Türkiye Jeoloji Bülteni
Türkiye Jeoloji Bülteni

Türkiye Jeoloji Bülteni

1976 AĞUSTOS Cilt 19 Sayı 2
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Description of The New Species Eoannularia Conica N.Sp. and New Observations on The Upper Lutetian - Lower Priabonian Limestone in The Darende - Gürün (West of Malatya) Region
Ercüment Sirel
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Abstract: Thin bedded limestones covering large areas in the west of Darende and in the southwest of Gürün (westof Malatya) are found to be Lower Priabonian in age. A new species of foraminifera, Eoannularia conica n.sp. occurringin these limestones is described.

  • foraminifera

  • Eoannularia conica n.sp.

  • limestone

  • Malatya

  • Akkuş, M.F., 1970, Darende-Balaban havzasındaki (Malatya ESE Anadolu) litostratigrafik birimler ve jipsli formasyonların ya§ı hakkında yeni bilgiler: M.T.A. Dergisi, Ankara, 75, 1-14

  • Cole, W. S. ve Bermudez, P.J., 1944, New foraminiferal genera from the Cuban Middle Eocene: Bull. Amer. Paleont. 28, 113, 333-344.

  • Kaever, M., 1970, Die alttertiaren Grossforaminiferen südost-Afganistans unter besonderer Berüeksichtigung der Nummuli tiden, Morphologie, Taxonomie und biostratigraphie: Münster. Forsch. Geol. PalUont, 16/17, 1-400.

  • Sirel, E., 1976, Description of the species of Rhapydionina liburnica Stache, Rhapydionina malatyaensis n.sp. and new observation on the genus of Rhapydionina Stache: Bulletin of the Mineral Research and Exploration Institute of Turkey, 86 (inpress).

  • Environmental Geology Problems of Ortahisar
    Vedat Doyuran
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  • pumice flows

  • flow tuffs

  • Neogene

  • Ortahisar

  • Fenner, C.N., 1948, Incandescent tuff flows in southern Peru: Geol. Soc. America Bull., 59, 879-893.

  • Pasquara, G., 1968, Geology of. the Cenozoic volcanic area of Central Anatolia: Accademia Nazionale Dei Lincei, Roma, Seri VIII, IX, 204 s.

  • Reynolds, D.L., 1954, Fluidization as a geological process, and its bearings on the problem of intrusive granites: Am. Jour. Sci., 252, 577-613.

  • Ritchie, A.M., 1963, Evaluation of rockfall and its control: Highway Research Record, 17, 13-28.

  • Ercüment Sirel
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    The Ophiolitic Melange and Other Formations in The Karaman-Ermenek (Konya) Region.
    Ali Koçyiğit
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    Abstract: The rock units cropping out in the investigation area form two associations differing from each other bytheir stratigraphic and tectonic properties. The units are termed Ophiolitic melange and Other formations.The investigation area consist of a coloured melange including olisthostromes and blocks of various lithology andsize with an age between Middle Permian and Maastriehtian, Bloke and olisthostromes are emplaced in a matrix mostlycomposed of voleanies (diabase, spilite, dolerite, ignimbritic tuff, vitric tuff) and partly of sedimentary rocks(graywackes, clay, marl, radiolarite and pelagic limestones with aboundant Badiolaria). The minimum age of thismixture (coloured melange) is Maastriehtian and all of its members are of marine origin.The rock units forming the coloured meloured melange are covered by marine Miocene sediments. The Miocenesediments (polygenic conglomerates, sandstone, sand, silt, clay, marl, reef limostone, sandy limestone) showing laterallyand vertically gradation to each other and composing of different thicknesses and lithofacieses and also lacustrinePliocene limestones unconformably overlyines the Miocene sediments have been termed as Other formations. 

  • Ophiolitic melange

  • diabase

  • radiolarite

  • pelagic limestones

  • Konya

  • Blumenthal, M., 1956, Karaman-Konya Havzası Güneybatısında Toros kenar silsileleri ve şist-radyolarit formasyonu stratigrafi meselesi: M.T.A. Dergisi, Sayı 48, Ankara.

  • Niehoff, W., 1960, Mut 126/1 numaralı harita paftasının revizyon neticeleri hakkında rapor: M.T.A. Der. Rap., No. 3390, Ankara, yayımlanmamış.

  • Koçyiğit, A., 1972, Üçbaş-Sarıkaya (Karaman) çevresinin jeolojisi: Yüksek Lisans Tezi, A.Ü.F. Fakültesi G. Jeoloji - Stratigrafi Kürsüsü, yayımlanmamış.

  • Gökten, E., 1975, Mut-Silifke yöresinin temel kaya birimleri ve Miyosen stratigrafisi: Doktora Tezi, A.Ü.F. Fakültesi G. Jeoloji - Stratigrafi Kürsüsü, Türkiye, Jeol. Kur. Bült, 19, 117 - 126.

  • Basement Rock Units and The Miocene Stratigraphy of Silifke Region
    Yaşar Ergün Gökten
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    Abstract: Formations of Devonian, Middle Permian, Late Jurassic, Late Cretaceous, Lutetian and Miocene age Croppout in the investigation area. The Devonian consists of conglomerates, dolomitized limestones, quartzites and clayschist;The Middle Permian is composed of pisolitic-oolitic limestones; The Upper Jurassic formations consist of limestones anddolomitized limestones; The Upper Cretaceous is represented by pelagic limestones and serpentinites of melange character.The Lutetian transgressively covering the above mentioned formations is represented by a brecciated limestone outcrop.These rock units of an age between Devonion and Lutetian, and various lithology, constitute the Basement rock units inthis region.The Miocene sediments overlying the Basement rock unitsj as transgressive and grading in to each other vertically andlaterally are represented by polygenic conglomerates, sandstones, marls and reef limestones. Five planctonic foraminiferalblozones, which three of them of Burdiga`ian age, the others two of Helvetian to Tortonian (?) were defined in theseformations

  • pisolit

  • oolitic

  • transgressive

  • Silifke

  • Akarsu, I., 1960, Mut bölgesinin jeolojisi: M.T.A. Enst. Derg. No. 54, s. 36-45.

  • Blow, W.H., 1969, Late middle Eocene to Recent planktonic foraminiferal biostratigraphy: Proc. of the first international conf. on plank, microfossils. Geneva, s. 199-421

  • Blumenthal, M.M., 1956, Karaman-Konya havzası güneybatısında Toros kenar silsileleri ve şist-radyolarit formasyonu stratigrafi meselesi: M.T.A. Enst. Derg. No. 48 s. 1-36, Ankara.

  • Bizon, G. Bizon, J.J., Feinberg, H. ve Öztümer, E., 1974, Antalya, Mut ve Adana havzaları Tersiyer biyostratigrafisi ve mikropaleontoloji yenilikleri: Tür. 2. Pet. Kong. Teb. s. 217-228, Ankara

  • Cati, F. ve Borsetti, A.M., 1968, Biostratigrafia del Miocene in facies Romaglona (Formazione Marnoso-Arenacea): Committee on Medi terranean Neogene Stratigraphy Proceedings: Gior. Geol. s. 401- 410, Bologna

  • Cita, M.B. ve Blow, W. H., 1969, The biostratigraphy of the Langhian, Serravallian and Tortonian stages in the type-sections in Italy: Riv. Ital. Paleont. V. 75 No. 3 s. 549-603, Milano.

  • Cita, M.B. ve Premoli s. I., 1968, Evolution of te planktonic foraminiferal, etc.: Gior. Geol. (2), XXXV, fasc. Ill s. 1-28, Bologna.

  • Crescenti, TJ., 1966, Sulla biostratigrafia del Miocene effiorante al confine marcigiano-abruzzese: Geol. Rom. 5, s. 1-54. Roma.

  • Koeyigit, A., 1975, Karaman-Ermenek (Konya) bölgesinde ofiyolitli melanj ve diğer oluşuklar: Tez. A.Ü.F.F. Jeol-Strat. Kurs., Türkiye Jeol. Kur. Bttlt, 19, 103-116.

  • Kraseninnikov, V.A., 1968, Correlation of te Miocene deposits of the Miocene deposits of the eastern, ecc.: Gior. Geol. (2) XXXV, fasc. I ll s. 167-178, Bologna.

  • Nieoff, W., 1960, Mut 126/1 numaralı harita paftasının revizyon neticeleri hakkında rapor: M.T.A. Derleme Rap. No. 3390.

  • Geochemistry and Origin of The Hırka Diatomaceous Earth Deposit
    Ali Uygun
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    Abstract: The Hırka diatomaceous earth deposit from Taşhan formation in the north of Kayseri (Central Anatolia)is Lower Pliocene age. Chemical analyses have been performed for quality tests and study of the origin. The results ofthe mathematical correlations show three element-assemblages in opal-, carbonate-, and detritic minerals (clay-minerals,plagioclases and others from volcanics) groups. Montmorillonite minerals are identified in diatomaceous earth layers.Based on paleogeography, distribution of the flora and clay minerals and on siliceous concretions, the origin of thedeposits is explained with silica - rich, postvolcanic springs and silicate alteration.

  • diatomaceous

  • opal

  • Montmorillonite

  • clay

  • Kayseri

  • Alexander, G.B., Heston, W.M., Her, H.K., 1954, The solubility of amorphus silica in water: J. Phys. Chem. 58, 453-455.

  • Benda, L,., 1974, Die Diatomeen der niedersâchsisehen Kieselgur-Vorkommen, palökologische Befunde und Nachweis einer Jahressehichtung: Geol. Jahrb. Reihe A, Heft 21, 171-197.

  • Cholnoky, B. J., 1968, Die ökologie der Diatomeen in Binnengewassern: 699 s., Lehre.

  • Degens, E.T., 1968, Geochemie der Sedimente; Stuttgart, 282 s.

  • Füchtbauer, H., Müller, G., 1970, Sedimente und Sedimentgesteine: 726 s., Stuttgart,

  • Harder, H., 1965, Experimente zur Ausfâllung der Kieselsâure: Geoch. Cosmoch. Acta, 29,5, 429-442.

  • Hustedt, F., 1969, Kieselalgen (Diatomeen): Stuttgart, 70 s.

  • Krauskopf, K.B., 1956, Dissolution and precipitation of silica at low temperatures: Geoch. Cosmoch. Açta, 10, 1-26.

  • Lewin, J.C., 1961, The dissolution of silica from diatom walls: Geoch. Cosmoch. Acta, 21, 3-4, 182-198.

  • Nebert, K., 1959, Die Kieselbildungen des simischen Magmatismus in Anatolien: Bull, of the Min. Kes. and Expl. Institute of Turkey, 53, 1-20.

  • Okamoto, G., Okura, T., Goto, K., 1957, Properties of silica in water: Geoch. Cosmoch. Acta, 12, 123-132.

  • Siever, R., 1957, The silica budget in the sedimantary cycle; Am. Miner. 42, 821-841.

  • Taliaferro, NX., 1933, Relation of volcanism to Diatomaceous and associated siliceous sediments: Bull. Univ. California, Dept. Geol. ScL, 23, 1, 1-55.

  • Taylor, S.R., 1965, The application of trace elements data to problems in petrology: Physics a. Chem. of the earth, 6, 133-213.

  • Tessenow, U., 1967, Untersuehungen über den Kieselsâurehaushalt der Binnengewasser: Arc. Hydrobiol. Suppl., 32, 1, 1-136.

  • Türkiye Diyatomit Envanteri, 1968, M.T.A. Enstitüsü, 138, Ankara, 28 s.

  • Uygun, A., 1976, Geologie und Diatomit-Vorkommen des Emmiler-Hırka Neogen Beekens (Kayseri-Türkei), doktora tezi, 137 s., Bonn. (yayımlanmamış).

  • Ergani (Maden) Copper Deposits and Plate Tectonics
    Saldiray İleri Berkin Salanci Mehmet Bitem Ramazan Doğan
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    Abstract: Ergani (Maden) copper mineralization which takes place in "Ophiolitic Belt" of "Taurid Tectonic Unit" inSoutheastern Turkey, show some similarities to the Cyprus type of deposits assumed to be formed at sites of sea-floorspreading. The occurence of so many different ore minerals in Anayatak ore body and their puzzling relations to eachother, indicate that during and after mineralization equilibrium conditions changed continuously and the area was affected by drastic geological events. Interpretation of data reveals intensive marine volcanism and extensive tectonicdeformation have been taken place during and after mineralization. Such conditions, in the light of today`s tectonic understanding, may occur at sites of sea-floor spreading and deposits for med at such places may outcrop on the mainlanddue to later obduction. With the data at hand, it is assumed that Ergani copper mineralization is a Cyprus type deposit,formed at site of sea-floor spreading and pushed on the mainland by obduction. 

  • copper

  • plate tectonics

  • Cyprus type

  • Ophiolitic Belt

  • Aslaner, G., 1968, Doğu Anadolu`da bulunan Ergani-Maden bakır yatağının ve bilhassa yan taslarının maden mikroskopik incelemesi: M.T.A. Dergisi, 72, 176-188.

  • Ataman, G., Buket, E. ve Çapan, U., 1975, Kuzey Anadolu fay zonu bir Paleo-Benioff zonu olabilir mi?: M.T.A. Dergisi, 84. 112-118.

  • Bamba, T., ve Tin, A., 1972, Ergani Maden bölgesinin bakır yatakları, Güneydoğu Türkiye: M.T.A. Rapor No. 4968, yayımlanmamış.

  • Borehert, H., 1952, Ergani Maden bakır cevher yataklarında yapılan tetkikata dair rapor: M.T.A. Rapor no. 2803, yayımlanmamış.

  • Constantinou, G., ve Govett, G.J.S., 1973, Geology, geochemistry and genesis of Cyprus sulphide deposits: Econ. Geol., 68, 843-858.

  • Çoğulu, E., 1975, Hatay-Kızıldag Masifinin oluşumu hakkında yeni buluşlar: 50. yıl Yerbilimleri Kongresi, M.T.A. yayınları, 409-423.

  • Dewey, J.F., ve Bird, J.M., 1971, Origin and emplacement of the ophiolite suite: Appalachian ophiolites in Newfoundland: J.G. R., 76, 3179-3206.

  • Dickinson, W.R., 1972, Evidence for plate tectonic regimes in the rock record: Amer. Jour. Sci., 272, 551-576

  • Graff, XL., ve Skinner, B.J., 1970, Strength and deformation of pyrite and pyrrhotite: Econ. Geol., 65, 206-215.

  • Griffits, W.R., Albers, J.P., ve Öner, Ö., 1972, Massive sulphide copper deposits of the Ergani Maden area, Southeastern Turkey: Econ. Geol., 67, 701-713.

  • Ketin, I., 1948, Ergani Eğil bölgesinin jeolojik etüdü hakkında memuar: M.T.A. Rapor no. 2015, yayımlanmamış.

  • Ketin, t, 1966, Anadolu`nun tektonik birlikleri: M.T.A. Dergisi, 66, 20-34.

  • Sillitce, R.E., 1972, Formation of certain massive sulphide deposits at sites of sea-floor spreading: I.M.M. Bull., 81, B 141-148.

  • Sirel, M.A., 1952, Die Kupfererzlagerstaette Ergani Maden in der Türkei: N. Jb. Miner. Abh, 80 Abt. A, 36-100.

  • Skinner, B.J., ve Peck, D.L., 1969, An immiscible sulphide melt from Hawaii; Wilson, H.D.B., ed., Magmatic Ore Deposits de Econ. Geol. Monograph 4, 310-322.

  • Takashima, N., 1975, Geology of cupriferous pyrite deposits in the ophiolite series between Ergani and Madenköy (Siirt), southeastern Anatolia, Turkey: M.T.A. Maden Etüd Rapor no. M-218, yayımlanmamış.

  • Wijkerslooth, P., 1943, Ergani Maden bakır zuhuratının primer mineralleri: M.T.A. Dergisi, 31, 66-78.

  • Wijkerslooth, P., 1944, Elazığ ili (Ergani Maden) bakır yatakları hakkındaki bilgiye yeni bir ilâve: M.T.A. Dergisi, 33, 76- 104.

  • Polje of Akseki, The Formation and The Development of The Intramontane Plains in The Karstic Areas in The Taurus
    Nuri Güldali
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    Abstract: Akseki Plain is a small intramontane basin located at the north of Alanya in the highest part of TaurusMountain Range. This plain is a polje as far as the geomorphological characteristics are concerned. Compared with itsnearest surroundings the geological structure of this polje shows close similarities to the intramontane plains whichare various in number and size at the central and the West Taurus. Almost half of the polje basin is surrounded byboth the karstic pure limestones of the mesozoic age and an old Paleo-Eocen flysh formation which doesn`t show anyevidence of karstification. The floor of the polje is covered by a thin alluvial soil. In a large pat of it the eroded headsof the beds of flysh marn and limestones are expodes; even in a small part, mostly in marginal areas, the formation ofkarstic island hills has been observed (hum). Although surface drainage is effective in a small part of this polje, thelarger pat is drained by ponors lying in the South and the West. In some areas where ponors are found surroundinglimestone mountains of polje are steeply sloping. In the same areas it is generally noticed that the chemical solutionhas continued progressively and still continues. As a result of this study it is found that there are many factors in theformation and the developement of Akseki Polje. Of which the most important one is the mechanical erosion and thecarrying capability of the rivers, yet the tectonic movements in part and the carstic solutions in some small areas aoreeffective. 

  • marn

  • limestone

  • polje

  • Akseki

  • Bhımenthal, M.M. 1949, Akseki civarındaki dağlarda boksit zuhuratı, bunların jeolojik durumu ve jenezi hakkında İzahat: Maden Tetkik Arama Enst. Tay., Ankara 66 S.

  • Güldalı, N., 1970. Karstmorphologische Studlen im Cebiet des Poljesystems von Kestel (West-Taurus): Tüblnger Gegr. Studien, H. 40, 104 S.

  • Louis, H., 1956., Dis Enstehung der Poljen und ihre Stellun? in der Karstabtragımg, auf Grund von Beobachtungen im Taurus: Erdkunde 10, 33-53.

  • A Comparison Between The San Andreas and The North Anatolian Faults
    İhsan Ketin
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    Abstract: In many aspects, the San Andreas and the North Anatolian fault zones show many similarities. Fromthe geological point of view, as the San Andreas Fault in California, the North Anatolian Fault Zone is one of the estknown structure of the world. They are similarly right-lateral, strike-slip faults, at the same time, are transforms.They are of Late Miocene - Pliocene in age (10-12 m.y.) and are about 1100 - 1600 km long. Their zonal widths (0.5 - 10km) are in the same order and magnitude. Although sense of their strike-slip movement is principally right - lateral,they have a lef t-lateral branch (The Bast Anatolian Fault of the North Anatolian Fault and the Garlock Fault of theSan Andreas Fault). However, they vary in the maximum amount of lateral displacement and show different topographic features. The maximum offset is nearly 300 km along the San Andreas Fault whereas it is approximately 85-90km along the North Anatolian Fault. As far as the physiographical characteristics are concerned, The North AnatolianFault Zone is more spectacular than San Andreas Fault. 

  • San Andreas Fault

  • North Anatolian Fault

  • transform fault

  • Miocene

  • Abdüsselâmoğlu, S., 1959, Almacıkdağı ile Mudurnu ve Göynük civarının jeolojisi: Fen Fak. Monogr., 14, istanbul.

  • Arpat, E. ve Şaroğlu, F., 1975, Türkiye`deki bazı önemli genç tektonik olaylar: TJK Bült., 18/1, 91-101.

  • Aytun, A., 1973, İsmetpaşa istasyonu civarında krip ölçümleri: Kuzey Anadolu Fayı ve Deprem kuşağı simpozyumu/MTA. Enst., 114- 121.

  • Baird, A.K. ve diğerleri, 1974, Transverse Ranges Province: A unique structural - petrochemical belt across the San Andreas fault system: Bull., Geol. Soc. America, 85, p. 163-174.

  • Bird, A.K. ve Welday, E. 1974, Chemical trends across Cretaceous batholithic rocks of southern California: Geology, 2, p. 493-495

  • Canıtez, N., 1973, Yeni kabuk hareketlerine ilişkin çalışmalar ve Kuzey Anadolu Fay problemi: simpozyum, M.T.A. Enst., 35-58.

  • Crowell, J.C., 1975, San Andreas fault in southern California: Division of Mines and Geology, special Report, 18.

  • Ehlig, P.L. ve diğerleri, 1975, Offset of the Upper Miocene Caliente and Mint Canyon formations along the San Gabriel and San Andreas fault: Calif. Div. Mines and Geology, sp. Rep. 18.

  • Hill, M.L. ve Bibblee, T.W., 1953, San Andreas, Garlock and Big Pine faults, California: Bull. Geol. Soc. America, 64, p. 443-458.

  • Ketin, İ., 1969, Kuzey Anadolu Fayı hakkında: M.T.A. Dergisi, 72, 1-27.

  • Lawson, A.C. 1895, Sketch of the geology of the San Francisco Peninsula: P.S. Geol. Survey 15th. Ann. Rept., P. 405-447.

  • M.T.A. Enstitüsü. 1973, Kuzey Anadolu Fayı ve Deprem Kuşağı simpozyumu, Ankara.

  • Seymen, İ., ve Aydın A., 1972, Bingöl deprem fayı ve bunun Kuzey Anadolu Fay Zonu ile ilişkisi: M.T.A. Dergisi, 79, 1-8.

  • Seymen, İ., 1975, Kelkit Vadisi kesiminde Kuzey Anadolu Fay Zonu`- nun tektonik özelliği: I.T.Ü. - Maden Fak., Doktora tezi, istanbul.

  • Sharp, R.V., 1967, San Jacinto fault zone in the Peninsular Ranges Southern California: Geol. Soc. America, Bul., 78, p. 705-729.

  • Suppe, J., 1970, Offset of Late Mesozoic Basement terrains by the San Andreas fault system; Geol. Soc. America, Bul., 81, p. 3253-3258.

  • Tokay, M., 1973, Kuzey Anadolu Fay zonunun Gerede ile Ilgaz arasındaki kısmında jeolojik gözlemler: simpozyum, M.T.A. Enst. 12-29.

  • Vedder, J.G., 1970, Geologic map of the Wells Ranch and Elkhorn Hills quadrangles, California: U.S. Geol. Survey, Map 1-585.

  • Vedder, J.G., 1975, Juxtaposed Tertiary strata along the San Andreas fault in the Temblor and Caliente Ranges: Calif. Div. Mines and Geology spec. Report 18.

  • Wallace, R.E., 1970, Earthquake recurrence intervals on the San Andreas fault: Geol. Soc. America, Bull, 81, P. 2875-2890.

  • Wallace, R.E., 1975, The San Andreas fault in the Carrizo PlainTemblor Range region: Calif. Div. Mines and Geology, sp. Eep. 18.

  • Wilson, J.T., 1965, A new class of faults and their bearing on continental drift: Nature, 207; p. 343-347.

  • Woodford, A.O., 1960, Bedrock Pattern and strike-slip faulting in south-western California: Am. jour. Sci, 258A, p. 400-417.

  • The Stratigraphy and The Species of Nummulites of The Marine Oligocene of Kırklareli Region (North of Thrace)
    Ercüment Sirel Hatice Gündüz
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    Abstract: Systematic description of the species of Nummulites have been studied in the marine Oligocène sediments of Kırklareliregion (North of Thrace), in the otherhand the stratigraphy of the region is given shortly.The rock units of Paleozoic and Paleogene ages crop out in the region. Paleozoic (Lower Paleozoic) sequence is composed of metamorphic rocks. The Paleozoic rocks are unconformably overlain by the sandy and algal limestones of theLutetian? age. Algal limestones contain genera of the Foraminifera such as Discocyclina sp., Rotalia sp., Priabonian sequence conformably overlies the algal limestones of Lutetian (?) age, it is composed of sandy limestones and it ischaracterized by the species of Foraminifera such as Nummulites fabianii (Prever), Chapmanina gassinensis (Silvestri), Fa.biania cassis (Oppenheim), Discocyclina sp., Asterocyclina sp. and Queraltina sp., Lower-Middle Oligocène sequence conformably overlies the sandy limestones of Priabonian age. It is composed of clayey limestone. Oligocène sequence containsabundant Nummulites species, such as Nummulites intermedius (d`Archiac), N. fichteli Michelotti, N. vascus Joly andLeymerie in large amount. 

  • Nummulites

  • Foraminifera

  • Oligocène sequence

  • Kırklareli

  • Akartuna, M., 1953, Çatalca - Karaeaköy Jeolojisi; İ.Ü. Fen. Fak. Monog., 13, 1-88.

  • Archiac, A.d`, 1846, Description des fossiles recueillis par M. Thorent, dans les couches a Nummulines des environs de Bayonne: Soc. Geol. France, Mem., Paris, 2, 2, 1, 4, 1-199

  • Archiac, A.d`, 1850 Description des fossiles du groupe Nummulitique recueillis par M.S.P. Pratt et M.J. Delbos aux environs de Bayonne et de Dax: Soc. Géol. France, Mem., Paris, 2, 3, 397-456.

  • Archiac, A.d` ve Haime, J, 1853, Description des animaux fossiles du groupe nummulitique de l`Inde preceded d`un râsume géologique et d`une monographie des Nummulites: Paris, 1-373.

  • Ayhan, A., 1972, Istranca masifinin Yıldız dağları jeolojisi: M. T. A. Enst. Ankara, derleme no. 5130 (yayımlanmamış).

  • Belmustakov, E., 1959, Les fossiles de Bulgarie: Bulgarska Akad. Nauk, Sofia, 7-79.

  • Bursch, J.G., 1947, Mikropalaontologische Untersuchungen des Tertiars von Gross Kel (Molukken): Schweiz. Pal. Abh. (Mem. Suisses Pal.), 65, 3, 1-69

  • Boussac, J., 1908, Succession des faunes Nummulitique â Biarritz: Bull. Soc. Gol. de France, 4, VIII, 1-251.

  • Boussac, J., 1911, Etudes paléontologiques sur le Nummulitique alpin: France Serv. Carte Geol., Mâm., Paris, 1-437

  • Checchia - Rispoli, G., 1911, Sull`Oligocene dei dintorni di Campofiorito in Provincia di Palermo: Giorn. Sci. Nat. Econ., İtalya, Palermo, 28, 281-303.

  • Cizancourt, M. de, 1935, MatSriaux pour la stratigraphie du Nummulitique dans le dSsert de Syrie: Soc. GSol de France, Bull., Paris, 5, 4, 8-9, 737-758.

  • Cole, W.S., 1960, Upper Eocene and Oligocene larger Foraminifera from Viti Levu: Fiji, U.S. Geol. Survey, Prof. Paper, Washington, D.C., 374 - A, 1-7.

  • Dizer, A., 1962, Les Foraminiferes de L`Eocene et L`Oligocene de Denizli: Fac. Sci., Rev., Univ. Istanbul, B, 27, 1-2, 39-47.

  • Eames, F.E., Banner, F.T., Blow, W.H. ve Clarke, W.J., 1962, Fundamentals of Mid - Tertiary stratigraphical correlation: - Part 1. Cambridge, England: University Press, 1-59.

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  • The Stratigraphy and Paleogeographical Evolution of The Upper Cretaceous-Lower Tertiary Sediments in The Haymana-Polatli Region (SW of Ankara)
    Güner Ünalan Vedat Yüksel Gürol Ataman Osman Gönenç Zinet Seyîrt Selahî Hüseyin
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    Abstract: Deposits ranging from Upper Cretaceous (Maestrichtian) to Lower Tertiary in age crop out in Haymana - Polatlı region. At the base of these deposits there are Temirözü, Mollaresul, Dereköy Formations which are outof scope of present study. The formations, starting from Maestrichtian are as follows: Haymana Formation (Maestrichtian) is in flysch faeies, and 1850 m thick. Maestrichtian aged Beyobasi Formation is represented by coral sandstonesand conglomerates and 125 m thick. Çaldağ Formation (Montian) which is represented by algal limestones and 1187 mthick, crops out near Haymana. In the North, West and South of the region, this unit shows interfingering with redcolored Kartal Formation, and in the Southeast of the region wedges out to Yeşilyurt Formation which contains limestone .blocks. Thanetian aged Kirkkavak Formation is represented by algal limestone and black marls and 640 m thick.Ilgmlikdere Formation (Ilerdian) is in flysch facies and. 350 m thick. Eskipolatli Formation (lower parts Herdian, upperparts Cuisian) consists of marls with sandstone and limestone and limestone bands. Cuisian - Lutetian aged ÇayrazFormation consists of sandy limestones with abundan NummuUtes. This unit is equivalent to Beldede Formation (conglomerates, marls, limestones) in the North and West, and to Yamak Formation, which is in flysch facies, in the Southeast of the region. Neogene overlies all these formations unconformably. The thickness of the Upper Cretaceous -Lower Tertiary deposits is 5800 m in the region. Deposition was continious with the exception of the local unconformitybetween Çayraz and Eskipolatli Formations in the North of Haymana. Lateral and vertical facies changes are abundant. Interpretation of the facies studies shows that there existed a semicircle-shaped shelf near Haymana; Çaldağ andÇayraz Formations are deposited on this shelf. Behind the shelf partly continental units, Kartal, and Beldede, and infront of the shelf flysch units, Haymana, Yeşilyurt, and Yamak were deposited. Throughout Late Cretaceous - EarlyTertiary times, Haymana - Polatlı basin is believed to be joined with the Salt _ Lake basin toward the Southeast, andflysch deposits are accumulated in this part of the region. This shows that the North and West parts of the regionwere filled with sediments and were uplifted afterwards. 

  • limestone

  • marl

  • sandstone

  • Haymana

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  • Observations on Some Analcime Bearing Pyroclastites Occured in Taurus Mountains, at SW of Karaman
    Nezih Tuzcu
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    Abstract: The analcime bearing pyroclastic rocks »situated at 45 km SW of Karaman (Konya) are interbedded within the rocks of Cretaceous age which have a thickness of approximately 600 m. These pyroelastites, formed by volcanicactivity, show a normal graded bedding. Their classification is based not on the size of the fragments, but the compositional properties of them.By XRF analysis, it has been found that these rocks contain Na2O in quantities higher than normal, and were probably rich in terms of volcanic glass. It is possible that this oxyde has entered in the composition of the pyroclastitesby chemical action of the sea water - probably metasomatic processes. In the first of two stages of transformations thattook place later, the analcime, which is the mos characteristic mineral of the pyroclastites, was most likely formed bydiagenesis of volcanic glass. Subsequently, a low grade metamorphism corresponding to the upper most part of zeolitefaeies occurred. In fact, the analcime is partially - totally transformed in a secondary albite in which relicts of theformer mineral can often be observed.

  • pyroclastic

  • XRF analysis

  • zeolite

  • Karaman

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  • Tuzcu, N., 1972, Etude mineralogique et pétrographique de la région de Başkısla dans le Taurus occedental (Karaman, vilâyet de Konya, Turquie): Mem. Dept. Mineral. Univ. Geneve, no: 1, 1-109.

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