Türkiye Jeoloji Bülteni
Türkiye Jeoloji Bülteni

Türkiye Jeoloji Bülteni

1993 AĞUSTOS Cilt 36 Sayı 2
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The Study of Cinoptilolite - Rich Tuffs from Bigadiç by NMR Technique
Işik Kumbasar Saim Özkar
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Abstract: The clinoptilolite - rich upper tuffs of Bigadiç area are in the form of coarse grained glassy as tuffs at thebottom and fine grained dust tuffs on the top. The framework structures of natural clinoptilolites taken from this both formation have been characterized by means of high - resolution solid - state nuclear magnetic resonans (NMR). The results of 29Si and 27A1 - MAS NMR studies of these samples have been compared with the data for various natural clinoptiloties. It is seen that they differ from the data of heulandite.

  • clinoptilolite

  • heulandite

  • NMR Technique

  • Bigadiç

  • Baysal, O., N. Gündoğdu, A., Temel, F. Ömer, 1988, Bigadiç Zeolit Oluşumlanmn Ekonomik Jeolojik İncelenmesi Projesi, H.Ü. Yuvam / 85 - 2 (Basılmamış).

  • Ercan ve diğ., 1984; Bigadiç çevresinin (Balıkesir) jeolojisi ve mağmatik kayaçlann petrolojisi. TJ.K. Kurultayı Bülteni S. 5,75 - 85.

  • Esenli, F., 1992, Gördes çevresindeki Neojen Serilerinin ve Zeolitleşmenin Jeolojik, Mineralojik ve jeokimyasal incelemesi. Doktora Tezi (Basılmamış).

  • Göktekin, A., 1989, Bigadiç Tülü Ovası Zeolitlerinin Teknolojik Özelliklerinin Araştırılması, (Rapor, basılmamış) l.T.Ü. Yer Bilimleri ve Yeraltı Kaynaklan UYGAR.

  • Gündoğdu, N., 1982, Neojen Yaşlı Bigadiç Sedimanter Baseninin Jeolojik Mineralojik ve Jeokimyasal İncelemesi. Doktora Tezi, H.Ü. Yayınlanmamış.

  • Nakata, S., Asaoka, S., Kondoh, I. and Tabakashi, H., 1986, Identification and Characterization of Natural Zeolites by Magnetic Resonance. Stud. Surf. Sci. Catal. 28 (New Dev. Zeolite Sci. Technol).

  • Petrov, Sr., 1983, X - ray Powder Diffraction Studies of Cation Exchanged Natural Zeolites. Mat. 1st. Nat. Symp. Diffr. Methods. 156.

  • Sirkecioğlu, A., Esenli, F., Kumbasar, I., Eren, R.H, Şenatalar, A.E., 1990 Mineralogical and Chemical Properties of Bigadiç Clinoptilolite: Variation of Ammonium ion Exchange Capacity With Zeolite Content. IESCA.

  • Thomas, J.M. and Klinowski, J., 1985, The Study of Aluminosilicate and Related Catalysts by NMR Spectroscopy. A<*v. Catal .33,199.

  • Stratigraphy of Autochthonous and Cover units of the Bozdağlar Massif NW Konya
    Yaşar Eren
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    Abstract: This paper is concerned with the stratigraphy of autochthonous (? parautochthonous) metamoiphic rocksof the Bozdağlar massif and its unmetamorphosed cover units, in northwest of Konya.The Upper Permian - Lower Cretaceous Gökçeyurt group, which is obducted by Mesozoic Ladik metamorphitesin the study area, is the autochthonous/parautochthonous assemblage of the massif. The group consists mainly oflower - grade metamorphic rocks originally representing shallow - marine environment and is herein subdivided in three formations which are gradational to one another. These are, in ascending order, (1) The Upper Permian Derbentformation composed of metecarbonate, metaquartzite and phyllite, (2) The Upper Permian - Upper Triassic Aladağ formation consisting of alternation of metaconglomerate, metasandstone, phyllite and metacarbonate with exotic metacarbonate blocks and rare metabazite intercalations, and (3) The Upper Triassic - Lower Cretaceous Lorasdağı formationwhich is made up of a thick sequence o metacarbonate rocks with a few interbeds o metachert.The Upper Miocene - Lower Pliocene Dilekçi group consisting of alluvial fan, lacustrine and volcanic rocks, TheUpper Pliocene - Quaternary alluvial complex of Topraklı formation and Recent alluvia unconformably rest on theolder units and form the cover rocks of the massif.

  • autochthonous

  • alluvial fan

  • metaconglomerate

  • Konya

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  • Brennich, G., 1954, 1/100.000 ölçekli genel jeolojik harita izahnamesi, Akşehir (90 - 1, 2, 3, 4) ve Ilgın (91/1 ve 91/3) Paftaları, M.T.A. Derleme Rap. No: 2514 (Yayınlanmamış).

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  • Eren, Y., 1990, Engilli (Akşehir) ve Bağkonak (Yalvaç) köyleri arasında Sultandağları Masifi`nin tektonik özellikleri, Türkiye Jeol. Bült., 33/1, 39 - 50.

  • Eren, Y., 1991 a, Engilli (Akşehir) - Bağkonak (Yalvaç) arasında Sultandağlan Masifi`nin stratigrafisi, Ahmet ACAR Jeolojisi Sempozyumu Bildiriler, Adana, 83 - 92.

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  • Esen, Y., 1993 a, Eldeş - Derbent - Tepeköy - Söğütözü (Konya) arasının Jeolojisi, Doktora Tezi, S.Ü. Fen Bilimleri Enstitüsü, Konya, 224 s. (yayınlanmamış).

  • Esen, Y., 1993 b, Konya kuzeybatısında Ilgın. Kadınhanı güneyinin stratigrafisi, 46. Türkiye Jeoloji Kuruüayı, Bildiri Özleri, s. 72.

  • Eren, Y., 1993 c, Konya kuzeybatısında Bozdağlar Masifi`nin yapısal özellikleri, 46. Türkiye Jeoloji Kurultayı Bildiri Özleri, s. 27.

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  • Güzel, A., 1983. Sarayönü - Kadınhanı (Konya) dolayının hidrojeoloji incelemesi. S.Ü. Müh. Mim. Fakültesi Jeoloji Müh. Böl, Doktora Tezi, Konya, 115 s., (yayınlanmamış).

  • Jung, D., Keller, J., 1972, Die jungen vulkanite im raum zwischen Konya und Kayseri (Zentral - Anatolien) Z. Deutsch. Geol. Ges., 123, 503 - 512.

  • Keller, J., Jung, D., Burgath, K. ve Wolff, F., 1977, Geologie und petrologie des Neogenen kalkalkali - vulkanismus von Konya 5erenler Dağı - Alacadağ Massiv, Zentral - anatolien), Geol. Jb.,B25,37-117.

  • Ketin, İ, 1966, Anadolunun tektonik Birlikleri (Tectonic Units of Anatolian Asia Minor), M.T.A. Enstitüsü Dergisi, 66,20 - 34.

  • Okay, A.I., 1984, Distribution and characteristics of the nortwest Turkish blueschistes, In: Robertson A.H.F. and Dixon, J. E., (eds.) The Geological evolution of the Eastern Mediterranean, spec. publ. Geol. Soc. London, 17,297 - 308.

  • Okay, A. L, 1986, High - pressure / low temperature metamorphic rocks of Turkey, in Blueschits and eclogites, The Geol. Soc. of Amer, Mem. 164,338-348.

  • Ota, R., Dinçel, A., 1975, Volcanic rocks of Turkey, Bull. Geol. Surv. Japon, 26,18 - 45.

  • Özcan, A., Göncüoğlu, M.C., Turan, N., Uysal, Ş., Şentürk, K. ve Işık, a., 1988, Late Paleozoic evolution of the Kütahya - Bolkardağ belt, METU Journal of Pure and Appl. Sci., 21, 1/3,211-220.

  • Özgül, N., 1976, Toroslar`ın bazı temel jeolojik özellikleri, Türkiye Jeol. Kur. Bült., 19, 65 - 78.

  • Özgül, N., 1984, Stratigraphy and tectonics evolution of the central Taurides, International Symposium on the geoloy of the Taurus Belt., 77 - 90, Ankara.

  • Öztürk, E. M., 1987, Of NW - SE trending Sultandağ and Anamasdağ NW of Western Taurides, IGCP Project No: 5, Guide Book, 26 - 34.

  • Roberts, N., 1982, Age paleoenvironments and climatic significance of Late Pleistocene Konya Lake, Turkey, Quaternary Research, 19,154 -171.

  • Selley, R.C., 1976, An Introduction to sedimentology, Acad. Press., London, 408 s.

  • Şengör, A.M.C., Yılmaz, Y., 1981, Tethyan evolution of Turkey: A plate tectonic approach, Tectonophysics, 75,181-241.

  • Üstündağ, A., 1987, Sızma - Kurşunlu - Meydan - Bağrıkurt köyleri arasında Karadağ çevresinin jeolojisi, Yüksek Lisans Tezi, S.Ü. Fen Bilimleri Enstitüsü, Konya, 65 s. (yayınlanmamış).

  • Wiesner, K., 1968, konya civa yatakları ve bunlar üzerindeki etüdler, M.T.A. Enstitüsü Dergisi, 70,178 - 213.

  • The Geology of Şaplıca (Şebinkarahisar - Giresun) Alunite Deposit and An Approach to the Genessis of Alunite by Using Sulfur Isotope Data
    İsmet Özgenç
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    Abstract: Şaplıca alunite deposit is located near the Şebinkarahisar town (Giresun) within Pontide belk Alunite mineralization exists at the vicinity of the vein type sulfide deposits. Alunite deposit and part of sulfide veins occur in intensly alterated volcanites of late Cretaceous. The alunite deposit is exclusively confined by the volcanites. Alunite mineralization is controlled by E - W and NE - SW trending normal faults which are barren. They form the channel - wayof H2SO4 rich magmatic hydrothermal fluids. Alunites are produced by the base leaching of phenocrysts (typically alkali feldspar) of rhyolitic and rhyodacitic host rocks. Alunite minerals typically occur as aggregates of bladed or lathlikecrystals up to 1 mm. long, replacing alkali feldspar and groundmass, intergrown with quartz. Alunite is locally abundantin the centre of the advanced argillic alteration zones which develop throughout the late Cretaceous volcanites. As thealunite zone develops vertically downward, advanced argillic alteration zone develops laterally outward from the aluniteborder. Kaolinite is the dominant clay mineral of this extensive alteration type. The alunite zone is ringed by kaolinite zone. The acid sulfate alteration is typically characterized by a mineral assemblage of predominantly alunite, kaolinite,silica (as quartz and chalcedony), pyrite and sericite. Alunitization is a subset of this advanced argillic alteration.Sulfur isotope analyses have been performed on monomineralic concentrates from Şaplıca alunites and associated sulfides. The alunites (+ 8,9 %o + 10,7 %o + 12,8 %o) are enriched 34s, relative to sulfides (-1,3 %o; -2,9 %c; -5,3%6) which are depleted in 34 S . Calculated isotopic fractionation factors (a * = 1,007 - 1,018) and isotopic differences(A34s = 6,93 - 17,83) of associated alunit - sulfide pairs indicate the hypogene origin of alunites. This result is supported by the textural and mineralogical features of Şaplıca alunite deposit. It is most likely that requisite amounts ofH2SO4 must have been generated by a magmatic hydrothermal environments.

  • alunite

  • Sulfur isotope analyses

  • rhyolit

  • Giresun

  • Ayan, Z., 1991, Şebinkarahisar (Giresun) kuzeybatısındaki Pb - Zn - Cu cevherleşmelerinin mineralojik - jeokimyasal incelenmesi ve kökensel yorumu: D.E.Ü. Müh. Fak. Jeoloji müh. Bölümü., Doktora Tezi, 186 s. (yayınlanmamış),, izmir

  • Berger, B.R., ve Henley, R.W., 1989, Advances in understanding of epithermal gold - silver deposits, with special reference to the western United States: Econ. Geol., Mon. 6, 405 - 423.

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  • Cunningham, C.G., Rye, R.O., Steven, T.A., ve Mehnert, H.H., 1984, Origins and exploration significance of replacement and vein type alunite deposits in Marysvale volcanic field, west central Utah: Econ. Geol., v. 79,50-71.

  • Çalapkulu, F., 1982, Asarcık (Şebinkarahisar - Giresun) uranyumlu Pb - Zn - Cu cevherleşmesinin incelenmesi: E.Ü. Yerbilimleri Fak., Doçentlik Tezi (yayınlanmamış), İzmir

  • Field, C.W., 1966, Sulfur isotopic method for discriminating between sulfates of hypogene and supergene origin: Econ. Geol., v. 61, 1428 - 1435.

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  • Güner, S., 1991, Giresun - Şebinkarahisar, Sivas - Suşehri yöresi maden jeolojisi raporu: MTA derleme no. 9248, Ankara.

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  • Ketin, 1., 1966, Anadolu`nun tektonik birlikleri: MTA Derg., 66,20 - 35, Ankara

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  • Ohmoto, H., 1972, Systematics of sulfur and carbon isotopes in hydrothermal ore deposits: Econ. Geol.,v.67,p.551-578.

  • Pişkin, Ö., Delaloye, M., ve Fontigne, D., 1993, The geochronology by K/Ar method of the plutonics of Şebinkarahisar area, Giresun - Turkei: In press.

  • Rye, R.O., Bethke, P.M., ve Wasserman, M.D., 1992, The stable isotope geochemistry of acid sulfate alteration: Econ. GeoL, v. 87, p. 225 - 262.

  • Rye, R.O., ve Ohmoto, H., 1974, Sulfur and carbon isotopes and ore genesis; a review: Econ. Geol., v. 69, p. 826-842.

  • Sakai, H., 1968, Isotopic properties of sulfur compounds in hydrothermal processes: Geochem. J. (Japan)., 2,29-49.

  • Sakai, H., ve Yamamoto, M., 1966, Fractionation of sulfur isotopes in the preparation of sulfur dioxide; an improved technique for preccision analyses of stable sulfur isotopes: Geochem. J. (Japan)., 1,35-42.

  • Schoen, R., ve Rye R.O., 1970, Sulfur isotope distributions in solfataras, Yellowstone National Park: Science., v. 170, p. 1082 -1084.

  • Taşkın, C, ve Polat, A., 1986, Giresun ili, Şebinkarahisar ilçesi, Gedehor (Şaplıca) köyü, alünit etüd ve aramalarına ait rapor: MTA derleme no: 4809, ankara.

  • Terzioğlu, N., 1985, Reşadiye (Tokat) kuzeyindeki Eosen yaşlı Hasanşeyh plato bazaltlarının mineralojik, petrografik ve jeokimyasal incelenmesi: C.Ü. Müh. Fak. Yerbilimleri Derg., 2, 1,106-133, Adana.

  • Tokel, S., 1977, Doğu Karadeniz bölgesinde Eosen yaşlı kalkalkalen andezitler ve jeotektonizma: TJK Bült., 20,43-54, Ankara.

  • Tuncalı, E., 1974, Giresun ili, Şebinkarahisar ilçesi alünit ruhsat sahalarının jeolojik etüdü: MTA derleme no: 5261, Ankara.

  • The Chemical Changes During Zeolitization (Heulandite - Clinoptilolite Type) of the Acidic Tuffs in the Gördes Neogene Basin
    Recep Fahri Esenli
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    Abstract: The tuffs of Neogene basin around the Gördes Region have high content of zeolite about 2/3 magnituteof their volume and contain less or not in some zones. Zeolite mineral type is clinoptilolite in the lower tuffs and heulandite is present in the upper tuffs. This difference is seen clearly on the whole rock chemistry of two tuff units. The geochemical relations between chemical elements and the quantity of zeolitization were examined and it is found thatall the major chemical elements are mobile. Some elements were been liberated from fresh glasses and used again for zeolitization or other alterations in the same system. Although, some of the major elements may have come from out ofthe system. Lossing of SiO2, Na ^ and K^O, and gaining of A12O3, MgO, CaO and HgO have been determined whenwe compared unaltereted rock with zeolite - rich rock. These changes show more increasing in both the loss and gain inthe heulandite alteration than in the clinoptilolite alteration. 

  • zeolite

  • alteration

  • tuff

  • Gördes

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  • Esenli, F., 1992, Gördes çevresindeki Neojen serilerin ve zeolitleşmenin jeolojik, mineralojik ve jeokimyasal incelenmesi. Doktora tezi, Î.TÜ. Fen Bilimleri Enstitüsü, Yayınlanmamış, 208 s.

  • Esenli, F., Özpeker, I., 1993, Gördes çevresindeki Neojen havzanın zeolitik diyajenezi ve höylandit - klinoptilolitlerin mineralojisi. 46. Türkiye Jeoloji Kurultayı, Bildiri Özleri Kitabı, s. 63.

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  • Walton, a., 1975, Zeolitic diagenesis in oligocene volcanic sediments, Trans - Pecos, Texas. Geol. Soc. of Amer. bull., 86,615 - 624.

  • Lithostratigraphic and Tectonic Features of Himmetoğlu (Göynük - Bolu) Oil Shale Field of Neogene Age
    Mehmet Şener
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    Abstract: Oil shales have been deposited from Precambrien to Tertiary in the geological history of the Earth, andthey are distributed in Europe, South America, Western United States, and in Turkey. Middle anatolia, Western Blacksea, Aegean and Marmara regions are important in respect to oil shales in Turkey. Volcanosedimentary lacustrine basins of Neogene age are the main geological environments in which oil shales were deposited in Turkey. Himmetoğluoil shale field have been selected as an example among the others. So, only this field have been investigated in detail.Himmetoğlu formation occurs in a graben, caused by reactivation of paleotectonic structures in the neotectonicregime. Lithostratigraphical features of this formation have been investigated in detail on core samples.Himmetoğlu formation has 4 different zones: Green clay and conglomerate, lignite bearing, banded bituminousmarl, laminated bituminous marl. Organic matters and pyroclastic sediments which were transported in different periodshave been deposited together in the basin. 

  • oil shale

  • paleotectonic

  • pyroclastic

  • Bolu

  • Abdülselamoğlu, Ş., 1959, Almacık dağı ile Mudurnu ve Göynük civarının jeolojisi: İ.Ü. Fen Fak. Mon, No: 14

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  • Besbelli, B., 1991, Adapazarı H 25 b 1, b 4, c 1 paftalarının jeolojisi ve petrol olanakları: MTA Raporu (Yazımda).

  • Beseme, P., 1967, Kabalar senklinalinin (Göynük - Bolu) genel ve uygulamalı jeolojik etüdü: MTA Raporu (No: 4629).

  • Beseme, P., 1968, Seyitömer (Tavşanlı - Kütahya) monoklinalinin genel jeolojik ve uygulanmalı incelenmesi: MTA Raporu (No: 4673).

  • Cole, R.D., 1984, Sedimantological, mineralogical and geochemical definition of oil shale facies in the lower Parachute Creek member of Green River formation, Colorado: 17 th Oil Shale Symposium Proceedings. Colorado School of Mines. Edited by James H. Gary.

  • Douglas, A.G., and Hall, P.B., 1983, Comparative organic geochemistry of some Europen oil shales: in geochemistry and chemistry of oil shales. Ed. by Mıknıs, F.P. and McKay, F.J.

  • Eroskay, S.O., 1965, Paşalarboğazı - Gölpazarı sahasının jeolojisi: Î.Ü. Fen Fak. Seri: B, Cilt: XXX, 3 - 4,135 -170.

  • Gündoğdu, M.N., ve Gökçen, S., 1983, Bigadiç gölsel Neojen basenindeki birincil sedimanter yapılar ve kökenleri: H.Ü. Yerbilimleri, 10, 89-93.

  • Hufnagel, H., 1984, Die ölshiefer Jordaiens: Geol. Jb. A. 75, 295 -311.

  • Hufnagel, H., 1989, Investigation of oil shale deposits in Western Turkey. Part 1. Seyitömer and Beypazarı - Çayırhan: BGR. Hannover. 215 p.

  • Hutton, A.C., 1986, Classification of Australlian oil shales: Energy explor. Exploit. 4, 81 - 93.

  • Kalkan, 1., 1991, Adapazarı H 25 b 2, b 3, c 2 ve Adapazarı H 26 b 1, b 2 paftalarının jeolojisi: MTA Raporu (Yazımda).

  • Ketin, L, 1966, Anadolu`nun tektonik birlikleri: MTA Dergisi, 66, 20 - 34.

  • Ketin, î., 1984, Türkiyenin bindirmeli - naplı yapısında yeni gelişmeler ve bir örnek: Uludağ Masifi. Ketin Sempozyumu. TJK. 227 s.

  • Kulaksız, S., ve Demirbugan, M.A., 1988, Göynük - Bolu linyit yatağı duyarlılık analizi: Türkiye Kömür Kongresi, TMMOB Maden Müh. Od. Yayını. Zonguldak.

  • Patterson, J.N., Ramsden, A.R., and Dale, L.S., 1988, Geochemistry and mineralogical residence of trace elements in oil shales from Condor deposit, Queensland, Australia: Chem. Geol, 67,327 - 340.

  • Saner, S., 1977, Geyve - Osmaneli - Gölpazarı - Taraklı alanının jeolojisi, eski çökelme ortamları ve çökelmenin evrimi: Doktora Tezi, İ.Ü. Fen Fak.

  • Saner, S., 1980, Mudurnu - Göynük havzasının Jura ve sonrası çökelim nitelikleriyle paleocoğrafya yorumlaması: TJK Bült, 23,1, 39 - 53.

  • Sarı, A., 1985, Himmetoğlu yöresinin ekonomik jeolojisi: Yük. Müh. Tezi. A.Ü. Fen Fak.

  • Sonel, N., Sarı, A., ve Tozlu, E., 1987, Himmetoğlu - Göynük - Bolu yöresinin jeolojisi ve linyit oluşukları: S.Ü. Müh. Mim. Fak. Derg., 2, 51 -67.

  • Şener, M., 1992, Himmetoğlu (Bolu - Göynük) Neojen baseninin jeolojik, mineralojik ve jeokimyasal incelenmesi: Doktora tezi. H.Ü. Fen Bil. Ens. 145 s.

  • Taka, M., 1988, Himmetoğlu (Göynük - Bolu) sahasının bitümlü şeyi olanakları ve sondajları: MTA Raporu. (No: 8533).

  • Temel, A., ve Gündoğdu, M.N., 1988, Distribution and characteristics of primary sedimentary structures in borate containing sedimentary units withi the Bigadiç lacustrine volcanosedimentary basin of Neogene age, NW Turkey: METU Journal of pure and Applied sciences. 21,251-269.

  • Tuğluhan, M., ve Mehmetoğlu, T., 1990, Bolu - Göynük - Himmetoğlu bitümlü şistinin oksidasyon kinetiği: Türkiye 5. Enerji Kongresi. Teknik oturum tebliğleri. 3,147 -158.

  • Turgut, A., ve Dümenci, S., 1980, Bolu - Göynük linyit havzasına ait jeolojik rapor: MTA Raporu (No: 6885).

  • Ziegler, J., 1936, Kütahya linyit havzası (Seyitömer) kenar mıntıkası jeolojik tetkikati hakkında rapor. MTA Raporu (Yayımlanmamış).

  • Stratigraphy of the Northern Portion of Akseki and Üzümdere (Antalya) Vicinity
    Hatice Vedia Toker Nurettin Sonel Turhan Ayyildiz Mustafa Albayrak
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    Abstract: In this study the stratigraphy of the northern portion of Akseki region (Middle Taurus, Antalya), and itsdepositional environments is described. The units in the study area is divided in two tectonics slices and named as Akseki and Akdağ - Yelekdağ tectonic units. The Akseki units are represented by neritic facies during Jurassic (Dogger) -Middle Eocene time, and pelagic to hemi - pelagic during Eocene (Lutetian) time. In contrast, Akdağ - Yelekdağ unitsare represented by neritic facies until late Cretaceous (Maestrichtian), and hemipelagic to pelagic until Eocene (Lutetian) time.

  • pelagic

  • stratigraphy

  • sedimantary rock

  • Akseki

  • Akbulut, A., 1980, Eğridir gölü güneyinde Çandır (Sütçüler - İsparta) yöresindeki Batı Toroslann Jeolojisi, T.J.K., 23,1 - 9.

  • Ayyıldız, T., 1992, Üzümdere - Akkuyu (Akseki - ANTALYA) Civannm Petrol Olanaklan, Yüksek Lisans Tezi, 196 s, Ankara.

  • Blumenthal, M.M., 1947, Seydişehir - Beyşehir hinteralanmdaki Toros dağlarının jeolojisi. M.T.A., 2,242 s.

  • Blumenthal, M.M. ve Göksu, E., 1949, Akseki civanndaki dağlarda boksit zuhuratı, bunlann jeolojik durumu ve jenezi hakkında izahat: M.TA. Raporu.,n. 14.

  • Blumenthal, M.M., 1951, Batı Toroslarda Alanya ard ülkesinde jeolojik araştırmalar: M.TA., n. 3, 194 s.

  • Bouma, A.H., & Brouwer, A., (Eds) 1964., Turbidites, Elsevier, Amsterdam, pp: 264.

  • Demirtaşlı, E., 1976, Akseki - Manavgat - Köprülü bölgesinin temel jeoloji incelemesi: T.J.K., 32. Bilimsel ve Teknik Kurultayı (yayımlanmamış),Ankara.

  • Demirtaşlı, E., 1977, Toros Kuşağının petrol potansiyeli: 3. Petrol Kongresi Tebliğleri, 55 - 62, Ankara.

  • Demirtaşlı, E., 1979, Batı Toros kuşağının (Akseki kuzeybatısı) petrol potansiyeli: T.J.K. 1. Bilimsel ve Teknik Kongresi., 187 -190, Ankara.

  • Demirtaşlı, E., 1984, Stratigraphy and tectonics of the area between Silifke and Anamur, Central Taurus Mauntains. Geology of the Taurus Belt.,p: 101-119, Ankara.

  • Demirtaşlı, E., 1987, Akseki - Manavgat - Köprülü bölgesinin temel jeoloji incelemesi: M.TA. Rapor no: 3292 (yayımlanmamış), Ankara.

  • Dumont, J.F., 1976, Etudes geologiques dans les Taurides occidentals: les formations paleozoques et mesazoiques de la coupole de Karacahisar (province d1 İsparta, Turquie): These 3 cycle. Univ. Paris - Sud (Orsey), 213 p.

  • Dumont, J.F., Uysal, Ş., Poisson. A., 1980, Batı Toros Platformu: M.T.A., n: 823 (yayımlanmamış), Ankara.

  • Dunham, RJ., 1962 Classification of carbonate rocks according to depositional texture, A.A.P.G., Memoirl,p: 109-121.

  • Farinacci, A & Radoicic, R., 1965, Correlazione fra serie giuresi e cretacee dell` Appennino centrale e delle Dinaridi esterne: Ricerca Scienüf.,v.34,pp.269-300.

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  • Gutnic, M., Monod, O., Poisson, A., et Dumont, J.F., 1979, Geologie des Taurides Occidentales (Turquie): Mem. Soci. Geol., 58, pp: 109.

  • Günay, E, Bölükbaşı, A.S., Gözeğer, C, İnançlı, L, 1979, Bati Toroslarda Murtiçi - İbradı - Seydişehir arasındaki alanın jeolojisi ve petrol olanaktan: T.P.A.O., Rapor no: 1390, (yayımlanmamış).

  • Koçyiğit, A., 1984, Tectonostratigraphic Characteristic of Hoyran Lake Region (İsparta Bend). Geology of the Taurus Belt, p: 53 - 69, Ankara.

  • Martin, C, 1969, Akseki kuzeyindeki bir kısım Toroslann stratigrafik ve tektonik incelemesi: M.TA.Derg., 72. 157-175.

  • Monod, O., 1977, Recherchcs geologiques dans les Taurus occidental au sud de Beyşehir: These Eresente a I`Universite de Paris sud Centre d`Orsa, 442 p.

  • Nebert, K., 1964, Güneybatı Toroslardaki kuzey hareketleri (Akseki güneyi), M.TA. Derg., 62, 12 -41.

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  • Özgül, N., 1976, Toroslann bazı temel jeoloji özellikleri: T.J.K., Bült., 19,1,65 - 78.

  • Özgül, N., 1984, Staritigraphy and tectonic evolution of the Central Taurides, Geology of the Taurus Belt, p: 77 - 90, Ankara.

  • Özlü, N., 1979, Akseki - Seydişehir boksitlerinin kökeni hakkında yeni bulgular: Türkiye Jeol. Kur. Bült., 22,215 - 227

  • Toker, V., Sonel, N., Ayyıldız, T., 1993, Akseki - Aydmkent (ANTALYA) Civarının Jeolojisi ve Stratigrafisi, TBAG - 922,100 s., Ankara.

  • Türkünal, S., 1969, Toros dağlarının kuzeyde Beyşehir ile güneyde Oymapınar köyü enlemleri, doğuda Güzelsu bucağı ile batıda Kırkkavak köyü boylamları arasında kalan kesimin jeolojisi: E.1.E.1, Ankara.

  • Wilson, J.L., 1975, Carbonate Facies in Geologic history, Springer - Verlag., Berlin, pp: 476.

  • Wippern, J., 1962, Toros boksitleri ve bunun tektonik durumu, M.TA. rapor no: 58 (yayımlanmamış), Ankara.

  • Stable Isotope (O, H and C) Geochemistry and Origine of The Mineralizing Fluid in Kurşunlu (Koyulhisar - Sivas) Vein Type Pb-Zn-Cu Deposits
    Ahmet Gökçe Baruch Spiro Milke F. Miller
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    Abstract: The vein type Pb-Zn-Cu deposits in Kurşunlu area are hosted by the Upper Cretaceos volcanicand volcanosedimentary units with an average attitude of N50°W / 75 - 85°NE. They contain galena, sphalerite, chalcopyrite, pyrite, chalcosite and hematite as ore minerals and accompained quartz, calcite and localy barite as gangue minerals.Previous sulfur isotope and fluid inclusion studies showed that the sulfur in sulfide minerals is magmatic origineand might have been leached from the surrounding volcanic rocks and mineralising fluid has a character of low salinityand dominantly contains NaCl (±KC1, CaCl, MgCl) indicating that the water may be meteoric origine.Oxygen and hydrogen isotope studies (81 8O = in the range of -3.4 ile +0.6 %o, 8 D = in the range of - 31.4 ile70.4 %o) show that the water in mineralising fluid is the deepsirculated meteoric water in mineralising fluid is the deepsirculated meteoric water with some 18O enrichment as a result of isotopic exchange reaction with the surrounding volcanic rocks. Carbon isotopic composition of CO2 in inclusion fluid indicate that the mineralising fluid might have penetrated trough the marine or terrestrial carbonate unites. According to the results of all field and laboratory investigations helded on the mineralization; it may be said thatthe vein type Pb-Zn-Cu deposits in the area were formed by the deep - sirculated meteoric water leaching the sulfur andpossibly metal ions from the surrounding volcanic rocks and depositing along the fault zones. 

  • Stable Isotope

  • volcanic rocks

  • gangue minera

  • Sivas

  • Clayton, R.N. ve Mayeda, T.K., 1963. The use of bromine pentafluoride in the extraction of oxygen from oxides and silicates for isotope analysis. Geochim. Cosmochim. Acta, 27,43 - 52.

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  • Gökçe, A., 1990b. Kurşunlu (Ortakent - Koyulhisar - SİVAS) Pb-Zn-Cu yataklarında kükürt izotopları incelemesi M.T.A. Dergisi, 111, 111 - 118.

  • Gökçe, A., 1993. Hidrotermal maden yataklarının köken ve oluşum koşullarının araştırılmasında kararlı izotoplar jeokimyası incelemeleri ve Türkiye`den trnekler. Jeoloji Mühendisliği Dergisi, Sayı 42 (baskıda).

  • Gökçe, A. ve Özgüneylioğlu, A., 1988. Kurşunlu (ortakent - Koyulhisar - Sivas) Pb-Zn-Cu yataklarının jeolojisi, oluşumu ve kökeni. Cumhuriyet Univ., Müh. Fak., Yerbilimleri Dergisi, 5/1,23 - 36.

  • Hoefs, J., 1987. Stable isotope geochemistry. Springer Verlag,241p.

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  • Geologic Evolution of the Anatolian Segment of the Tethyan Belt
    Metin Şengün
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    Abstract: The geological constraints presented in this paper show that the northern strand of Neotethys isnon-existent and the existing suture is actually of the Tethys (Paleotethys). Geologic and published paleomagneticevidence has been integrated to the conclusion that this ocean has persisted for the entire Palaezoic and Mesozoic andhas been consumed through periodically recessing northward subduction between the Triassic and Lutetian in westernand central Anatolia.Western Pontides has been rotated dextrally during the Permo - Triassie, contributing to upwarp of the Triassicarc, initiation of rifting of the western Black Sea and obduction of marginal ophiolites onto the active margin. Theenigma for the coeval Pontian and Gondwanian Karakaya formations is briefly discussed with emphasis on regressivenature of Triassic - Early Liassic sedimentation in Pontides versus the continuous fining - upward Mesozoic sequencesof the passive margin.The Jurassic (Late Triassic - Early Liassic) granitoids of the Pontides are suggested to correspond to thefractionated residue of the basic volcanism of the Triassic arc. These granites have intruded the Karakaya formation andhave been transgressed by a carbonate - flysch wedge of the southward onlapping back - arc basin, the Black Sea, inliaison with oceanward shift of the respective compressive and dilatational systems of the fore-arc and back-arc basinsdue to a presumable recess of subduction. The deposition in the extensional basins has started in troughs of earliercolapse and the intervening areas have been subject to progressive submergence between Portlandian - Berriasian andthe uppermost Cretaceous.There has been an incipient collision during the Cretaceous with intense shearing of the fore-arc and thepremontories of the passive margins of the intermediate and Arabian plates. A HP/LT deformation deletes all pre -Cretaceous deformations along the 50 km. wide Tethyan suture. The Cretaceous shear zones repeat with widening,towards the north, deformation being resticted to planes of movement when sufficiently away from the suture, enablingobservation of juxtaposed Cimmerian and Cretaceous deformations.Ophiolites have been obducted onto the passive margins of both Tethys and Neotethys during the early stages ofthe collisional period, uplifted by imbricate thrusting on the passive margin, finally gliding in foredeeps(exogeosynclines) that have been forming due to rotational processes.The Neotethys has sutured along immediate north of Bitlis/Puturge massives by Late Lutetian. However, thecompletion of colage has lasted until the Late Miocene in between these massives. The role of transform faults foracquisition of the fit of continental masses has been emphasised. Numerous left-lateral transforms are still active,aiming to push Western Anatolia southwards, onto the oceanic crust in the Eastern Mediterranean, the part of theNeotethys which has not completed its obliteration.

  • Tethyan Belt

  • ophiolite

  • granite

  • Anatolian

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  • Dercourt, J., zonenshain, L.P., Ricou, L.E., Kazmin, V.G., Le Pichon, X., Knipper, A.L., Grandjacquet, C, Sbortshikov, I. M., Geyssant, V., Lapurier, C, Perhersky, D.H., Boulin, J., Sibuet, J.C., Savostin, L.A.., Sorokhtin, O., Westphal, M., Bazhenov, MX., Lauer, J.P. and Biju - Duval, B., 1986, Geological evolution of the Tethys belt from the Atlantic to the Pamirs since the Lias. Tectonophysics, 123: 241 - 315.

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  • Stratigraphy of the Gürün Autochthon (Between Gürün and S ar iz), Eastern Taurus-SW Sivas (Turkey)
    Eşref Atabey
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    Abstract: In this study the stratigraphical aspects of the Gürün autochthone between Gürün and Sanz part havebeen investigated. In the area, between time interval of Paleozoic and Tertiary, the 14 different units have been differentiated. The lower part of the Gürün autochthone (relative autocthone) is represented by rock units of the Upper Devonian and Upper Permian. Gümüşali formation (Upper Devonian), is composed of sandstone, quartzite, limestone, dolomite and shale and Yığılıtepe formation (Upper Permian) consist of limestone and dolomite. The Carboniferous and LowerPermian is not represented by any units. The boundary relation between Yığılıtepe formation and, recrystallized limestone, clayey limestone, marl, sandstone of Katarası formation (Lower Triassic) is an unconformity. The presence ofMiddle Triassic has not been detected.The firstly differentiated units of the Upper Triassic and Lias, rock units; The Toycu Tepe formation (UpperTriassic) is composed of algae limestone and dolomitic limestone while the Çukuryurt formation (Lias) is representedby conglomerate/breccia, sandstone, algaecoral limestone, and shale. Yüceyurt formation of Middle JurassicCenomanian age is overlying the Çukuryurt formation with an angular unconformity. This unit consists of algae limes tone, dolomitic limestone and dolomite. The lower levels of Turonian-Coniacian and Santonian are not presend. TheUpper Santonian-Campanian (Yaniktepe formation) is represented by conglomerate/breccia, rudist limestone.The Akdere formation (Upper Campanian-Maastrictian) transitional to Yaniktepe formation is composed ofconglomerate/breccia, calcarenite and clayey limestone.In the study aera, The Adbalpman formation (Paleocene-Lower Eocene) locally trasitional with underlyingAkdere formation and is composed of dominant pebbly sandstone whose pebbles are conglomerate/breccia, calcarenite,clayey limestone, cherty nodule marl, Demiroluk formation (Lutetian) locally transitional with Abdalpmari formation isrepresented by conglomerate/breccia, Nummulite bearing limestone and marl. These rock units are overlain by an angular unconformity, which the youngest overlying units are conglomerates of Gövdelidağ formation (Upper EoceneLower Miocene) and sandstone, marl and limestone of the Gürün formation (Miocene).

  • marl

  • dolomitic limestone

  • breccia

  • Sivas

  • Akkuş, M. F., 1963, Gürün bölgesinin genel jeolojisi ve petrol olanakları (Elbistan-K38a3, di, d4 paftaları), MTA,, Derleme Rap. No, 4063. (yayımlanmamış).

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  • Ayan, T., 1963, Darende batısındaki Hezanlı-Işkın ve Tüde dağlan bölgesinin (Elbistan K38-c4 L38-a2, SE) detay jeolojisi ve petrol imkanları, MTA. Derleme Rap., No, 4435 (yayımlanmamış).

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  • Aziz, A., Erakman, B., Kurt, G. ve Meşhur, M., 1982, Pınarbaşı - Sanz - Gürün ilçeleri arasında kalan alanın jeolojisi raporu, TPAO. Rap., no, 1601 (yayımlanmamış).

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  • Varol, B., Kazancı, N., ve Altmer, D., 1987b, Doğu Toroslarda otokton Geyikdağı Birliğinde OrtaÜst Triyas` in varlığı (Sarız-Tufanbeyli yöresi, Kayseri), MTA, Derg., 10), 170-171.

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  • Yoldaş, R., 1972, Kayseri (Sarız) dolayının (ElbistanL36-b2, L37-al paftaları) jeolojisi ve petrol olanakları, MTA. Derleme Rap., no, 4729 (yayımlanmamış).

  • The Ostracode Biostratigraphy of the Antakya Basin
    Ümit Şafak
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    Abstract: It this study, ostracode biostratigraphy with the lithologic features of the Lower Miocene - Pliocene squences in Antakya and surrounding area has been investigated. 142 samples were taken from 7 measured stratigraphicsections. 120 ostracode species have been identified from the Lower Miocene - Pliocene sequence. The datumplane ofCarinocythereis and Cyprideis with Neomonoceratina helvetica - Aurila soummamensis Zone, Gökçen (1984) havebeen described with these species in the region. This zone and datumplanes have been correlated within the previously -studied Tethys - Paratethys regions and with contemporary sequences deposited in Turkey. When the environmentaldistribution of ostracodes was taken in  consideration, together with shallow marina fauna, that lagoonal environmentostracodes are effective from place to place, found from the beginning of the sequence to top, were established.

  • ostracode

  • lagoonal environment

  • e biostratigraphy

  • Antakya

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  • Petrology and Geochemistry of the Jurassic - Cretaceous Magmatic Rocks Between Tirebolu - Harşit (Giresun)
    Nezihi Köprübaşi
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    Abstract: In the investigation area, the basement area formed by Pontid Lower Basic Volcanic Complex of Jurassic- Lower Cretaceous age and is intruded by the Harşit Granitoid. The unit is covered by the Lower Harşit VolcanicComplex of Upper Cretaceous. This rock group comprises three phases independent of one another, begining wiyh volcanism and ending with sedimentation. The youngest volcanics in the area are the olivine - augite basalts of Neogeneage.The rocks belonging to the Pontid Lower Basic Volcanic Complex are in a geochemical character, which is generally calcalkalen, but rather, showing transition to tholeiite and indicating a primitive arc environment. The Harşit Granitoid has I-type, peraluminus, calcalkalen features and characterize an island arc environment that is getting mature.The rocks bellonging to the Lower Harişt Volcanic Complex are also related to the subduction and are calcalkalen in character. 

  • tholeiite

  • calcalkalen

  • basalt

  • Giresun

  • Acar, E., 1972, Giresun - Tirebolu - Harşit - Köprübaşı Kurşun, Çinko, Bakır Madenin Jeolojik Araştırma ve Ön Rezerv Etüd Raporu, M.T.A. Rap. No: 1354 (yayınlanmamış), Ankara.

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  • Zanettin, B., 1984, Proposed new chemical classification of volcanic rocks: Episod, 7 / 4,19 - 20.

  • Zankl, H., 1959, Harşit Vadisi Bölgesinde Yapılan Maden Yatakları ile ilgili Jeolojik Etüd Hakkında Rapor., M.T.A. Rapor No: 2751 (Yayınlanmamış), Ankara,

  • Zankl, H., 1962, Magmatismus und Bauplan des Astpantischen Gebirges im Querprofil des Harşit - Tales., Bayerisch Akademie der Wissenchaften, Abhandlungen, Neue Folge., Heft 109,61-69.

  • Characteristics and Origin of Chromite Occurrences in Ortakale (Sarıkamış - Kars) Region, E - Turkey
    Necati Tüysüz
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    Abstract: A number of chromite occurrences different in size and shape are encountered in Ortakale region. Chromites around Ortakale appear as massive and highly rounded bodies of 4 - 5 m in diameter. They are enveloped by a 2 -20 cm thick dunitic sheath, whereas those around Kurtdeliği Tepe are hosted by hartzburgites. The area of interest is amelange and hence, the chromites are more likely aligned along the fault zones.The massive chromites have higher Cr2O3 wt. % and lower Al and Fe*3 than the accessory chromites in juxtoposed gabbros. A gradual decrease in Cr/Al ratio occurs between the massive and accessory chromites. In addition, accessory chromites in harzburgites are mostly idiomorphic and are resorbed at varying degrees. These chemical and pysicalvariations in the chromites may be attributed to fractination which played an important role at the frist stage of chromiteprecipitation. Therefore, it may be concluded that the chromites are formed in an environment similar to stratiformcomplex, but have passed through a complex history before residring as podiform bodies in their present - day position.The chromites show pull - apart features and are altered along margins and fractures to ferritchromite that is enriched inCr and Fe and impoverished in Mg and Al compared with the parent grains. 

  • chromite

  • gabbro

  • harzburgite

  • Kars

  • Ahmed, Z., 1984, Stratigraphic and textural variations in the chromite composition of the ophiolitic Sakhat Qua complex, Pakistan, Econ. Geol, 79,1334 -1359

  • Boudier, F. ve Nicolas, 1986, Harzburgite and subtypes in obpiolitic and oceanic environments, Earth Planet. Sci. Lett., 76, 84 - 92

  • Dick, H.J.B. ve Bullen, T., 1984, Chromian spinel as a petrogenetic indicator in abyssal and alpine - tpe peridoties and spatially associated lavas, Contrib. Mineral. Petrol., 85,54 - 76

  • Dickey, J.R. ve Yolder, H.S., 1972, Partitioning of chromium and aluminium between clinopyroxene and spinel, Carnigie Ins. Washington, Year book, 71, 384-392

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  • Hutchinson, C.S., 1972, Alpine - type chromite in north Borneo, With special reference to Danuel Bay, Am. Mineral, 37, 835 - 856.

  • Irvine, T.N., 1965, Chromian spinel as a petrogenetic indicator, Part 1, Theory, Can. J. Eadth Sci., 2, 648-671.

  • Irvine, T.N., 1967, Chromian spinel as a petrogenetic indicator, Part 2, Petrologic applications, Can. J.EarthSci.,4,71-103

  • Jan, M.Q. ve Windley, B.F., 1990, Chromian Spinel - Silicate Chemistry in Ultramafic Rocks of the Jijal Complex, NW - Pakistan, Journ. Petrology, 31,666-715

  • Leblanc, M. ve Temagoult, A., 1989, Chromite pods in a lherzolite massif (Colto, Algeria): evidence of oceanic - tpe mantle rocks along the western Mediterranean Alpine Belt, Lithos, 23, 153 -162

  • Loney, R.A., Himmelberg, G.R. ve Coleman, R.G., 1971, Structure and petrology of the alpine - type peridotite at Burro Mountain, California, U.S.A., Jour. Petrology, 12,245 - 309

  • Marakushev, A.A., 1979, Some aspects of ore formation in ultramafics, Min. Deposita, 14, 81 -101

  • Musallam, K., 1989, Geologische, petrologische und lagerstattenkundliche Untersuchungen an den ophiolitischen Gesteinen des Aras Gebirges (Provinz Kars, Türkei), arşiv no: 105875, 71 s., BGR - Hannover (yayınlanmamış)

  • Nicolas, A. ve Violette, J.E., 1982, Mantle flow at ocenic spreading center model derived from ophiolites, Tectonophysics, 81, 319 - 339

  • Paktunç, A.D., 1990, Origin of podiform chromite deposits by multistage melting, melt segregation and magma mixing in the upper mantle, Ore Geol. Rev., 5,211-222

  • Panayiotou, A., 1978, The mineralogy and chemistry of the podiform chromite deposits in the serpentinites of the Limassol Forest, Cyprus, Min. Deposita, 13,259 - 274

  • Schwarz, H, 1986, Übersichtsbefahrung des westlichen Aras - Gebirges zwischen Ağn, Kağızman und Kuloğlu, 5s, Vermerk, BGR - Hannover (yayınlanmamış)

  • Sinton, J.M., 1977, Equilibration history of the basal alpine - type peridotite, Red Mountain, New Zealand, Jour. Petrology, 18,216 - 246

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  • Thayer, T.P. 1969, Gravity differantiation and magmatic re - emplacement of podiform chromite deposits, Econ. Geol. Monogr. 4,132 -146

  • Thayer, T.P., 1970, Chromite segregations as petrogenetic indicators, Geol. Soc. S. Africa, spec, publ. 1,380-390.

  • Üşümezsoy, Ş., 1986, Kefdağ ve Soridağ (Guleman) kromit kütlelerinin oluşumu üzerine yeni bir yaklaşım, Jeol. Müh. derg., 29,47 - 60

  • Zhou, M.F. ve Bai, W.J., 1992, Chromite deposits in China and their origin, Min. Deposita, 27, 192-199

  • Characteristics and Formations of Fossil Manganese Nodules in the Koçali Komplex, Adıyaman, Turkey
    Hüseyin Öztürk
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    Abstract: Manganese nodules in the dölostone and radiolarian brown claystone in the Konak Formation of KoçaliComplex Upper Jurassic-Lower Cretaceous in age had been developed by early diagenetic processes. The replacement of silicic tests by Mn and other transition heavy metals such as Cu, Ni, Ba is the main mechanism of the nodule development. Both manganese nodules and associated manganese mineralization was effected by late diagenetic processes. The proceses resulted in the dissolution and migration of elements such as Cu, Ni, Mn, Si and addition of the elements such as Ca, Mg, Si. Thus, dolomite manganocalcite, calcite, quartz and pyrolusite veinlets formed as late diagenetic mineral assamblages. Hydrogenetic manganese nodules was not formed at the sediment sea water interface owing to oceanic bottom currents and episodic fluctuations of Mn in the sea water. Another reason for the absance of formationhydrogenous manganese nodules could be high sedimentation rate which indicates an enverionment close to active plate margin.

  • Manganese nodules

  • calcite

  • dolomite

  • Adıyaman

  • Amthor, J.E. and Friedman, G.M., 1992, Early to late diagenetic dolomitization of platform carbonates: Lower Ordovician Ellenburger Group, Permian basin, west Texas. Journal of sedimentary petrology, v. 68, no 1, P. 131 — 144.

  • Bonatti, E., Kraemer, T., Rydell, H., 1972, Classification and genesis of submarine iron manganese deposits. In Horn, DR., ed. Ferromanganese deposits on the ocean floor: Washington D.C. National science foundation, p. 149 — 165.

  • Crerar, D.A. and Barnes, H.L., 1974, Deposition deep sea manganese nodules. Geochim. Cosmochimica Acta, 38, p. 279 — 300.

  • Dymbnd, J., 1981, Geochemistry of Nazca Plate surface sediments: An evalution of hyrothermal, biogenic, detrital and hyrogenous source. In : L.D. Kulm, J. Dymond, E.J. Dasch and D.M. Hussong (eds), Nasca Plate: Crustal formation and Andean Convergence. Geol. Soc. Am. Mem., 145,133 —137.

  • Dymond, J.R., Lyle, M., Finney, B., Piper, D.Z., Nurphy, K., Conrand, R. and Nicklas, P., 1984, Ferromanganese nodules from MANOP sites H,S and R — control of mineralogical and chemical deposition by multiple accretionary processes. Geochim. Cosmochimica Acta, 48 : 931 — 939.

  • Halbach, P., Gursky, H.J., Gursky, M.N., Schmidt, R., Maresch, W.V., 1992, Composition and formation of fossil manganese nodules in Jurassic to Cretaceous radiolarities from Nicoya ophiolite complex (NW Cocto Rica). Mineralum deposita, 27,153 — 160.

  • Heath, G.R., 1981, Ferromanganese nodules of deep sea. Economic Geology, 75, p. 736 — 765.

  • Hein, J.R., Lisa, A.M., David, A.C., Ranhold, A.K., 1987, Cobalt rich ferromanganese crust from the exculusive econimic zone of the U.S. and nodules from oceanic Pasific. Sircum Pasific Council for Energy and Mineral Resources. Earth science series, vol. 6, p. 753 — 771.

  • Hein, J.R., Ross, C.K., Alexander, E. and Yeh, H.Z., 1979, Mineralogy and diagenesis of surface sediments from DOMES areas A,B and C. In J. Bischoff and D.Z. Piper (eds) Marine geology and oceanography and the Pasific manganese nodule Province. Plenum, New York, p. 365 —396.

  • Hein, C.R., Koski, R.A., 1987, Chert hosted manganese deposits in sedimentary sequences of the Fransiscan Complex, Diablo range, California. Siliciceous sedimentary rock hosted ores and petroleum. By Van Nostrand Reinhold Company, Inc. New York, p. 207 — 230.

  • Hein, J.R., 1987, Bacterially mediated diagenetic origin for chert hosted manganese deposits in Franciskan Complex, California coast ranges. Geology v. 15, p. 722 — 726.

  • Hein, J.R., Marjorie, S.S., Gein, L.M., 1992, Central Pasific cobalt rich ferromanganese crusts. Historical perspective and regional variability. Keating, BH., and balton, B.R., (eds) Geology and offshore mineral resources of the central Pasific basin, sircum Pasific council for energy and mineral resources. Earth science series, v. 14, New York Springer Verlag.

  • Klinkhammer, G.P. and bender, M.L., 1980, The distribution of Manganese in Pasific Ocean. Earth and Planetary Science Letters, v. 46, p. 361 — 384.

  • Maxon, J.H., 1937, Reconnaissance geology, oil possibilities and mineral resources of Southeastern Turkey, M.T. A. rap. no 680, Ankara

  • Mukhopadhyay, S., Dasgupta, S. and Roy, S., 1988, Distribution and charecter of micronodules in pelagic sediments from Central Indian Ocean and their implications: Marine Min. 7, p. 351 — 360.

  • Nishimura, M., 1992, Sedimantation and hiatuses in the central Pasifle Basin: Their relationship to manganese nodule formation. Keating, B.H. and Balton, B.R. (eds), Geology and offshore mineral resources of the Central Pasific Council for energy and mineral resources. Earth science series, v. 14, New York, Springer Verlag.

  • Perinçek, D., 1978, Çelikhan Sincik Koçali (Adıyaman ili) alanının jeoloji incelemesi ve petrol olanaklarının araştırılması. Doktora tezi, l.Ü. Fen Fakültesi, Tatbiki Jeoloji Kürsüsü. 212 sayfa.

  • Robertson, A.H.F. and Dixon, J.E., 1984, Introduction: Aspects of the geological evolution of the Eastern Mediterranean In: J.F. Dixon and A. H.F. Robertson eds. The geological evolution of the eastern Mediterranean. Spec. Publ. Geol. Soc. London. 17,1 —74.

  • Roy, S., Dasgupta, S., Mukhopadhyay, S. and Fukuoka, M., 1990, Atypical ferromanganese nodules from pelagic Areas of the Central Indian Basin, Equatorial Ocean. Marine Geology, 92 p. 269 —283.

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  • Şengör, A.M.C. and Yılmaz, Y., 1981, Tetyan evolution of Turkey, A plate tectonic approach, Tectonophysics, 75, p. 181 — 251.

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  • Sungurlu, O., 1972, VI. Bölge Gölbaşı Gerger arasındaki sahanın Jeolojisi. TPAO Rapor no: 802, yayınlanmamış, Ankara.

  • Tromp, S., 1940, Preliminary report on the oil possibilities of SE Turkey, M.TA. Report, Ankara.

  • Yalçın, N., 1976, Narince — Gerger (Adıyaman ili) alanının jeoloji incelemesi ve petrol olanaklarının araştırılması, Doktora tezi, Î.Ü. Tatbiki Jeoloji Kürsüsü.

  • Yamamoto, S., 1988, Ferromagnesian and metalliferous pelagic clay minerals in oceanic sediments. In Chilingarian, G.V. and Wolf, K.G. eds., Diagenesis II: Developments of sedimentology, 43, Amsterdam, elsevier, p. 115 — 146.

  • Yamamoto, S., 1992, Diagenetic enrichment of manganese and other heavy metals in hemipelagic brown clay of Palu Trench floor. Journal of Sedimentary petrology v. 62, p. 706 — 711.

  • An Example From Bozburun (Marmaris, Muğla) Peninsula to Transgressive Carbonate Platform Sequence
    Şükrü Ersoy
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    Abstract: In this paper, an environments and their interpretation of platform carbonates underlying the sedimentarytectonic sheets exposed on the Bozburun (Marmaris, Muğla) peninsula have been explained.Ptatform carbonates, at the base, begins with replacement dolomites being generally coarse crystaline. These passes upwards pelloidals. Packstönes and wacestones occured in the subtidal environments. Abudant bearing pelloidal carbonates have been most probably sedimented in the shelf lagoon. The sections of platform caibonates exposed on thesouth of study area are represented by loferitic siklothems upward deepening consisting of collapse breccia, algal crustand mats, abudant bioclast bearing limestones, from bottom to top, respectively. This facies suggesting periodic relativechanges of sea-level on the immediate backreef or bank-ende of the carbonate platform. 

  • dolomite

  • caibonate

  • breccia

  • Muğla

  • Berneouilli, D.; Graciansky, P. C. de; Monod, O. (1974), The extension of the Lycian Nappes (SW Turkey) into the Southeastern Aegean islands. Eclogae Helv., 67,1,4-90.

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  • Ersoy, Ş. (1989), Fethiye (Muğla)- Gölhisar (Burdur) arasında Güney Dağı ile Kelebekli Dağ ve dolaylarının jeolojisi (doktora tezi). l.Ü. Fen Bilimi. Ens., 246s.

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  • Two Different Type of Cu - Mineralizations of Zahuran (Maden - Elazığ)
    Ayhan Üstündaş Ahmet Sağiroğlu
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    Abstract: Zahuran and its vicinity are composed of two different units, (1) Middle Eosen Maden Complex which isthe oldest unit of the studied area, is composed of basalt, basaltic andesites, diabase, pillow lavas, sandstone - shale intercalations, red - gray mudstones, calcerous shale and various sized limestone blocks. (2) Lower Miosen Lice Formation is made up of alternating sandstone, shale and marls Lice Formation exposes through a tectonic window under theMaden Complex.The Mineralizations of Zahuran occur in two types; (a) Volcano - sedimantary mineralizations in pillow lavas,(b) Fault zone fillings what appears to be formed circulating hydrothermal solutions in the fault zone, These two typesof mineralizations show different charecteristies in respect two their relations with country rock, mineral assemblagesand wall-rocks alterations.The mineralizations in pillow lavas are roughly bedded and beds are parallel to pillow lava horizons, A wall -rock alteration which is closely related to the mineralization is absent, However a more conspicuos and general alteration is present. Ore minerals of this type are bornite, chalcopyrite and pyrite and in lesser amounts sphalerite, covellite -chalcocite,The fault fillings are concordant to the country rocks and have extensive alteration zones in wall - rock. Ore minerals of the fillings are pyrite, chalcopyrite, sphalerite and in supergene zones native copper and chalcocite - covelliteare present. The fault filling type mineralizations seem to be formed of the mobilized cations form the pillow lava mineralizations.

  • pillow lava

  • calcerous shale

  • bornite

  • Elazığ

  • Aktaş, G, and Robertson A. H. F., 1984, The Maden Complex, SE Turkey: Evolution of a Neotethyan active margin: J.E. Dixon and A.H.F. Robertson (Ed.). The Geological Evolution of the Eastern Mediteiranean, 375 - 402, Edinburgh.

  • Baştuğ, M.C., 1980, Sedimentation, deformation, and melange emplacement In the Lice basin, Dicle-Karabegan area, Southeast Turkey; ODTÜ, Ph. D. Thesis, 282 p. (Unpublished).

  • Borchert, H., 1958, Türkiye`de inisiyal ofiyolitik mağmatizmaya ait krom ve bakır cevheri yatakları: MTA yayınlan no. 102, Ankara.

  • Çağatay, A, 1977, Güneydoğu Anadolu bakır yatak ve zuhurlarının jeolojik - mineralojik etüdü sonunda elde edilen jenetik bulgular: MTA Dergisi, 89,46 - 74, Ankara.

  • Çağatay, N., 1979, Yeni gelişmelerin ışığında Türkiye`nin volkanik kökenli masif sülfit yatakları: Jeol. Müh. Odası yayını, 6,35 - 56.

  • Erdoğan, B., 1977, Geology, geochemistry and genesis of the sulfide deposits of the Ergani - Maden region, SE Turkey: Ph. D. Thesis, University of New Brunewick, 288 s, Kanada, (unpublished)

  • Erdoğan, B., 1982, Ergani - Maden yöresindeki Güneydoğu Anadolu Ofiyolit kuşağının Jeolojisi ve volkanik kayaları: TJK Bülteni, 25,1,49-60.

  • Evans, A.M., 1980, An introduction to ore geology: Blackwell Sc. Publication, Oxford, 231 p.

  • Heaton, T.H.E. and Sheppord, S.M.F., 1977, Hydrogen and oxygen isotope evidence for, Sewater complex, Cyprus.

  • Michard, A. Whitachurch, H., Ricou, L.E., Montigny, R. and Yazgan, E., 1984, Tauric Subduction (Malatya - Elazığ Provinces) and its bearing on tectonics of the Tetyan realm in Turkey: J.E. Dixson and A.H.F. robertson (Ed.), The geological Evolution of the Eastern Mediterranean, Edinburgh, 361 - 373.

  • Özçelik, M., 1985, Malatya Güneydoğusundaki Maden mağmatik kayaçlannın jeolojisi ve tektonik ortamına jeokimyasal bir yaklaşım: Türkiye Jeol. kur. Bült, 28,19-34.

  • Özkan, Y.Z. and Öztunalı, Ö., 1984, Petrology of the mağmatik rock of Guleman Ophiyolite; Procedings of the intern symp on the Geol of the Taurus Belt, 285 - 294, Ankara.

  • Özkaya, I., 1978, Ergani - Maden yöresi stratigrafisi: TJK Bülteni, 21,2,129-139.

  • Perinçek, D., 1979, The geology of Hazro - Korudağ - Çüngüş - Maden - Ergani - Elazığ - Malatya area: Guid Book, TJK yayını, 33 s., Ankara

  • Ramdohr, P., 1984, The Ore Minerals and Their intergrowths: Akademia - Verlog, Berlin, 1202 p.

  • Rigo de Righi, M.R. ve Cortesini, A., 1964, Gravity tektonics in foothills structure belt of southeast turkey: American Assoc, Petrol Geol. Bull., 48,1911-1937.

  • Soopner, E.T.C., 1977, Hydrodynamic model for the origin of the ophiolitic Cupriferous pyrite ore Cyprus.

  • Sungurlu, O., Perinçek, D., Kurt, G., Tuna, E., Dülger, S., Çelikdemir, E. ve Naz, H., 1984, Elazığ - Hazar - Palu alanının jeolojisi: TPAO dergisi, no. 29,83 -135, Ankara.

  • Şengör, A.M.C., 1980, Türkiyenin neotekniğinin esasları: TJK Konferans dizisi, 1.40 s., Ankara,

  • Tatar, Y., 1986, Elazığ çevresinde Fırat havzasının yapısal jeolojik özellikleri: Elazığ çevresinde Fırat havzasının jeolojisi ve yeraltı zenginlikleri sempozyumu, Bildiri özetleri, F.Ü. Müh. Fak. Jeoloji müh. Böl., 4 - 5., Elazığ.

  • Üstüntaş, A., 1988, Zahuran - Maden - Elazığ Piritik Cu Cevherleşmeleri: YQksek Lisans Tezi, F.Ü. Fen bilimleri Enş.y 58 s., Elazığ, (Yayınlanmamış).

  • Yazgan, E., 1981, Doğu Torolarda etkin bir paleo - kıta kenarı etüdü (Üst Kıetase - Orta Eosen) Malatya - Elazığ Doğu Anadolu: Yerbilimleri, Hacettepe Univ., 7,83 -104.

  • Tectonics of the Region Between Tercan (Erzincan) and Aşkale (Erzurum)
    Cevdet Bozkuş Özer Yilmaz
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    Abstract: Pre - Upper Maastrichtian is the first emplacement period of the ophiolitic melange which is the Neotethys product. During the interval of the Upper Cretaceous - Oligocene, ophiolitic malenge becamed thicker by thrusting due to the regional compressional tectonism and local emergence was an investigation area. Intermountain bassinsinfilled by continental elastics were developed in the early Oligocene, in front of the thrusts with approximately E-Wtrending and inclined to the North (Çayırlı - Tercan basin). Tectonic features of different character have developed during pre - and post - late Miocene, in the study area. E- W trending thrusts, high angle reverse - faults and asymetricoverturned folds with E-W trending axis have developed before Late Miocene. Following Late Miocene, compressionhas been compensated by lateral - movements which coused NW - SE, NE - SW striking right and left - lateral strikeslip faults and shear fractures with the same orientation. These structural data show that the investigation area and surroundings are under - control of appoximately N - S striking compressive stress. 

  • ophiolit

  • reverse - fault

  • Erzincan

  • Erzurum

  • Arpat, E., 1965, Ilıca - Aşkale (Erzurum) arasındaki sahanın ve kuzeyinin genel jeolojisi - petrol imkanları: M.T.A. Rap. No: 4040, Ankara.

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  • Some Remarks on the Article of Meriç and İnan titled "Cideina Soezerii (Sirel): Outcrops, Description, Lectotype - Paratypes and Discussion"
    Ercüment Sirel
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    Abstract: The genus Cideina Sirel is characterized by the presence of the orbitoidal lateral chambers on the dorsalside of the shell. Despite of the absence of these lateral chambers, a foraminiferal beast was described and figured as Cideina by Meriç ve İnan. Regarding that the comparisons materials of the authors is very probably a quite differentgenus, the discussion seems to be principally inconclusive. Because of the presence of the orbitoidal lateral chambers onthe dorsal side, Sirtina Bronnimann and Wirz was placed in Lepidorbitoididae by Loeblich and Tappan. Consideringnumerous structural similarities between Sirtina and Cideina, Sirel followed Loeblich and Tappan and placed the Anatolian genus Cideina also in Lepidorbitoididae. In the orginal description, however, Sirel clearly remarked that a distinct family name should be used for such types. These facts also seem to be completely ignored by the authors. On theother hand the name of the type species of Cideina, the terms of the lectotype and paratypes have been used wrong byMeriç ve İnan.

  • Lepidorbitoididae

  • foraminifera

  • orbitoidal

  • lectotype

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