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    History of natural stones and industry of Turkey
    (2009) Tuncer G.; Kerey I.E.
    Anatolia was one of the centers of marble production and trade especially in antique ages.Quarries that provided the marble used in the majestic structures in huge proportions of the antique era were located mostly in Western Anatolia.Marmara Island is in the Northwest Anatolia, Marmara Sea took its name from "Marmaro", meaning marble in Greek; it contains the most important white marble quarries and was the most important export center especially during Roman period.Quarries where the bluish Marmara Marble was mined were expanded by Romans and turned into big enterprises.Marble was transported to Mediterranean and Black Sea as well, with Roman's Ships that could carry big blocks. Marble was not only exported as blocks from there,they were sold first as semi-processed (decorations would be made on arrival) pillars, sarcophagus and similar products, then fully pocessed in late antique age. Most of the white marble used in Istanbul in Byzantium and Ottoman periods were shipped from Marmara Island. © 2009 All Rights Reserved by the International Multidisciplinary Scientific GeoConference SGEM.
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    Sedimentological characteristics of the Çukurbag Formation deposited along the Ecemis Fault Zone, Central Anatolia, Turkey
    (2007) Gürel A.; Çiftçi E.; Kerey I.E.
    The Oligocene Çukurbag Formation, deposited within a long narrow basin surrounded by the Aladag, Ulukisla, and Nigde metamorphic Groups, consists of conglomerate, sandstone, siltstone, mudstone, marl, mudstone-gypsum successions. A number of analytical methods including morphological, mineralogical, and chemical techniques were employed to investigate the sedimentological characteristics of the formation. According to the grain size analyses, sediments of the formation are very poorly sorted with strong positive to near symmetrical skewness. The analyses show that irregular flow regime should have occurred during sedimentation of the Çukurbag Formation. These sediments comprises mainly of quartz, feldspars, calcite, clinopyroxene, and Fe-oxides. Common clay minerals include smectite, chlorite, and kaolinite. The chemical analyses carried out on the samples representing the bottom to the top of the formation indicated that SiO2, Al2O3, K2O, and P2O5 contents are low compared to the world mudstone averages. However, MgO, CaO, and C contents are comparatively high. Four measured profiles showing the distribution of principle facies within the formation are prepared. Based on the profile analyses, seven distinct lithological facies were distinguished that include massive conglomerate, bedded conglomerate, stratified sandstone, cross-bedded sandstone, laminated siltstone, massive mudstone-marl, and laminated mudstone-gypsum. This study suggests that the sediments of this formation must have been reworked material transported from unknown distances and deposited in an alluvial fan-braided stream and lacustrine environments. © Geol. Soc. India.
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    Sedimentology and mineralogy of late miocene Paleosols and calcrete rich sediments in the western part of central anotolian volcanic province (CAVP), Turkey
    (2008) Guel A.; Kerey I.E.; Ozcan S.
    The Dogantarla-Aksaray area is situated in western part of the CAVP. This province contains nine (9) different ignimbrite levels, for which a Late Miocene age is indicated by vertebrates as well as K/Ar ages of 11 to 2.8 Ma (Viereck-Goette et al 2006). However, most paleosol and calcrete occur within the interval of 7.6 to 2.8 Ma (Gurel and Kadir, 2006). Among this ignimbrite levels, fluvial and lacustrine sediments are found, so called Bayramhacili Formation of western CAVP consist of alternation of typical red conglomerate, sandstone, mudstone, diatomite-limestone and intercalated with several red colored paleosol and calcrete levels. Paleosols and calcrete occurs in sequences with in the whole stratigraphic profile. It is recognized that they are aridisols, inceptisols, locally associated with, oxisols and vertisols, according to the soil taxonomy (Soil Survey Staff, 1992). Paleosols and calcrete of Dogantarla-Aksaray area are characterized by thin section, X-ray diffraction (XRD), and scanning electron microscopy (SEM). Paleosols and calcrete are composed of feldspars, quartz, opal-CT, amphibolites, serpentine, and talk are dominant in the whole profile. They are accompanied by smectite, chlorite, palygorskite, and illite, locally associated with accessory sepiolite. The grains are cemented clay minerals or iron oxide, calcite, and gypsum. The calcite content is attributed mainly to calcrete building, which has a sub-parallel relationship with calcrete, and occurs mainly in the interlayer space of smectite. The clay content decreases with increase in calcite. The non-carbonate fraction is, therefore, quite rich in aluminosilicate minerals. Thus, the presence of an inverse relationship between CaO and other oxides may correspond to an inverse relationship between calcite and other minerals. Minerals such as palygorskite, chlorite, and gypsum are enriched in some levels of the profile. In addition that authigenic smectite, palygorskite and calcite formed as a result of the calcretion of paleosol and calcrete units in alkaline conditions, high Si and Mg activity and low Al; Paragenesis and textural features of the minerals of the fluviallacustrine sediments determined in the study area indicate that precipitation should have been occurred due to climatic fluctuations ranging from arid, semi arid to wet conditions.
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    Stratigraphic features and geotectonic evolution of the south edge (narman-oltu-olur) of eastern Pontids (Northeast Turkey)
    (2008) Bozkus C.; Kerey I.E.; Tuncer G.
    The southern edge of Eastern Pontids is covered by rock units belonging to two distinct continental crusts that reunited through a Late Upper Cretaceous-Eocene suture zone. In the north of the Suture zone (Olur), Paleozoic aged acid magmatits (Permo- Carboniferous) constitute the continental crust basement. On this basement, there is uninterrupted marine sediment which has disconformably developed between Upper- Lias Late Cretaceous. These sediments have deposited under the conditions of Lias- Lower Malm basic volcanic intercalated and fragmented shallow marine, carbonate Upper Malm-Neocomien (Valanjinien), Hotrivien-Kampanien flysh and Meastrihtien shallow marine carbonate facieses. Thus, the deposition period that was dominated by pyroclastics as a result of Kampanien volcanic activity has come into being. At the lowest level of suture zone (Oltu), Santonien-Meastrihtien aged external blocked (olistolithe) tectono-sedimenter mixture take place in the typical flysh facieces. In the south of Suture zone (Narman), ophiolite units take place in the position of tectonic segments that are generally inclined to the north and belonging oceanic crust in the shape of ophiolite mixture. In the north of continental crust where arc volcanism is situated, the fact that the ophiolite rocks, in the south, outcrops of north-inclined tectonic segments and oceanic crust is a proof of a northwards subduction. The volcanic activity that is seen in the pyroclastic type in this field has first started in Kampanien and then in dasitic Turonien type in the relatively north. This displays the fact that the northwards subduction has developed at the beginning of Upper-Cretaceous. These three rock units belonging distinct tectonic environments are generally covered with angular disconformity that are constituted by units of volcanic and Eocene aged shallow marine-continental fragments. Thus, opening in Lias, with the developed oceanic northwards subduction, has been closed before Eocene. At the end of Eocene, in the completely non-marine suture zone and intermountain molas basins, which were limited between the mountain ranges that are stuck between the overlapping postorogenic ophiolite, Oligocene aged continental fragments have been developed. These units have been covered by Post and Upper Miocene and generally horizontal or almost horizontally situated volcanic and continental sediments. This zone has been under the influence of the tectonic controls of both the Lias-Lower Cretaceous and the beginning of Upper-Cretaceous to recent compression. A control of mutual Upper Cretaceous-Upper Miocene compression and thickening, and another compression control influenced by Upper Miocene to recent compression and thickening activity have been dominant, because curved and overlapping structures of pre-upper Miocene have been covered by almost horizontally situated Late Miocene aged rock units in disconfirmity. In this respect, the beginning of the neotectonic period in this zone has to be in the Upper Miocene.