Türkiye Jeoloji Bülteni

Abstract: In den letzten 40 Jahren wurde die tektonische Eigentümlichkeit desÇamlıca-Gebietes von vielen Kollegen in verschiedener Weise erklört. Diese Tatsache zeigt uns vor allem, dass der geologische Bau dieser Gegendnicht so einfach sein dürfte.Im Jahre 1919 behauptete w. PENCK (1), dass eine Diskordanz zwischen der hochiegenden und vermutlich permokarbonischen Quarzitserie(Quarzite und Arkosen) und den darunterliegenden unterdevonischenSchiefern und Grauwacken bestehe. Bis 1925 schloss sich W. PAECKEL-MANN dieser Behauptung an, kam aber dann 1938 zu einer anderenAnsicht und betonte ausdrücklich, dass die Quarzitserie stratigraphischunter den devonischen Schiefern läge und daher dem oberen Silur gehörte.Ausserdem seien diese beiden Formationen sich meist durch Verwerfungen begrenzt (2).Nach einer kurzfristigen Untersuchung im Çamhca-Gebiet im Jahre1946 hatten wir w. J. McCALLIEN und der Verfasser (3) die Vermutungausgesprochen, dass die abnormale Grenze der beiden Formationen tektonischer Natur sei, das heisst: die obersilurischen Quarzite und Arkosenlägen als tektonische «Klippe» über den devonischen Schiefern undGrau-wacken (Abb. 2).In der letzten Zeit zweifelte E. ALTINLI (4) an dem Überschiebungs-vorgang und versuchte wie PAECKELMANN (2), die abnormalenGrenzverhältnisse zwischen der obersilurischen und der unterdevonischenSchichtserie durch steile polygonale Verwerfungen zu erklären (Abb. 3).Schon 1953, nach den tektonischen Untersuchungen auf den Prin-zeninseln konnte ich eine Diskordanz zwischen der west-oststreichendenobersilurischen Quarzitserie und den nord-südstreichenden devonischenSchief era (5). Die neuen Studien im Çamlıca-Gebiet führten den Verfasserzum gleichen Resultate, und zwar herrscht auch hier eine deutliche Diskordanz zwischen den obersilurischen und den unterdevonischen Serien;die beinahe westoststreichenden Falten des Obersilurs werden von dennord-südlaufenden devonischen Schichten umgerahmt. Das Ziel dieserkurzen Arbeit besteht daher, diese beobachtungstatsachen mit Hilfe derdetaillierten Kartierung und Profile zu illustrieren.

Abstract: The studied area is located in the central part of the largeKızılırmak river meander of Central Anatolia ,and the cities of Çorum, Sungurlu ,and Alaca are located in this district. Paleozoic, Mesozoic, Tertiary, ,and Quaternary sediments ,and rocks are found in this area.Paleozoic sediments contain chlorite, sericite, epidote, argillaceous ,and calcareous schists.Mesozoic sediments are mainly volcanic rocks which contain radiolarite ,andserpentine.Tertiary layers could be divided in Lutetian, Oligo-Miocene ,and Pliocenesubdivisions, Lutetian sediments are represented by a flysch which is made up ofconglomerate, sand, marl, arenaceous limestone ,and limestone layers. The approximate thickness is 800 m. Oligo-Miocene sediments are represented by a serieswhich contains discontinuous salt ,and gypsum beds between the conglomerate,sand, marl ,and clay layers overlying the Eocene sediments discordantly. Its thickness is approximately 1 000 -1 200 m. Pliocene sediments consist of the sand ,andmarl layers which contain limestone beds about 1-2 m. in thickness ,and overly theOligo-Miocene sediments discordantly.The Quaternary areas are mostly old ,and new alluvium ,and terrace deposits.In this area the gabbro ,and serpentines are represented by the magmatic rocksin the Mesozoic sediments. Andesites ,and basalts are the extrusive rocks which arefound in the Tertiary sediments.During the Paleozoic, the area was completely covered by the sea. The basinwas similar to a geosyncline. Toward the end of this time tectonic compression began ,and the land emerged above sea level. Some of these areas remained uncovereduntil the beginning of the Eocene epoch.After a long erosional period the Cretaceous sea covered most of the area. Atthe end of this period the sea was gone ,and after that the Eocene sea transgressiontook place. Toward the end of Eocene the sea regressed slowly ,and some lagoonswere formed. During this time the sediments, which contained discontinuousgypsum beds of Upper Eocene, were deposited. At the end of Upper Eocene thesea was mostly gone ,and new tectonic action took place. The erosional product ofthese Upper Eocene rocks made up the basal conglomerate of the Oligo-Miocenesediments. At the end of Oligocene some brackish lakes remained as remnants ofthe vanishing Eocene sea. During the Miocene, one arm of the sea transgressingin the E-W direction covered some parts of the area, which contained varicoloredseries, ,and caused the deposition of Miocene sediments of 2-3 m. in thickness.Fossils were found in these sediments. The direction of the layers, fault ,and folddirections ,and the axis of the anticlines ,and synclines are seen parallel to each otherin this area.All these phenomena are the result of Alpine tectonics. Oberved angular unconformities in the Paleozoic sediments indicate the presence of the pre-Alpinetectonic movements.

Abstract: The study is made on the maps, (scale 1/100,000 sheet number66/4, 67/3, 67/4, 83/2 and 84/1) of the eastern part of Lake Van. The area is mostlymountainous and has very poor road conditions. Previous works on this area weremade by F. Oswald, J. H. Maxson, E. J. Foley, P. Arni, I. Ortynski, and E. Altınlı.The following formations are seen in this area:Paleozoic.- The Paleozoic is represented by the limestones which are foundparallel to the shores of the Micinger suyu. The age of these limestones is Permianand they are completely crystallized. The Paleozoic in the vicinity of Özalp is represented by schists. 

Cretaceus.- Thisformation is represented by the limestones and overlyingthick flysch beds.

P a l e o c e n e.- The Paleocene sediments are composed of variegated shales,marls, and thin-bedded limestone beds.

Eocene.- The lower part of the Eocene sediments is represented by 100 - 150m. of sandstones and marls. Above these formations there are white fossiliferouslimestones, which are about 300 m. in thickness.

Miocene.- The Miocene is represented by the alternating sandstones andmarls. Generally the Miocene sediments contain more fossils.

Neogene.- The Neogene is represented by the continental deposits composed of sands, limestones, conglomerates and clays, which are probably Pliocene inage.

Recent.- The alluvium deposits are found, in the valleys of this district.Volcanic rocks.- These are serpentines, andesites and basalts. Serpentines areUpper Paleocene, andesites Pliocene and basalts probably Pleistocene in age.

Paleogeography.-The area was above the sea level from Paleozoic to Cretaceous. A general transgression had occurred during the Upper Cretaceous and thearea occupied by the sea until Lower Eocene age. At the beginning of the Miocenethe second transgression had taken place. At the end of the Miocene the sea regressed.The tectonic actions took place during the Tertiary period and some dislocations have resulted.Due to the fact that no favorable structural features were observed in the areastudied, it may be concluded that no economically important petroleum resourcesexist in this region.

Abstract: The study was made on the farm of Ercüment Özbaş, who hadnotified the presence of oil indications on his farm, located in Söke.The area is covered by the following secies: gneiss-micaschist ,and metamorphosed limestone of Menderes group, at the bottom; this group is overlain by thesandstones, limestones, conglomerates, ,and fossiliferous sands of the Miocene age ,and, overlying these sediments, are found some fossiliferous sands ,and alluvium.The Menderes group represents the main rock of the area, which had solidifiedat the beginning of the Primary; probably orogenic actions took place during theCaledonian ,and Antecambrian. From the end of Paleozoic until the beginning ofMiocene, the area was above the sea level. At the beginning of Miocene the area wascovered by a sea.As a result of Alpine movements, a vertical subsidence of thick sediments tookplace during Miocene. These tectonic actions continued also during the Pliocene.Because of this tectonic activity, the area is fractured and faulted. In this area themagmatic activity has also taken place.The area does not contain any important geological structure / reservoir rocks.Therefore, it is impossible to expect here any economically important oil deposits.The natural gas-which was found during the drilling for water in the Özbaşfarm- has the following characteristics: it is colorless ,and odorless ,and has a lowpressure. This kind of gas is usually produced by the decomposition of the organicmaterial within the layers of Quaternary sediments ,and is accumulated in the pockets, which are usually found in these sediments. The gascontaining pockets are generally surrounded by impervious argillaceous sediments, which do not permit thegas. to escape. This gas is found under thick recent sediments, which compress thegas in the pockets. When these pockets are drilled, the gas-relieved from the highpressure-escapes the hole.The gas found in Söke, being of the similar origin, is an unimportant, burningswamp gas.

Abstract: İt is well known that the existence of slag heaps ,and galleries containingacid waters, near sulphide deposits, make It extremely difficult, If not impossible, to Interpret the self potential measurements taken around them.This is due to the generation of self potentials by the slags ,and wet galleries,having magnitudes of the same order as those given by the deposit itself.Hence, the elimination of such effects from the total anomaly is essentialfor an intelligible interpretation of the total anomaly.

The problem of elimination of these effects is attacked in two ways:

1. By the method of finite differences with the resulting linear equations solved by relaxation methods.

2. By an empirical method of finding the self potential moment of theslag / gallery ,and thereby proceeding to the calculation of the spuriouseffect.

Abstract: Suivant les méthodes de Poldervaart (2, 3), l`auteur a fait l`étude deszircons provenant d`un gneiss oeillé du Menderes-massif d`origine controversée. Selon les uns les gneiss oeillés représenteraient d`ancienes granitesporphyroides. Sa texture alors serait blastoporphyrique. Selon d`autres lesgneiss oeillés seraient d’anciens sédiments. Dans ce cas les yeux de feldspathdevaient être nommés des porphyrablastes. Pour déterminer l`origine deces gneiss une étude des zircons accessoires paraissait très utile, puisqueles zircons sont des minéraux très réfractaires. Si les zircons sont d`originesédimentaire dans une roche, ils garderont une forme arrondie par toutephase de métamorphisme et d`orogenèse, tandis que les autres minérauxrecristallisent. Si, par contre, les zircons sont d`origine magmatique ils resteront idiomorphes, tandis que les autres preuves du stade magmatiquepeuvent être effacées par une gneissification et des processus metasomatiques ultérieurs. Dans le cas qu`une roche sédimantaire entre par ultramétamorphisme dans le stade magmatique, une redistribution du matériel deszircons commence, qui se traduit par des croissances idiomorphes sur desnoyaux arrondis (4).

Abstract: Kurumumuz üyelerinden Paleontolog P. Bayrak, 1957 Eylül ayında, verimli ve genç çağında aramızdan ayrılmıştır. Geride bıraktığı üç çocuğu ve ailesi kadar meslekdaş ve arkadaşlarının da acısı büyüktür. Perihan Bayrak, Nisan 1922 de Arapkir`de doğmuştur. İlk ve Orta tahsilini Sivas`ta yapmış ve 1940 da Sivas lisesinden mezun olmuştur. Yüksek tahsilini İstanbul Üniversitesi Fen Fakültesinde yapmış ve 1946 yılında Tabiî İlimler lisansiyesi olarak Üniversiteyi bitirmiştir. Mezuniyetinden sonra öğretmenlik mesleğine girmiş ve Sivas lisesi ve Öğretmen okulunda yedi yıl tabiîye öğretmenliğinde çalışmıştır. Bu vazifesini muvaffakiyetle ifa ederken, eşinin Ankara`ya tâyini dolayısiyle, ayrılmak mecburiyetinde kalmıştır.1954 yılında. M.T.A. Enstitüsü Paleontoloji servisinde çalışmağa başlamıştır. Burada Brachiopod`lar üzerinde çalışmış ve kısa zamanda gayreti sayesinde, mevzuu tamamiyle kavramıştır. Buradaki çalışmaları esnasında, muhtelif jeologlara ait arazi numunelerinin determinasyonlarını ihtiva eden, 6 adet paleontolojik rapor yazmıştır. Üçüncü bir evlât sahibi olacağını düşünerek, meslekten muvakkaten ayrılmak mecburiyetinde kalan arkadaşımızın, bu çocuğunu büyütemedenânî olarak hayata veda etmesi, hepimizi teessür içinde bırakmıştır. Ailesinin ve çocuklarının acısını paylaşır ve arkadaşlarımıza başsağlığı dileriz.

Abstract: Kurumumuz üyelerinden ve Mikropaleontoloji mesleğinin değerli simalarından olan arkadaşımız S. Başad, 14 Temmuz 1958 Pazartesi günü, âni olarak hayata gözlerini kapamıştır. Arkadaşımızın genç yaşta aramızdan ebediyen ayrılışı ailesi, meslekdaşları ve tanıdıkları arasında büyük bir teessür uyandırmıştır. Sevinç Başad 15 Haziran 1922 de İzmir`de doğmuştur. İlk tahsilini İzmir Fransız mektebinde bitirdikten sonra, Orta tahsilini İzmir Kız lisesinde yapmış ve 1940 yılında Fen şubesinden mezun olmuştur. Yüksek tahsilini İstanbul Üniversitesi Fen Fakültesinde yapmış ve 1946 yılında Tabiî İlimler lisansiyesi olarak Ünivetsiteyi bitirmiştir. Mezuniyetinden sonra öğretmenlik mesleğine girmiş ve 1947 den 1953yılına kadar Tokat lisesi Tabiiye öğretmenliğinde çalışmıştır. Bu arada bir müddet lisenin müdür muvainliğini de başarı ile ifa etmiştir. Bu vazifelerde pek çok talebe yetiştirmiş ve onlarda bilhassa tabiat ilimlerine karşı heves vealâka uyandırmağa gayret etmiştir.1953 yılında öğretmenlikten ayrılarak, M.T.A. Enstitüsü Paleontoloji servisinde çalışmağa başlamıştır. Burada Mikropaleontoloji ve bilhassa Mesozoik Foraminiferleri mevzuu üzerinde çalışmalar yapmıştır. Doktora tezi olarak verilen «Ankara civarı, Etimesut-İstanbul boğazı stratigrafik etüdü ve mikrofaunası» mevzuundaki çalışmasını ne yazık ki, tamamlıyamadı. Bu çalışmasını yaparken, Paleontoloji servisinde, M.T.A. nın muhtelif jeologlarına ait arazi numunelerinin determinasyonlarını ihtiva eden, 73 adet mikropaleontolojik rapor yazmıştır. Çalışmalarının en verimli olacağı bir çağda, aramızdan âni olarak ayrılması, acımızı bir kat daha artırmaktadır.