composite tube-shaped, and within bed calcite crystalls (Plate-ll, fig. calcite-filled gas cavities are present (Plate-ll, 6). Jones and Renaut (1995) is their study in fig. 1). Kenya, defined the dendrite structures as MICROSCOPICAL CHARACTERISTICS OF non-crystal asicular dendrites. DENDRITIC STRUCTURES AND CRYSTAL Crystal bunches BUNCHES Based on the samples collected from hot Crystal bunches are mostly found in water originated Kırşehir travertine-tufa depo- fissure-parallel laminated travertine crusts sits, there are shrub-like structures changing and in thin-bedded, laminated crusts at both from milimeter to centimeter in scale. These slopes of the ridge. The crystal bunches, are 1-Dendritic structures and 2-Crystal bunc- unlike the dendrites, similar to reed bunches hes. The widely occurrence of these dendritic are fan, ray-shaped and longer in length. The structures in hot water travertines has been reed bunch-like ones are in 5-8 cm in length assigned in studies by Chafetz and Folk and fan in shape (Plate-Ill, fig. 1). The area (1984), Chafetz and Guidry (1999) in Italy. As among twigs is spari-calcite. The ray, fibrous a result of x-ray analyses of samples, toget- crystal bunches (Plate-Ill, fig. 2) and fan- her with aragonite and calcite crystal structu- shaped crystal bunches are also present re, iodine, phosphate, iron, chlorine, borax (Plate-Ill, fig. 3). Jones and Renaut (1995) and sodium carbonate has been detected. defined the similar crystal bunches as scandulitic dentrites in Kenya. Dendritic structures FORMATION AND DIAGENESIS The dendritic structures are extensively developed within the yellow, brown, green, A close relationship is present between blue, reddish, beige colored, laminated and the thickness of basement marble mass and thin-bedded travertine crusts and microterra- thickness or depositional rate of travertine-tu- ce pools at both slopes of the ridge, and wit- fa. Based on the drilling data, the thickness of hin the porous, spongy tufa. They are chan- travertine and depth to the marble is different. THE FORMATION OF FISSURE RIDGE TYPE LAMINATED TRAVERTINE-TUFA 63

The bicarbonate-saturated hot-water origina- (Plate-IV, figs. 4, 5). This layered structure ted from massive and thick marble basement has formed as a result of neomorphism accor- rock has caused the thick travertine deposition. ding to Love and Chafetz (1988). The ne- The fissures-parallel hard and compact, omorphism takes place in such processes; laminated and thin-bedded travertine crusts first overgrowth of crystalls on dendrites, later have developed with the lower hydrostatic along their c-axes the overgrowing of these pressure and decreasing water content. In crystalls in the form of columnar crystalls contrast, the porous tufa has been deposited (Figs. 5, 6). There after, as it is seen from Pla- at higher hydrostatic pressure, much water te-IV, figs. 5 and 6, the bedded and inclusion- type crystal structures are formed at progres- content, turbulant and during sudden CO2 loss. Dentdritic structures have been formed sive stage of diagenesis. Jones and Kahle in microterrace pools at suitable environment. As it is seen from the scanning electron microscopic view, they are the calcitized algae filaments (Plate-IV, figs. 1, 2, 3). These filaments, formed from carbonate crystalls, are a green type of algae which are Schzotrix cf. and Bryum cf. (Nevbahar Atabey, personal communication). The algae survive by feeding with CO2 present in the calcium bicarbonate-rich hot groundwater. Later the calcite crystalls increased at periphery of algae filaments and carbonate deposition occurred. The filament has a tube at its center and kni- (1986, 1993), examined the crystal shrub fe-shaped calcite crystalls are formed at inner structures formed by the calcitization of algae and outer part of this tube. At a later diagene- filaments. Furthermore, they pointed out that; tic stage, this type formations are caused the the secondary twigs orthogonally cutting the development of dentritic and crystal bunch first asicular crystalls and the third-order twigs shape structures. After completion of each cutting the secondary asicular crystalls were calcium carbonate structure, suitable to the developed. Pentecost (1990) interpreted the second, third and there after laminated crust formation of hot water originated dendritic structures, the bedded shape dendritic and structures, as the overgrowth of preferred crystal bunch structure layers formed (Fig. 4) crystalls on sharpened top part of mounds of microstructures. The calcitized bunches are arranged in a pattern parallel to laminated crusts. When viewed under the microscope, on the early formed coarse crystalls, fibrous, small, ray crystalls, that also developed along c-axes of the fibrous crystalls (Fig. 6). The deposits precipitated from mineral-rich hot water at slope of travertine ridge are in different colors (Plate-IV, fig. 6). This is due to oxi- dation and evaporation processes. 64 Eşref ATABEY

these structures as microbial originated. Pentecost (1990) pointed out a cyanobacteria origin for the hot-water travertine shrubs in Wyoming. USA, also Chafetz and Folk (1984) agreed with the bacterial origin. Based on the x-ray analyses, phosphate, iodine, chlorine, borax and sodium carbonate in Kırşehir travertine-tufa deposits might have been developed from basement and surrounding rocks. The dominant tufa deposits formed at both slopes of travertine-tufa mass indicate high hydrostatic pressure, great groundwater

discharge and sudden CO2 loss. The bedded crusts within the fissure of the ridge, depict the low hydrostatic pressure, less groundwa-

ter dischange and slow loss of CO2. The lower content of water caused the slow rate of deposition and the complete depleted water with time made carbonate deposition within DISCUSSION AND CONCLUSION the fissure at the center of the travertine-tufa The Kırşehir travertine-tufa has been mass. deposited by the precipitation of calcium car- Manuscript received November 11, 2001 bonate developed due to mineral-rich and calcium bicarbonate-saturated hot groundwater, REFERENCES reached at ground surface and loss of its CO2 content. However, green algae species Altunel, E., 1996, Pamukkale travertenlerinin morfolo- Schrotrixsp., has played an active role during jik özellikleri, yaşları ve neotektonik önemleri: formation of Kırşehir travertine-tufa deposits. MTA Derg., 118, 47-64. Especially, the slow rate of decreasing and Hancock, 1993, Morphology features and amount of CO dissolved in microterrace tectonic setting of Quaternary travertines at 2 Pamukkale, western Turkey: Geology J., 28. pools has caused algae to use and deposite 335-346. the carbonates. This also has made suitable Atabey. E.. 2002, Traverten içi oolit ve pizolit oluşu- conditions for feeding green algae to form the mu. MTA Derg., (inpress). dendritic structures developed at both slopes Braithwaite, C. J. R., 1979, Crystal textures of recent of the ridge. Dendrites have relatively formed fluvial pisolites and laminated crystalline in horizontal areas and microterrace pools. crusts in Dyfed, South Wales: J. Sed. Petrol.. Guo and Riding (1992, 1998), in their studies, 49. 181-194. assigned the neccessity of low-slope surfaces Chafetz, H. S. and Folk. R. L. 1984. Travertines: De- for microorganism activity. The crystal bunches positional morphology and the bacterially have developed in fissure-parallel laminated constructed constituents: J. Sed. Petrol., 54. crusts and those at both slopes of the ridge. 289-316. The algae activity in Kırşehir travertine-tufa and Guidry, S. A., 1999, Bacterial shrubs, deposits led to the formation of dendrites. crystal shrubs, and ray-crystal shrubs: bacteri- Guo and Riding (1994), in their study about al vs. abiotic precipitation: Sedimentary Geol hot-water travertines in Italy, considered 126, 57-74. THE FORMATION OF FISSURE RIDGE TYPE LAMINATED TRAVERTINE-TUFA 65

Didik. S. and Tekin. A.. 1995. Kırşehir-Terme 8 sıcak- Julia, R., 1983, Travertines: Carbonate depositional su sondaji kuyu bitirme raporu. MTA Rap. no: environments (Ed. By P.A Scholle, D.G. Bebo- 9834, (unpublished). ut and C. H. Moore). Tulsa, Oklahoma: Am. Ekmekçi, M.; Şimşek, Ş.; Yeşertener, C.: Elkhatip, H. Ass. Petrol. Geol. Spec. Publ., 33, 64-72. and Dilsiz. C., 1995, Pamukkale sıcak suların Kara. H.. 1991, 1/100 000 ölçekli açınsama nitelikli traverten çökeltme özelliklerinin CO kaybı çö- 2 Türkiye jeoloji haritaları serisi, No: 47, Kırşehir kelme kinematiği ilişkileri açısından irdelen- G18 paftası: MTA publ., Ankara. mesi: Yer bilimleri. 17. 101-113. Love, K. M. and Chafetz. H. S.. 1988, Diagenesis of Evans. J. E.. 1999. Reconation and implications of laminated travertine crusts, Arbuckle Mounta- Eocene tufas and travertines in the Chadron ins, Oklahoma: J. Sed. Petrol., 58, 441-445. formation, White River Group, Badlands of South Dakota: Sedimentology, 46. 771-789. Özmutaf, M. and Didik, S., 1992, Kırşehir-Terme kap- Ford, T. D. and Pedley, H. M.. 1996, A review of tufa lıcası. Terme-4 ve 5 sıcak su sondaji kuyu bi- and travertine deposits of the world: Earth-Sci- tirme raporu: MTA Rap., no: 9330. (unpub- ence Reviews. 41, 117-175. lished). Guo. L. and Riding, R., 1992, Aragonite laminae in Pedley, H. M., 1990, Classification and environmen- hot water travertine crusts, Rapolano Terme. tal models of cool freshwater tufas: Sedimen- Italy: Sedimentology, 39, 1067-1079. tary Geol., 68, 143-154. and . 1994, Origin and diagenesis of Qu- Pentecost. A.. 1990. The formation of travertine aternary travertine shrub fabrics, Rapolano shrubs: Mammoth Hot Springs. Wyoming: Ge- Terme. central Italy: Sedimentology, 41. 499- ol. Mag.. 127, 159-168. 520. ; Bayarı, S. and Yeşertener, C., 1997, Photot- and , 1998, Hot-spring travertine facies ropik microorganisms of the Pamukkale tra- and sequences, Late Pleistocene. Rapoline vertine, Turkey; their distribution and influence Terme, Italy: Sedimentology, 45, 163-180. on travertine deposition: Geomicrobiology Jo- Jones, B. and Kahle, C. F., 1986, Dentritic calcite for- urnal, 14, 264-283. med by calcification of algal filaments in a va- Tekin, E.: Kayabalı, K. and Ayyıldız, T., 2000, Eviden- dose environment: J. Sed. Petrol.. 56, 217- ce of microbiologic activity in modern traverti- 227. nes: Sıcakgermik geothermal field, central and . 1993, Morphology, relationship, Turkey: Carbonates and Evaporites, 15, 19- and origin of fiber and dentrite calcite crystals: 27. J. Sed. Petrol., 63, 1018-1031. Weijermars, R.; Mulder-Blanken, C. W. and Weigers, and Renaut, R. W., 1995, Noncrystalographic calcite dentrites from hot-spring ''deposits at J., Growth rate observation from the moss-bu- Lake Bogoria. Kenya: J. Sed. Research. A65. ilt Checa travertine terrace, central Spain: Ge- 154-169. ol. Mag.. 123, 279-286. PLATES PLATE-I Fig. 1- View to the eastern flank of travertine-tufa mass. Kuşdili district.

Fig. 1-2- The ridge of travertine-tufa mass and central fissure (y), ridge slope (Y) and fissure-parallel laminated and thin-bedded travertine crust structures (Tk).

Fig. 4- The microterrace pools developed at travertine ridge slope EŞREF ATABEY PLATE -1 PLATE-II Fig. 1- The composite tube (Bt) and laminated crust (Lk) developed in tufa deposit formed at slope of travertine-tufa mass.

Fig. 2- Microscopic view of the mottled (B) and micritic aggregate (Ma) dendritic structures (6X).

Fig. 3- Microscopic view of the herbage-shaped dendritic structures (09) (6X).

Fig. 4- Microscopic view of the feather-shaped dendritic structures (6X)

Fig. 5- Small tree twig-shaped (aç) dendritic structures overgrown on laminated crust surface (6X)

Fig. 6- Microscopic view of small tree twig (Ad) and micritic aggregate (Ma) dendritic structures (6X)

PLATE-III Fig. 1- Microscopic view of the fan-shaped crystal bunch (6X)

Fig. 2- Microscopic view of the ray, fibrous crystal bunch (6X)

Şek. 3- Microscopic view of the fan-shaped, ray crystal bunch (6X)

PLATE-IV Figs. 1-2-3- SEM view of the calcitized algae filaments (Af).

Fig. 4- Prismatic crystalls (Pk) overgrown fibrous crystalls (K) that overgrown laminated crust (Lk)

Fig. 5- Microscopic view of the fibrous (L), prismatic (P) crystalls (6X)

Fig. 6- Different coloration developed due to • different mineral content in hot groundwater Eşref ATABEY PLATE - IV GEOCHEMICAL CHARACTERISTICS AND ORIGIN OF BARITE DEPOSITS BETWEEN ŞARKİKARAAĞAÇ (ISPARTA) AND HÜYÜK (KONYA)

Oya CENGİZ* and Mustafa KUŞÇU*

ABSTRACT.- Barite deposits in the region of Şarkikaraağaç and Hüyük which are generally located in the form of veins, lenses and layers along the contacts of these units and the schists showing an extensive distribution within the same formation found within recrystallized Çaltepe limestone and dolomite, Çavuştepe calcschists of the Cambrian-Devonian age Sultandede formation are epigenetic in character. According to the results of chemical analysis of barite mineralization in the region, the presence of trace elements such as Pb, Zn, Cu, Cd, Ni, Co, Ag, Sb are locally identified in low values within barites of the region. Especially, in some trace elements such as Pb, Zn, Cu, Cd, Ag and As show an increase towards from Hüyük region to Çarıksaraylar area. When the results of chemical analysis of barite samples evaluated statistically, the presence of high correlation between Ba-Pb, Ba-

Ag. Pb-Ag, and AI2O3-K2O element pairs and mediumgrade correlation between Ba-Sr, Pb-Cu, Zn-Cd, CaO-

Fe2O3, CaO-SiO2, SiO2-AI2O3, CO- MgO, Fe2O3-AI2O3, Fe2O3, Fe2O3-Na2O, MgO-K2O element pairs of barite ores have been determined. The deposition forms of the barites in the investigated area, paragenesis, wall rock alteration, the high amount of trace elements, high Ba/Sr ratio, SrO values over 1.5 %, 180°-360°C homogenisa- tion temperatures of the two-phase (liquid+gas) fluid inclusions, +30.15 %o and +13.9 %o 34S isotope ratio in galena and barites, and 434°C high formation temperature indicate a hydrothermal origin of barite deposits in the region. SEDIMENTOLOGY OF OYLAT CAVE SEDIMENTARY ROCKS İNEGÖL (BURSA)

Eşref ATABEY**; Lütfi NAZİK** and Koray TÖRK**

ABSTRACT.- Oylat cave is located at 17 km southeast of the İnegöl (Bursa) in the exit of Oylat River canyon. Oylat cave has been developed at the intersection of two fault zones striking along WNW-ESE and NE-SW directions in recrystalized limestone unit of Permian-Triassic age. Clastics and carbonate sediments are in the Oylat cave developet due to karstification. The cave, presenting multi-stage development character can be divided into three sections. In the third section karst breccias, siltstone and mudstone, in the second section the great rimstone pools and flowstones had grown. In the first division at the end of the cave huge rock fragments due to the collapsing of roof, karst breccia, stalactite, stalacmite, soda straws, flowstones and cave pearls (pisolites) had grown. Moreever, in this part, a sedimentary sequence formed by a alteration of conglomerate, sandstone, siltstone and mudstone crops out. The clastic sediments in the Oylat cave is deposited from the sediments carried by surficial water entering the cave system, and flowstones, rimstones, cave pearls have been formed by the dripping from the cave roof, whereas rimstones pools were formed by the steadly flowing intra cave river. POST STACK SEISMIC ATTRIBUTE ANALYSIS

Zafer ÖZER* and Turan KAYIRAN**

ABSTRACT.- Hydrocarbon accumulations sometimes have effects on seismic data which can be used to indicate suitable worthy accumulations of hydrocarbon areas. The most prominent of these effects in increase in amplitude. Hydrocarbon accumulations may produce sufficent changes in amplitude however changes in acoustic impedance can be caused by various reasons. To get more information possible from the seismic data, impedance comparison and examination of all the properties constitutes the basic idea of seismic attribute analysis. From the analysis of seismic data by the amplitude information which has a primordial importance and other factors to be taken into cosideration are called seicmic attributes which are used to get contribution to interpretation and to make detailed analysis. The most useful attributes are amplitude, phase, frequency, polarity and velocity. Depending on the problem to be solved, seismic attributes can be obtained from instantaneous analysis, lateral continuity relationship and large variety of seismic data. In this work, several post stack seismic attributes is defined and how they can be used to get opportunities for interpretation is examined. After the application of migration, seismic attribute analysis is applied to two dimensional seismic data in Trakya region and provide the opportunity for comparison between seismic subsurface characteristics. With the comparison of conventional sections by the information of seismic attributes, it is observed that attributes can be used to enhance the interpretation.