Türkiye Jeoloji Bülteni
Türkiye Jeoloji Bülteni

Türkiye Jeoloji Bülteni

1971 EYLÜL Cilt 14 Sayı 2
COVER
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CONTENTS
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Über Verwendungsmöglichkeiten Des Zinkblende Pyrrhotinmischkristalls Als Geologisches Thermometer
Osman Özcan Dora
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Abstract: Zunächst werden kurz die Untersuchungsmethoden erwähnt unddann die physikalisch-chemischen Entstehungsbedingungender untersuchten natürlichen Vorkommen nach petrologischenGesichtspunkten festgestellt. Nach der begleitenden Diopsid-Wollastonit-Andradifazies ist anzunehmen, dass das kontakt - metasomatische Zinkblendevor- kommen von Bağırkaç(im Eybek Granodioritmassiv) bei 500 bis 1000 Bar Druck und400° bis 500°C Temperatur entstanden ist. Dagegen rechtfertigen die spektroskopischen Analysen des Karakoca - Vorkommens (im Eğrigöz - Karakoca Granit- massiv) einen hydrothermalen Entstehungsbereich bei 100 bis 200 Bar Druck und 200°bis 300°C Temperatur.Weiter wurden die Pyrrhotingehalte und die Gitterkonstanten derZinkblendemischkristalle auf die Apsis - und Ordinatenachseneines Koordinatensystems aufgetragen und die Zusammenhänge diskutiert. Es konnte gezeigt werden, dass in den natürlichenZinkblendemischkristallen das VEGARD - Gesetz bis 10 % FeSGehalt gilt.Schliesslich wurden die analytischen Daten in die, aus den Literatür übernommenen Synthesediagramme eintgetragen undVergleiche gezogen. Es wurde gezeigt, dass die Ablesung derBildungstemperatur allein aus dem FeS - Gehalt der Zinkblende nicht möglich ist. İn übereinstimmenden Fällen kann dieserals Wegweiser dienen. Wie auch aus den Ietzten Synthesediagrammen hervortritt, nimmt der FeS-Gehalt derZink-blende mit abnehmender Temperatur zu. DieseFeststellung steht mit den älteren Anschauungen imW i d e rspruch.

  • Zinkblende Pyrrhotin Mischkristalls

  • einen hydrothermalen

  • Eğrigöz - Karakoca Granit- massiv

  • Arnold, R. G. (1962) : Equilibrium relations between pyrrhotite and pyrite from 325° to 743°C. — Econ. Geol. 75, 72 - 90.

  • Aslaner, M. (1965) : Etüde géologique et pétrographique de la region d’Edremit - Havran (Turquie). — Pub. d. L’Ins. d’Etud. et d. Rech. Min. d. Turc., No. 119, 1 - 98, Ankara.

  • Barton, B. P. Jr. & Toulmin, P. III (1964 a) : The electrum - tarnish method for the determination of the fugacity of sulfur in laboratory sulfide systems. Geochim. et Cosmochim. Acta., V. 28, 619 - 640.

  • Barton, B. P. Jr. & Toulmin, P. III (1964 b) : Experimental determination of the reaction chalcopyrite + sulfur = pyrite + bornite from 350 to 500°C. - Econ. Geol. , V. 59, 747 - 752.

  • Barton, B. P. Jr. & Toulmin, P. III (1966) : Phase relations involving sphalerite in the Fe - Zn - S System. Econ Geol., V. 61, 815 - 848.

  • Brinkmann, R. (1971) : Die Südflanke des Menderes - Massivs bei Milas, Bodrum und Ören. Scien Rep. of the Fac. of Scien. Ege Uni. No..43, İzmir

  • Chernyshev, L. V. & Anfilogov, V. N. (1967) : Experimental data on the composition of sphalerite in association with pyrrhotite and pyrite at temperatures of 350° to 500°C. - Doklady, V. 176, 209 - 211.

  • Dora, O. Ö. (1969 a) : Karakoca Granit Masifinde Petrolojik ve Metallojenik etüdler. MTA, Mecmuası, Nr. 73, 10-26. Ankara.

  • Dora, O. Ö. (1969 b) : Kontakt metasomatik Pb - Zn yataklarında Çinkoblend - Pirotit ve Granat karışım kristallerinin jeolojik termometre olarak kullanılması. TÜBİTAK II Bilim Kongresi, Yer Bilimleri Seksiyonu, (Özet, 68-69), Ankara.

  • Dora, O. Ö. 1971) : The mineralogical investigation of the Fe - Zn - S system inconnexion with kontakt - metasomatic and hydrohermal sphalerite deposits. - Scien. Rep. of the Fac. of Scien. Ege Uni., s. 1 -67, No.: 122.

  • Gümüş, A. (1964) : Contribution à l’étude Geologique du secteur septentrional de Kalabak Köy - Eymir Köy (région d’Edremit), Turquie. - Pub. d. L`lns. d`Etud. et d. Rech. Min. d. Turq. ,No. 117. 1 -109, Ankara.

  • Krause, H. (1961) : Analytische und röntgenographische Untersuchungen natürlicher Zinkbienden. - N. Jb. Miner. Abh., 97, 143 - 164.

  • Kullerud, G. (1953) : The FeS - ZnS System. A geological thermometer. - Norsk. Geol. Tidskr., 32, 61 - 147.

  • Kullerud, G.(1964) : Review and evaluation of recent research on geologically significant, sulfide - type systems. - Fortschr. Min., 41, 221 -270.

  • Metz, P. & Winkler, H. G. F. (1964) : Experimentelle Untersuchung der Diopsıdbildung aus Tremolit, Calcit und Quarz. - Naturw. 51, 19.

  • Skinner, B. J. & Barton, B. P. Jr. & Kullerud, G. (1959) : Effect of FeS on the Unit Cell Edge of Sphalerite a Revision. Econ. Geol. 54, 1040- 1046.

  • Toulmın, P. III & Barton, B. P. Jr. (1964) : A thermodynamic study of pyrite and pyrrhotite. - Geochim. et Cosmochim. Acta., V 28, 641 - 671.

  • Winkler, H. G. F. (1966) : Der Prozess Anatexis : Seine Bedeutung für die Gonese der Migmatie. - Tschermaks Min. u. Petr. Mitt. Bd. XI, H. 3-4.

  • Winkler, H. G. F(1967) : Die Genese der metamorphen Gesteine. 2. Aufl. Springer Verlag, Berlin, Heidelberg, New York, 228.


  • Dora, O. Ö. (1971). (German) Über Verwendungsmöglichkeiten des Zinkblende Pyrrhotinmischkristalls als Geologisches Thermometer . Türkiye Jeoloji Bülteni , 14 (2) , 103-134 . Retrieved from https://dergipark.org.tr/tr/pub/tjb/issue/54955/753482

  • Par Des Méthodes Géophysiques, La Résolution du Problème de L`eau Salée et Nonsalée, Dans La Région de Samandağı - Hatay
    Adnan Ertürk
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    Abstract: Dans des certaines parties de la région de Samandağı - Hatay, la qualité de l`eau est salée; il n`est guère possible de résoudrele problème de l`extesion de salinité par les méthodes géochmiques et tes sondages que l`on a déjà forés.II est donc bien connu que les méthodes géoélectriques s`appliquent couramment à la résolution de ces genres problèmes.Les paramètres électriques peuvent être calculés en utilisant desméthodes ée resistivité à partir de la surface.II est fort possible de résoudre les problèmes concernant les qualités des eaux, en déterminant ces paramètres qui correspondentaux propriétés électroniques et éléctrolitiques des roches, dansdes zones noncimentées et saturées 100 % par l`eau.Nous tenterons ici d`expliquer la résolution de l`interférence del`eau salée - nonsalée et les résultats que nous avons obtenus;selon lesquels nous voulons également montrer la coincidenceentre les forages proposés et effectués. 

  • Dans La Région de Samandağı - Hatay

  • de L`eau Salée et Nonsalée

  • Méthodes Géophysiques

  • Bertrand, Y. La prospection Electrique appliqueée aux problèmes des Ponts et Chaussées.

  • Doğan, O. (Petrolojik Münasebetler ve Petrofizik).

  • Ertürk, A. Hatay-Samandağı, Yenimahalle Toprak ve Su Kooperatifi Jeofizik Rezistivite Etüt Raporu, 1970.


  • Ertürk, A. (1971). Hatay - Samandağı Kooperatif Sahasında Jeofizik Metodlarla Tatlı ve Tuzlu Su Girişimi Probleminin Çözümlenmesi . Türkiye Jeoloji Bülteni , 14 (2) , 135-141 . Retrieved from https://dergipark.org.tr/tr/pub/tjb/issue/54955/753487

  • The Carboniferous Stratigraphy of İstanbul
    Orhan Kaya
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    Abstract: The Carboniferous stratigraphy of İstanbul is describedwith special reference to the western part of Bosporus (Thracianarea). On the basis of particular stratigraphic successions ,andstructural features the Thracian area is subdividied in subareas of Istinye, Kâğıthane, Cebeciköy ,and Zekeriyaköy.The upper part of a predominantly nodular limestone unit(Büyükada fm.) is subdivided in two members, in ancendingorder: Ayineburnu ,and Küçükyalı. The Ayineburnu member iscomposed of thin-to medium - bedded nodular limestone ,andlaminated calcareous shales ,and ranges from Late Devonian toEarly Tournaisian in age. İt conformably overlaps the older Devonian strata on Ordovician rocks. The Küçükyalı member isrepresented by channel-filled turbidite graywacke ,and shale. TheBaltalimanı formation is mainly composed of lydites ,and subordinate siliceous shales. İt is Early / Middle Tournisian, / both,in age. The Trakya formation is characterized by thick shales,graywackes ,and lithic - conglomerates which are highly variableboth lateraly ,and vertically. The flysch facies, anyway interrupted, is predominant. On the basis of fine- ,and coarse-clastics ,anddistribution of carbonates the Trakya formation is subdividedin three members, in ascending order: Acıbadem, Küçükköy ,and Çamurluhan. The formation ranges from Late Tour-naisian to nearly Late Middle Visean in age. The Acıbadem memberconsists of shale ,and claystone with limestones intercalated.The Küçükköy member is composed of shales, thick-beddedgraywackes, lithic-conglomerates ,and subordinate limestones.The Çamurluhan member is mainly made up of shales with graywckes, lithic-and quartz - conglomerates, ,and limestones. Theshales become sandier ,and pebbly toward the north. The thickness, the biofacies, likewise change in the same direction. Atthe north, the shales are the time equivalent of the lower part ofthe overlying Cebeciköy limestone. The Cebeciköy limestone İscomposed of bioclastic limestone, subordinate shales, secondary dolomite ,and chert. The unit is of shelf-edge carbonate type ,and is Late Middle to Middle Late Visean in age. The Gümüşdere formation consists of graywacke, feldispathic garywacke,feldispathic conglomerate, shale ,and Iydite. The basal siliceousshale ,and Iydite designated the Kartaltepe member. İn the souththe siliceous shales predominate which gradationally overlie theCebeciköy limestone. İn the north, the lydites discordantly reston the lower sections of the Çamurluhan member. The flora ofthe member is in favor of a Late Visean- Namurian age. The maingraywacke section of the formation is of flysch facies. Minorcoal seams are present in the uppermost part of the formation.The Çiftalan formation consists of medium-to thick - bedded,subgraywackes. İt strikes parallel with the Gümüşdere formation ,and bears some compositional similarity to it. The Değirmendere formation consists of aphanitic limestone, clayey limestone ,and intraformational limestone - breccia. Secondary dolomitization is widespread. The poor microfauna bears the commonelements for Carboniferous ,and Permian. The Uskumruköy formation is composed of reddish shales, at its base ,and pebblygraywackes, on its higher section. The contact to the underlying limestone is obscured. Some coalified plant remnants occursparodically in the sandstones.İn the Thracian area the late Laramide phases appear to havebeen responsible for a large part of the deformation. Three Alpine stages are differentiated, in relative age : (a) overturnedfolds, steep thrust faults which are arranged along a WNW linemay be virtually connected with the thrusting towards the north- Zekeriyaköy overthrust-, (b) mosaic-fault system, resulted inby the release tectonic, (c) sinistral strike-slip faults with the NEtrend. The N trends, more / less separated from the Alpine features, can be attributed to the Varistic.

  • The Carboniferous stratigraphy

  • conglomerate

  • nodular limestone

  • Istanbul

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  • Baykal, F. ve Kaya, O., 1963. İstanbul bölgesinde bulunan Karboniferin genel stratigrafisi. M.T.A. Derg., 61, 1-9.

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  • Boureau, E., 1967. Traité de Paléobotanique, T. II. Paris.

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  • Dacı, A., 1951. Küçükçekmece ile Çatalca arasındaki Nummulitiğin paleontolojik etüdü. Rev. Fac. Sci. Univ. İstanbul XVI, 2-3, 89-113, 207-247.

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  • Kaya, O., 1969. Karbon bei İstanbul. N. Jb. Geol. Paläont. Mh., 3, 16-173.

  • Kaya, O. (Ed.), 1972. Paleozoic of İstanbul. Baskıda.

  • Kaya, O. ve Mamet, B., 1971. Biostratigraphy of the Visean Cebeciköy limestone near İstanbul, Turkey. Jour. Foram. Res., 1, 77-81.

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  • Kuenen, Ph. H. ve Sanders, J. E. 1956. Sedimentation phenomena in Kulm. and flozleeres graywackes, Sauerland and Oberharz, Germany. Am. Jour. Sc. 254, 649-671.

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  • Kaya, O. (1971). İstanbul’un Karbonifer Stratigrafisi . Türkiye Jeoloji Bülteni , 14 (2) , 143-199 . Retrieved from https://dergipark.org.tr/tr/pub/tjb/issue/54955/753491

  • A Study on Vanadinite and Desclosite
    Tuncay Kineş
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    Abstract: Vanadinite ,and desclozite of secondary lead mineralsoccur in a cave between the ovelying dolomite marble ,and the sericitecale schist at the bottom of the Keban metamorphic massive, Elazığ county East Turkey.The minerals having different mineralogical properties show distinct zoning marking changes in composition during the formation.These supergene products of the lead ,and zinc deposit are believed to take their lead, zinc ,and copper content from the primary sulphides. The secondary deposit is lithogene in origin beingformed by lateral secretion.It is most unlikely that the occurrence indicates that additionallead-zinc ore bodies can be found further away from the knownare bodies. 

  • Vanadinite

  • desclozite

  • lead-zinc ore

  • Goldschmidth, V. M. 1954 Geochemistry: Oxform Press.

  • Kineş, T. 1969 The geology and ore minelalization of the Keban area east Turkey: Doktora tezi Univ. of Durham.

  • Loveringr T. S. 1963 Epigenetic, diplogenetic, syrigenetic and litogene deposits: Econ. Geol. Cilt 58, s. 315.

  • Maucher, A; 1937 Keban madeni zuhuratı hakkında rapor: MTA Enstitüsü Ankara.

  • Notestein, F. B. 1918 Some chemical experiments bearing on the origin of certain U - V ores: Econ. Geol. cilt 13, s. 50.

  • Watsserstein, B. 1945 Discussion on paper by CM . Schwellnus: Proc. Geol. Soc. South Africa, cilt, XC, s. 48


  • Kineş, T. (1971). Vanadinit ve Desklozit Üzerine Bir Çalışma . Türkiye Jeoloji Bülteni , 14 (2) , 201-204 . Retrieved from https://dergipark.org.tr/tr/pub/tjb/issue/54955/753494

  • Vertical Variations in Grain Size Parameters and Heavy Mineral Abundance of Harhor Formation (Eocene) in Çayraz Area (Haymana)
    Teoman Nuriddin Norman Madjid Rasi Rad
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    Abstract: Harhor formation (Late Middle Eocene) outcrops in asmall syncline, situated to the north of the Haymana Anticline.The formation overlies the Çayraz formation (with abundant nummilites ,and assylinas) with a thin conglomerate ,and consists ofalternations of thick (50-200 cm.) sandstones ,and thin mudstone bands. Total visible thickness of the formation is 255 m. Theupper part, forming the centre of the syncline, is eroded. Thesecalcareous sandstones contain approximately 20 % muddy matrix ,and consist of volcanic rock fragments (more than 50 % byvolume), metamorphic schist, granite, limestone ,and chert fragments, as well as angular quartz, orthoclase ,and abundant calcicpiagioclase. Thus, the rock may be named as a litharenite, / evena volcanic - arenite. Heavy minerals consist of mainly glaucophane, garnet, apatite, zircon ,and tourmaline, in addition to abundantopaque iron minerals ,and a few others. The first three mineralsshow a good correlation in their «abundance» (Norman, 1969) within the rocks.Sediments of Harhor formation are probably derived from variouscomplex sources : basic volcanic, metamorphic, sedimentary ,andacid intrusive areas. In technically active geologic conditions, theywere first accumulated in relatively shallow marine waters (neritic environment) where from time to time, they formed submarineslumps, turning in turbidity currents. These currents resedimented the materials as turbidites in the deeper parts of the basins.The increase / decrease of abundance of various heavy mineralgroups at different stratigraphic levels may be explained by differential uplift in the source areas ,and widespread climatic changes which affected the rate of erosion.

  • Harhor Formation

  • heavy mineral groups

  • volcanic rocks

  • Haymana

  • Erol, O., 1954. Ankara ve civarının jeolojisi hakkında Rapor. MTA Enstitüsü Derleme Raporu No. 2491 (neşredilmemiş).

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  • Norman, T. & Rad, M. R. (1971). Çayraz (Haymana) Civarındaki Harhor (Eosen) Formasyonunda Alttan Üste Doğru Doku Parametrelerinde ve Ağır Mineral Bolluk Derecelerinde Değişmeler . Türkiye Jeoloji Bülteni , 14 (2) , 205-225 . Retrieved from https://dergipark.org.tr/tr/pub/tjb/issue/54955/753499

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