Türkiye Jeoloji Bülteni
Türkiye Jeoloji Bülteni

Türkiye Jeoloji Bülteni

1999 AĞUSTOS Cilt 42 Sayı 2
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On Paleogeographical Distribution and Morphological Features of the Orhitoides gruenhachensis Papp in the Tethyan Ocean of Maastrichtian (Late Cretaceous)
İbrahim Engin Meriç Muhittin Görmüş
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Abstract: In this study, paleo geographical distribution and morphological features of Orbitoides gruenbachensis Papp in TethyanOcean is presented. The indicated species was found first time in Austria. The occurrence of Orbitoides gruenbachensis Pappin the Middle and Western parts of the Pontids and the northern part of the Helenid-Torid platforms indicates that thementioned species lived in a restricted area and preferred a shallow paleoenvironment having low salinity and temperature.Besides, its appearance in the Maastrichtian deposits both A ustria and Turkey also shows that its range has a resticted time.

  • Maastrichtian

  • Orbitoides gruenbachensis Papp

  • Paleo geography

  • Tethyan Ocean

  • Biju-Duval, Dercort, J. ve le Pichon, X., 1977. From the Tethlys Ocean to the Mediterranean seas: a plate tectonic model of the evolution of the Western Alpine System. Technip, 143-164.

  • Caus, E., Bernaus, J.M. ve Gomez-Garrido, A., 1996. Biostratigraphic utility of species of the genus Orbitoides. Journal of Foraminiferal Research, 26 (2), 124-136, Lawrence, Kansas.

  • Drooger, C. W. ve de Klerk, J.C., 1985. The punctuation in the evolution of Orbitoides in the Campaiiian of South-west France. Utrecht Micropaleontological Bulletins, 33, 143p. 5pl. 62 text-figs, Netherlands.

  • Ersoy, Ş., 1989. Fethiye (Muğla)-Gölhisar (Burdur) arasında Güney Dağı ile Kelebek Dağ ve dolaylarının jeolojisi. Doktora tezi, İstanbul Üniversitesi Fen Bilimleri Enstitüsü, 246s.

  • Görsel, J. T. van, 1978. Late Cretaceous orbitoidal foraminifera. In : Foraminifera (eds, Hedley, R. H. and Adams, C. G.) Academic press, 1-120, London.

  • Görmüş, M., 1992. Quantitative Data on the Relationship between the Orbitoides genus and its Environment. Revista Espanola de Micropaleontologia, XXIV (3), 13-26, Madrid.

  • Görmüş, M. 1996-1997. Osmaneli (Bilecik) yöresindeki Orbitoides`lerde fosilleşme ve mikroiz aktivite. İstanbul Üniversitesi Yerbilimleri, 10. Sayı, 47-58, İstanbul.

  • Görmüş, M. 1997a. Osmaneli (Bilecik) yöresindeki Orbitoides`lerin biyometrik incelemesinin ön bulguları. Çukurova Üniversitesi Jeoloji Mühendisliği Eğitiminin 20. Yılı Sempozyumu, Çukurova Üniversitesi, Geosound-Yerbilimleri, Cilt 1, 30, 151- 174, Adana

  • Görmüş, M., 1997b. Türkiye`den örneklerle Orbitoides parametreleri ve bunlarm zaman-mekan içerisindeki değişimi üzerine bir tartışma. Türkiye Jeoloji Bülteni, 41(1), 85-98, Ankara.

  • Görmüş, M. ve Sagular, E. K., 1998. Microboring activity in Orbitoides accumulations from Turkey, Journal of Isreal Earth Science, 47, 61-67, Isreal.

  • Hinte, J.E. van, 1976. Cretaceous time scale. Bulletin of American Association Petroleum Geology, 60(4), 498-516, Chicago.

  • Meriç, E., 1967. Sur quelques Loftusiidae et Orbitoididae de la Turquie. Publication of the University of Istanbul, Faculty of Sciences, B, 32(1-2), 1-58, İstanbul.

  • Meriç, E., 1974. Sur la presence du genre Loflusia aux environs de Gönyük (Bolu, Nord-Quest d ela Turquie). Publication of the Universitiy of İstanbul, Faculty of Sciences, B, 39(3-4), 227-232, İstanbul.

  • Meriç, E., Ersoy, Ş. ve Görmüş, M., 1999. Loftusia (foramınifer) türlerinin Maastrihtiyen (Geç Kretase) Tetis Okyanusu `ndaki paleocoğrafik yayılımı üzerine yeni görüşler, Hacettepe Üniversitesi Yerbilimleri Dergisi, 22 (basımda), Ankara.

  • Neumann, M. 1978. Le genre Orbitoides Reflexion sur les especes primitives attribuees a ce genre. Revue de Micropaleontologie, 29(4), 220-261, Paris.

  • Papp, A., 1955. Orbitoides aus der oberkreide der Ostalpen (Gosausbhichten). Sitzber. Osterr. Akad, wissensc, Math.-Naturw., K1(I), 164, 303-315.

  • Robertson, A. H. F., 1990. Microplate tectonics and evolution of the Mesozoic-Tertiary İsparta Angle, SW Turkey, IESCA, 1990, International Earth Science Congress on Eagean Regions, l-6#th Oct. 1990, İzmir, Turkey.

  • Robertson, A. H. F., 1993. Mesozoic-Tertiary sediments and tectonic evolution of Neotetyan carbonate platforms, margins and small oceon basins in the Antalya Complex, Southwest Turkey. Spec. Publs. Int. Ass. Sediment., 20, 415-465.

  • Salaj, J. ve Samuel, O., 1966. Foraminifera der Westkarpaten-Kreide (Slowakei), 390s., Bratislava.

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

  • A New Orbitoidal Foraminiferal Genus From The Maastrichtian of Şereflikoçhisar
    İbrahim Engin Meriç Nurdan İnan Turan
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    Abstract: In this study, a few individuals of probably a new orbitoidal foraminiferal genus, conic flabelliforme in shape, havinghyaline calcareous wall as well as in the same wall of the concave side of the Sivasella genus and including similarchamberlets to the equatorial chambers of the Ilgazina genus are described.

  • now. Gen.

  • Middle Maastrichtian

  • Şereflikoçhisar

  • Turkey

  • Erdoğan, K., 1995. Yeni bir orbitoidal foraminifer cins ve türü: llgazina unilateralis n.gen., n. sp. Türkiye Jeoloji Bülteni, 38(1) 11-23,.

  • Loebh, A. R. Jr. ve Tappan, H., 1988. Foraminiferal genera and their classification: Van Nostrand Reinhold Company, New York, 2 volumes, 970p. Plus 222p. 847pl.

  • Özer, S., 1983. Les formations a rudistes du Senomanien superieur d`Anatolie Centrale (Turquie). Trav. Lab. Stra. Paleoecologie, Univ. Provence, Nouvelle Serie, 1, 32p., Marseille.

  • Özer, S. 1985. İç Anadolu Bölgesi rudist paleontolojisi ve paleobiyocoğrafyası. Doktora tezi, DEÜ, 183p. İzmir

  • Özer, S., 1988. Orta-Doğu-Güneydoğu Anadolu ve Kocaeli Yanmadası`nda bulunan Pironea (rudist) türlerinin paleontolojisi ve biyocoğrafyası. Türkiye Jeoloji Kurumu Bülteni, 31 (1), 47-58.

  • Sirel, E. ve Gündüz, H., 1978. Description of Sivasella n.gen. (Foraminifera) from the Maastrichtian of Sivas (Central Turkey). Türkiye Jeoloji Kurumu Bülteni, 21 (1), 67-7.

  • The Geology of the Çolaklı (Harput - Elazığ) Vein Type Pb-Zn Mineralizations
    Ahmet Şaşmaz Ahmet Sağiroğlu
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    Abstract: Çolaklı-Elazığ mineralizations occur as vein type fillings in the fracture zones of diorite rocks of Coniacian-Camp onionElazığ magmatites. The veins strike N10-6Ö* W and dip vertically. They extend between 250-800 meters and their thicknessesvary between 0.5-3.5 meters on the surface. The ore mineral assemblage of the veins are galena, freibergite, pyrite, cubanite,chalcopyrite, tetralxedrite, barytine and secondaiy minerals derived there. The ore is massive or disseminated within thecarbonate minerals and quartz. The chemical analysis give high Pb, Ag, Zn andSb values. Ag takes places in the structure offreibergite which itself occurs always as enclosed in galena This is well demonstrated by high A g-Pb, Cu-Sb and A g-Sbvalues (r=0.82, r=0.73 and r=0.86 resprectively).Çolaklı mineralization appears to be fowned by the late phase magmatic solutions originated from granitic intrusionswhich followed the deformation and fractiuing of the dioritic rocks. This model is supported by the presence of aplite andquartz- filled veins within the ore veins.

  • Elazığ magmatites

  • Fmibergite

  • Pb-Ag mineralization

  • Akgül, B., 1993, Piran Köyü çevresindeki mağmatik kayaçlarm petrografik ve petrolojik özellikleri, Fırat Üniversitesi Fen Bilimleri Enstitüsü, Doktora Tezi, 128s. Elazığ (yayınlanmamış).

  • Akgül, B. ve Saymaz, A., 1996, Elazığ kuzeyinde pirometasomatik oluşuklar ve ilişkili Fe-Ti cevherleşmeleri, Türkiye Jeoloji Bülteni, C. 39, S.2, 39- 49.

  • Aksoy, E., 1994, Pertek çevresinin jeolojik özellikleri ve Bindirme fayı. Fırat Üniversitesi Fen ve Mühendislik Bilimleri Dergisi, Sayı, 6/2, 1-18 Elazığ.

  • Aktaş G. ve Robertson, A. H. F., 1984, The Maden Complex, S. E. Turkey: Evolution of a Neo Tethyan active margin, Geology Society of London Special Publication, 17, 372-402.

  • Altunbey, M., 1996, Tuzbaşı-Kanatburun-Ayazpmarı (Pertek-Tunceli) yöresindeki demir cevherleşmelerinin jeolojisi ve kökeni, Fırat Üniversitesi Fen Bilimleri Enstitüsü, Doktora Tezi, 186 s. Elazığ (Yayınlanmamış).

  • Asutay, H. J., 1985. Baskil (Elazığ) çevresinin jeolojik ve petrografik incelenmesi, Ankara Üniversitesi Fen Bilimleri Enstitüsü, Doktora Tezi, 176 s., Ankara, (Yayımlanmamış).

  • Avşar. N., 1983, Elazığ yakın kuzeybatısında stratigrafîk ve mikropaleontolojik araştırmalar, Fırat Üniversitesi Fen Bilimleri Enstitüsü, Doktora Tezi, 84 s, Elazığ (Yayınlanmamış).

  • Bingöl, A.F., 1984, Geology of the Elazığ area in the Eastern Taurus region, Int. Symp. the Geology of the Taurus Belt, Proceedings, 209-216.

  • İnceöz, M., 1995, Harput (Elazığ) yakın kuzeyi ve doğusunun tektonik özellikleri, Fırat Üniversitesi Fen Bilimleri Enstitüsü, Doktora Tezi, 112 s., Elazığ (Yayımlanmamış).

  • Naz, H., 1979, Elazığ-Palu dolayının jeolojisi, TPAO rapor no: 1360, (Yayınlanmamış).

  • Sağıroğlu, A., 1986, Kızıldağ (Elazığ) cevherleşmelerinin özellikleri ve kökeni, Jeoloji Mühendisliği Dergisi, 29, 5-13.

  • Sağıroğlu, A. ve Preston, R. M. F., 1987, Ore Mineralogy of Kızıldağ Pb-Zn veins-with a special emphasis on the composition of the tetrahedrites, Journal of Fırat University, V. 2, 83-94.

  • Hydrogeochemical Characteristics and Vulnerability to Contamination of the Diyarbakır A quifers
    Gültekin Tarcan Şevki Filiz Ünsal Gemici Ubeyd Sezer
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    Abstract: This study contains the hydro geological and hydrogecohemical investigations carried out in Diyarbakır and surrounding area. Mardin formation, which is the oldest unit in the field, forms the reservoir of the oil and its production water. The overlying Gercüş formation is aquiclude, and Midyat, Germik, Şelmo formations and basalt unit are aquifers. There are anumber of contaminant sources for both surface water and groudwater in the field. Particularly, reinjection of the productionwater, extracted from the Mardin formation, to the Midyat formation that consists of karstic limestone, instead of Mardin formation, (which is the reservoir of the production water) creates a high risk for the Diyarbakır City potable water. The hydmgeochemical properties and vulnerability to contamination of the aquifers in the study area are discussed.

  • Diyarbakır

  • Hydwgeochemistry

  • Hydrogeology

  • Vulnerability to contamination

  • APHA-AWWA-WPCF, 1975, Standart methods for examination of water and waste water. Fourteenth edition, copyright by American Public Health Association, Washington D.C., 1993s.

  • Başkan, H. E. ve Canik, B., 1983, IAH Map of mineral and thermal waters of Turkey Aegean Region. MTA no. 189, Ankara, 80 s.

  • Çamur, M. Z., 1996, Doğal salamura sularda mineral çökelim ve çözünümünün termodinamik değerlendirimi için bilgisayar programı. Jeoloji Mühendisliği Dergisi, Sayı :48, 40-56.

  • DSİ, 1979, Yukarı Dicle Havzası hidrojeolojik etüt raporu. Devlet Su İşleri Genel Müdürlüğü Jeoteknik ve Yeraltı suları Dairesi Başkanlığı, Ankara, 113 s.

  • DSİ, 1994 Devlet Su İşleri, X. Bölge Müdürlüğü, 1994 Yılı Programı takdim raporu. 3, 47-48.

  • DSİ, 1996, Devlet Su İşleri X. Bölge Müdürlüğü sondaj kuyu verileri ve kimyasal analizler Diyarbakır (Yayınlanmamış).

  • Fetter, C. W., 1994, Applied Hydrogeology. Third Edition University of Wisconsin-Oshkosh. Macmillian College Publishing Company, NewYork, 691 s.

  • Ford, D. C. ve Williams, P. W., 1989, Greenpeace Mediterranean basın duyurusu, 26 Mart 1996, Istanbul.

  • Resmi Gazete, 1988, Su kalitesine ilişkin planlama esasları ve yasaklar. 4 Eylül 1988, Sayı : 19, Bölüm . 4 Madde : 16-20, 22-24.

  • Sulin, 1946, Suların jenetik sınıflaması ve petrol yataklarından gelen suların kimyasal özellikleri, in.

  • Şahinci, A., 1991, Doğal Suların Jeokimyası. Reform Matbaası, Beyler-İzmir, 548 s.

  • Tarcan, G., 1989, Urla-İçmeler ve çevresinin jeolojikhidrojeolojik incelenmesi, sıcak-soğuk suların jeokimyasal yorumlanması. Dokuz Eylül Üniversitesi Fen Bilimleri Enstitüsü, Yüksek Lisans Tezi, İzmir.

  • TS-266, 1970, İçme Suları Türk Standartları, UDK 663.7.543, 32 s.

  • Formation features and engineering properties of the clays produced from the weathering of the andesites in Izmir and vicinity
    Mehmet Yalçin Koca
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    Abstract: A ndesitic volcanic rocks and their weathering products "clays" are highly widespread around İzmir. The materialproperties of andesites vary with their weathering grades. Smectite type clay minerals are formed in moderately andcompletely weathered andesites. The clays formed as a result of weathering are determired to have formed in two waysduring the field observations. First, the andesitic lava alters the previously flown and partially solidified andesitic lava and aresiduel clay is formed. Secondly, the andesite is weathered by groundwater circulation through the discontinuities and byatmospheric factors, produce clay and silt. The smectite type clays formed as a weathering product, swell by taking water in their structure and developed instabilities controlling by the discontinuities. This may cause slope failures even at gentleslopes along the clay-filled cooling joints.In this paper, the geomechanic test results of the clay s formed from weathering of the andesite taken from Susuzdede Park,Osmangazi, Asansör Quarry and the Nenehatun Shaft of the İzmir Metro, are presented and the influence of such soil types onthe stability of the abondoned quarries and road slopes, are discussed.

  • Andesite

  • clay

  • shear strenght

  • stereo graphic projection technique

  • weathering

  • Akartuna, M., 1962, On the geology öf İzmir, Torbalı, Seferihisar, Urla districts. MTA Bull. No. 5, 1-19.

  • ASTM, 1971, Standard Test Method for Plastic Limit and Plasticity Index of Soil. D. 424-59, 127-128.

  • ASTM, 1972a, Standard Test Method for Particle-Size Analysis of Soils. D. 422-63, 112-114.

  • ASTM, 1972b, Standart Test Method for Liquid Limit of Soils. D. 423-66, 123-126.

  • ASTM, 1979, Standard Test Method for Direct Shear Test of Soils Under Consolidated Drained Conditions. D. 3080-72,487-497.

  • ASTM, 1979, Standard Test Method for Unconfined Compressive Strength of Cohesive Soils. D. 2166- 66, 332-335.

  • Brown, G., 1961, The X-Ray Identification and Crystal Structures of Clay Minerals. Mineralogy Society, London, 544.

  • Kmcal, C, 1996, Yeşilyurt (İzmir) Tünel Şaftının Mühendislik Jeolojisi, Dokuz Eylül Üniversitesi, Bitirme Projesi, İzmir, 64s.

  • Koca, M. Y, 1995, Slope Stability Assesment of the Abandoned Andesite Quarries in and Around the İzmir City Centre. PhD. Thesis. Dokuz Eylül University Graduate School of Natural and Applied Sciences. 430 p (unpublished).

  • Koca, M. Y., ve Aydan, Ö., 1996, Andezitlerdeki süreksizliklerin pürüzlülük ölçümleri. 3. Ulusal Kaya Mekaniği Sempozyumu. Ankara, 101-112.

  • Landanyi, H. K., ve Archambault, G., 1977, Shear strength and deformability of filled indented joints. Proc. 1st International Symposium Geotechnically Structural Complex Formations, Capri, Italy, vol. 2, 317-236.

  • Means, R. E., ve Parcher, J. W., 1963. Physical Properties of Soils. Charles E. Merril Publ. Compt., Columbia, Ohio, 467 pp.

  • Philllippson, A., 1911, Reisen und Forschungen Westlichen Kleinasien. Peterm. Mitt. Ergaenz. 172. Gotha.

  • TS 1901, 1975, İnşaat Mühendisliğinde Sondaj Yolları ile Örselenmiş ve Örselenmemiş Numune Alma Yöntemleri. UDK 622.233: 624.131.36.

  • Velde, B., 1994, Origin and Mineralogy of Clays. Oxford University Press, Inc. New York. 103-105

  • Organic Geochemical Characteristics of the Miocene Yazır Limestones in the Southern İsparta
    Mehmet Altunsoy
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    Abstract: The aim of this study is to indicate the organic geochemical characteristics of the Lower Miocene limestones. The Yazırformation contains various lithological and biofacies deposits. These are, from bottom to top, the coarse grained elastics,clayey limestones with laminated algae and miliolid, thick bedded limestones with algae and corals, clayey to sandylimestones with benthic foraminiferaThe total organic carbon content of Yazır formation is poor, but in some levels, it seems to be rich. Rare hydrocarbonoccurrences are also seen in these sections. Samples are derived from the marine organic matters (amorphous) in general.Vitrinite reflectance values range between %0.12-0.44. When these data is considered, the Yazır formation is thought to be ina diagenesis stage. When all the data are evaluated together, the Yazır formation can be regarded as a source rock for oil atsome levels. Organic geochemical and microscopic data show B organic facies according to Jones (1987) and Baskin (1997)classifications.

  • West Taurus

  • Southern İsparta

  • organic petrography

  • Yazır formation

  • Akay, E., Uysal S., Poisson, A., Cravatte, J., ve Muller, C, 1985, Antalya Neojen Havzasının stratigrafisi: TJKBült.,28, 105-119.

  • Akbulut, A., 1980, Eğirdir gölü güneyinde Çandır (Sütçü ler-Isparta) yöresindeki Batı Torosların jeolojisi: TJKBült., 23,1,1-9.

  • Baskin, D. K., 1997, Atomic H/C ratio of kerogen as an estimate of thermal maturity and organic matter conversion: AAPG Bull, 81,9,1437-1450.

  • Espitalie, J.M., Madec, M., ve Tissot, B.,1980, Role of mineral matrix in kerogen pyrolysis: influence on petroleum generation and migration: AAPG Bull., 64, 59-66.

  • Görmüş, M., ve Özkul, M., 1995, Gönen-Atabey (Isparta)-Ağlasun (Burdur) arasındaki bölgenin stratigrafisi: SDÜ, Fen Bilimleri Ens. Derg., 1, 43-64.

  • Görmüş, ve Hançer, M., 1997, Dereboğazı (İsparta Güneyi) dolaylarındaki Alt Miyosen çökellerinin fasiyes özellikleri: SDÜ Fen Bilimleri Ens. Derg., 2, 39-50.

  • Gutnic, M., Monod, O., Poisson, A., ve Dumont, J.F., 1979, Geologie des Taurides occidentales (Turquie): Mem. Soc. Geol. France, 137, 1-112.

  • İlleez, H.İ., Harput, A., ve Gül, M. A., 1992, Üç Yıldız (İsparta) petrol sızıntısının organik jeokimyası: Türkiye 9. Petrol Kongresi ve Sergisi, Bildiriler, 1- 7.

  • Jones, R.W., 1987, Organic Facies. In: Advances in Petroleum Geochemistry: v.2, p. 1-91. Karaman, M.E., 1988, Ege-Anadolu levha sınırı hakkında bazı yeni görüşler: H.Ü., Yerbiliminin 20. Yılı Sempozyumu, Bildiri özleri, s. 15.

  • Kazancı, N., ve Karaman, M. E., 1988, Gölcük (İsparta) Pliyosen volkaniklastiklerinin sedimanter özellikleri ve depolanma mekanizmaları: Akdeniz Üniv. İsparta Müh. Fak. Derg., 4, 16-35.

  • Karaman, M.E., 1990, İsparta güneyinin temel jeolojik özellikleri: Türkiye Jeoloji Bülteni, 33, 51-61.

  • Monod, O., 1977, Recherces geologiques dans le Taurus occidental am sud de Beyşehir (Turquie): These d`etat, FUniv, de Paris Sud, Orsay, 442p.

  • Özgül, N., 1984, Stratigraphy and Tectonic evolution of the Central Taurides: In Geology of the Taurus Belt, Int. Symp. (Tekeli, O., ve Göncüoğlu, M.C., Eds.,) p. 77-99.

  • Peters, K.E., 1986, Guidelines for evaluating petroleum source rock using programmed pyrolysis: AAPG Bull., 70, 318-329.

  • Poisson, A., ve Poignant, A.F., 1974, Korkuteli Bölgesindeki Miyosen transgresyonunun tabanı olan Karabayır formasyonu, Karabayır formasyonunun yeni bir kırmızı alg türü: Lithothamnium pseadoramossissimum: MTA Derg., 82,65-69.

  • Poisson, A., 1977, Recherches geologuqe dans les Taurides occidentales (Turque): These Doc. Sci., Üniv. Paris-Sud, Orsay, 1-795.

  • Poisson, A., Akay, E., Dumont, J. F., ve Uysal, S., 1984, The İsparta angle In: Geology of the Taurus Belt Int. Symp (Tekeli, O., ve Göncüoğlu, M.C., Eds.) 11-16.

  • Powell, T.G., Creaney, S., ve Snowon, L. R., 1982, Limitations of use of organic petrographic techniques for identification of petroleum source rocks: AAPG Bull., 66, 4, 430-435.

  • Sonel, N., Sarı, A., Doğan, A. O., ve Bozüyük, 1., 1995, Üzümlü (Beyşehir) civarının petrol kaynak kaya fasiyesleri ve petrol oluşumunun organik jeokimyasal yöntemlerle incelenmesi: TJK Bült., 10, 34-40.

  • Staplin, F.L., 1975, Interpretation of thermal history from colour of particulate organic matter: Palynology, 1, 9-18.

  • Şenel, M., 1997, 1/250.000 ölçekli Türkiye Jeoloji Haritaları, İsparta Paftası: MTA Ens., Ankara, No: 4

  • Tissot, B., ve Welte, D., 1978, Petroleum Formation and Occurrence: Springer-Verlag, Berlin, 535p.

  • Tissot, B., ve Welte, D., 1984, Petroleum Formation and Occurrence: Revised edition, Springer Verlag, New York, 699p.

  • Yağmurlu, F., Tutaş, M., ve Keçeli, A., 1990, Eğirdir (İsparta) güneyinde yer alan asfaltit ve sıvı petrol emarelerinin jeolojik konumu: Türkiye 8. Petrol Kongresi, Bildiriler, 24-34.

  • Yağmurlu, F., 1994, İsparta güneyinde yer alan Tersiyer yaşlı türbiditik birimlerin fasiyes özellikleri: Geosound, 24, 17-28.

  • Yalçınkaya, S., Ergin, A., Afşar, Ö.P., ve Taner, K., 1985, İsparta büklümünün yapısal evrimi: 3. Mühendislik Haftası Bildiri özleri, 30-31.

  • Yalçınkaya S., 1989, İsparta-Ağlasun (Burdur) dolaylarının jeolojisi: İ.Ü. Fen Bilimleri Ens. Doktora Tezi, 176 s (Yayınlanmamış).

  • Conformable Benthic K/T Transition in Eastern Pontides : Şahinkaya Member of the Tonya Formation (SW Trabzon)
    Nurdan İnan Turan Selim İnan İskender Kurt
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    Abstract: Şahinkaya Member, represented by reefal limestone, of Tonya Formation is first defined as Maastrihtian-Danian aged by Korkmaz (1983). Korkmaz1 s (1983) type locality for Şahinkaya Member was not standardized. Thus, Çalköy section is chosenfor a representative type locality in this study The bottom of Şahinkaya Member is constituted by nidist- bearing biosparite,which contains Orbitoides apiculatus Schlumberger and Siderolites calcitrapoides Lamarck. The same lithology is continuingwith miliolidea, algea bryzoa-bearing intraclast sparites and passing through Caskinolina sp., Gyroidina, sp., Gyroidina sp. Anomalina sp., miliolidea, algea and bryozoa-b earing algal biosparites. At the top level section, algea-bearing biospantescontains Idalina sinjarica Grimsdale, Miscellanea sp., algae, biyzoa, annelid tubes, echinoid spine and crinoids. This facie slocally contains iron-bearing sandy limestone beds. At the top level of this unit is consisting of Discocyclina seunesi Douville. The fossil fauna above indicate that the age of Şahinkaya Member is Maastrihtian-Thanetian. K/T transition in the Eastern Pontides with benthic fauna is first defined in this study. 

  • Benthic foraminifera

  • Eastern Pontides

  • SW Trabzon

  • K/T transition

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  • The Bolkar Mountains (Central Taurides, Turkey): A Neogene Extensional Thermal Uplift?
    Damien Dhont Jean Chorowicz Tekin Yürür
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    Abstract: This paper concerns the neotectonics of the Bolkar Mountains, belonging to the Central Taurides in Southern CentralAnatolia. The study is based on observations on Synthetic Aperture Radar (SAR) scenes of the European Remote Sensing(ERS) satellite and Digital Elevation Model (DEM images, complemented with field structural analysis. Il is revealed thatextensional tectonics prevails in the area during the Neogene. In the northern sector, movements trend west and are attributedto the westward escape of Anatolia towards the Aegean basin. Further south, movements turn progressively to the southwestthen south and are related to the opening of the Adana-Cilicia basin probably as early as the Late Oligocene-Early Miocene.More importantly, uplift of the Bolkar Mountains occured in the Neogene coeval with this extension. The belt is interpreted asthe northern uplifted shoulder of the Adana-Cilicia basin, due to thermal effects of Neogene lithospheric stretching and thinning. This is the consequence of the inception of a backward and downward retreat of the African subducting slab beneathCyprus in the Late Oligocene-Early Miocene, which has resulted in a wide extension in the overriding plate. Transition between high elevations in the Central Taurides and deep bathymetry in the Cilicia basin suggests that gravitational forces mayalso contribute to the extension during the Neogene-Quaternary. 

  • Central Taurides

  • Neotectonics

  • Stress

  • Strain

  • Slab retreat

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  • Minamiite and Alunite Occurrences Formed From Volcanic Emanations, West-Southwest of Konya, Turkey
    Muazzez Çelik Karakaya
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    Abstract: Aluminum sulfate minerals, kaolin and bentonitic clay deposits and zeolites occur within upper Miocene-Pliocene high-Kandesitic-dacitic volcanic rocks and lacustrine sediments in the west southwest of Konya, Turkey. In the area, post-volcanic phenomena, such as solfatara activity, has already been continued.The samples taken from the study area were mineralogically and chemically examined using XRD, SEM-EDS, XRF,AAS, DTA-TG and microprobe instruments. As a result of this investigation, it has been determined that alteration mineralsformed by early-and/or post volcanic acid solutions reacted with the solutions were highly acidic in character, alunite and natroalunite were produced by the alteration of mainly dacitic volcanic rocks, while minamiite was formed by the alteration ofandesitic volcanic rocks. However, acidic or weakly acidic solutions yielded kaolinite and/or halloysite and illite.Alunite group minerals are K, Na and Ca sulfate with formula (Ca, Na, K) A13(SO4) 2 (OH) 6 and mainly form as hydrothermal minerals in the study area. Nearly pure minamiite and alunite have been found in a few samples. They are commonly associated with silica polymorphs, kaolinite and halloysite in various parts of the study area.Stability relations of minerals in the advanced argillic alteration zone indicate alteration took place under acidic conditionsin the near-surface environment. Mineralogical and textural evidence also suggests alteration occurred in steam-heated environment, rather in a supergene or magmatic hydrothermal origin.

  • Alunite

  • halloysite

  • kaolinite

  • Konya

  • minamiite

  • Turkey

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  • Temel, A. Gündoğdu, N.M. and Gourgaund, A., 1998. Petrological and geochemical characteristics of Cenozoit high-K calc-alkaline volcanism in Konya, Central Anatolia, Turkey, journal of Volcanology and Geothermal Research, 85, 327-354.

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  • Late Early Miocene and Quaternary small mammals in the surroundings of Söke (Aydm): Preliminary results
    Engin Ünay Fikret Göktaş
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    Abstract: The Late Cenozoic sediments in the surroundings of Söke are assigned to the Late Early Miocene and Quaternary on thebasis of small mammals from the Söke, Dededağ and Savulca formations. The Söke fauna from the Söke Formation and theDededağ fauna from the Dededağ Formation are correlated with the Orleanian (Late Early Miocene) and theMN4 mammalzone. The Kemalpaşa Mahallesi-I and the Kemalpaşa Mahallesi-II faunules from the Savulca Formation suggest EarlyBiharian (Early Pleistocene) and Toringian (Middle-Late Pleistocene) ages, respectively. The Burçaktepe fauna indicates aLate Early Biharian-Recent age. In the Söke fauna, a new species-A Ibertona aegeensis-is described.

  • Biochronology

  • Late Early Miocene

  • Quaternary

  • Small mammals

  • Söke (Aydın)

  • Becker-Platen ve Löhnert, E., 1972. Über Cardium Funde aus dem Kaenozoikum der Umgebung von söke (West Türkei): Geol. Jb., B2, 55-63.

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  • Klein Hofmeijer, G. ve De Bruijn. EL, 1988. The mammals from the Lower Miocene of Ali veri (Island of Evia, Greece). Part 8: The Cricetidae. Kon. Ned. Akad. Wetensch. Proc. B, 91 (2), 185- 204.

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  • Başnayayla (Yozgat) Molybdenum-Copper Mineralization
    Ercan Kuşcu Yurdal Genç
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    Abstract: Başnayayla molybdenum-copper mineralization is related to granitic rocks ofPaleocene age (?) which are located on thenorthern edge of the Central Anotalian Crystalline Complex and Kırşehir Massif, approximately 15 km southwest of Yozgat district The rock units around the mineralization are; Kamışcıdere gabbro, Başnayayla granitoid, Beşiktepe volkanosedimentary series and alluvium. Başnayayla granitoid consists of biotite granite, microcline granite, andalusite-sillimanitegranite ve two mica granite together with felsic dikes. Kamışcıdere gabbro and Başnayayla granitoid are cut by felsic andmafic veins. Molybdenum-copper mineralization is hosted by biotit granite, andalusite-sillimanite granite and two mica granite with cordierite granite, aplite granite and quartz veins of the Başnayayla granitoid surrounded by Kamışcıdere gabbro andBeşiktepe volkano-sedimentary series Molybdenum mineralizations are occured as molybdenite-bearing quartz veins/veinlets, coatings in joints and cracks and,disseminations in the host rock. Main ore minerals are molybdenite, pyrite, chalcopyrite and magnetite. Cubanite, pyrrhotite,sphalerite, galena, ilmenite, bornite and bismuthinite are also encountered in traces. Limonite, hematite, marcasite, chalcociteand covellite are occured as secondary minerals. Three types of alterations related to the mineralization were determined andthese are quartz+s e ricite+py rite, quartz+feldspar+biotite and quartz+feldspar+biotite+sericite/muskovite associations. Molybdenum mineralization is generally seen between quartz+sericite+pyrite and quartz+feldspar+biotite alteration zones andwithin quartz+feldspar+biotite alteration zone.The mineralizations my be defined as low-grade porphyry and/or stockwork molybdenum-copper type when the ore types,mineralogy and alteration properties are taken in account. Başnayayla granitoid which involves Başnayayla porphyry and stockwork molybdenum-copper mineralization posseses the different properties than those of the host rocks mentioned in theliterature from the points of origin and geotectonic environments. On the basis of mineralogical, petrographical andgeochemical data, although it has the properties of 1- and S-type granites, the properties of the S-type is dominant in theBaşnayayla granitoid. From the geotectonic environments point of view, the Başnayayla granitoid possesses the features of thesy n-co His ional granites.

  • Başnayayla granitoid

  • Kırşehir Massif

  • Molybdenum-Copper

  • Central Anatolian Crystalline Complex

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