Style and timing of the Meso-cenozoic deformations at the frontal part of the southern Greater Caucasus (Georgia): comparison between the western (Rioni basin domain) and eastern parts (Kura basin domain)
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The Pannonian basin system is an integrap part of the Alpine mountain belts of east-central Europe. It is completely encircled by the Carpathian Mountains to the north and east, the Dinaric Alps to the south, and the Southern and Eastern Alps to the west. In 1912, Kober defined the Pannonian basin as one of the type "Zwischengebirge," a relatively un-deformed region characterized by block faulting and situated between externally vergent thrust belts. More recent studies using subsurface data have shown that the Pannonian area was extensively deformed by Mesozoic thrusting and subsequently disrupted by a complex system of Cenozoic normal and wrench faults. Thus, the Pannonian "massif" has undergone several types of deformation, which are partly hidden by a thick sequence of sedimentary rocks of Neogene-Quaternary age. The Pannonian basin is actually a system of small, deep basins separated by relatively shallow basement blocks. The Neogene-Quaternary sedimentary rocks exceed 7 km in thickness in some areas, and the basin system (including the Transylvanian basin) is about 400 km from north to south and 800 km from east to west. It is currently interpreted by most workers as a Mediterranean back arc extensional basin of the middle Miocene age. The Carpathians, Eastern Alps, and Dinarides, which surround the Pannonian basin, are the result of Mesozoic and Cenozoic continental collision between Europe and several continental fragments to the south, including Africa. Thrusting was direted outward from the present Pannonian basin toward the European platform and the Adriatic region. In all the orogenic belts, the interior parts of the thrust belts were deformed in Mesozoic time, while the outer parts were deformed in Tertiary time. The volume presents 26 papers and eight regional maps resulting from a joint five-day symposium held in Veszprem, Hungary, in 1982 entitled "Evolution of Extensional Basins within Regions of Compression with Emphasis on the Intra-Carpathian Region." The symposium was sponsored jointly by the Hungarian Oil and Gas Trust, the Hungarian Geological Survey, and the U.S. National Science Foundation.
Neogene
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In 1967 and 1969, two oceanographic cruises were made in the Black Sea under the guidance of the Woods Hole Oceanographic Institute: The cruises included scientists from many countries and disciplines. Their aims were to determine the recent geological and geochemical evolution of the Black Sea, to map the shallow structure of the basin, and to study the interaction between the oxidized surface waters and the anoxic waters beneath them. The results were published 23 years ago, as AAPG Memoir 20 (Ross and Degens, 1974). During the 1969 cruise, the vessel Atlantis II collected 40 piston cores, which formed the basis of most of the subsequent geological studies that were restricted to very recent sedimentation. Speculations concerning the origin of the basin and the relationship of the geology offshore to that exposed around the margins of the Black Sea were rooted in pre-plate tectonic concepts of basin formation and were in any case hampered by a lack of relevant data (Brinkmann, 1974).In 1976, the Glomar Challenger visited the Black Sea on Leg 42B of the Deep Sea Drilling Project and drilled and cored three deep-water sites (379, 380, and 381). Well 381 north of the Bosporus encountered sediments as old as Miocene, including some apparently deposited in shallow water (Ross, 1978).The next major volume in Western literature to deal with the Black Sea was published a decade later, collecting papers presented two years earlier at a conference in Yalta. In this volume, a number of seismic reflection lines
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Black Sea
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Tension of the Greater Caucasus lithosphere, located in a zone of pseudosubduction articulation of the northern and southern Caucasus massifs (tectonic microplates), is the result of penetration of the Arabian indenter into the buffer structures of Eurasian during the continental stage of Alpine tectogenesis (since the end of Miocene).This statement is confirmed by geophysical observation data over the structure and seismodynamic activity of the regional Earth's crust that generally represents an underthrust zone of the southern Caspian microplate's Kakheti-Vandam-Gobustan margin under the Eurasia's southern underside (Scythian-Turanian epi-Hercynian platform), accompanied by heaving and southward advancement of the allochthonous accretionary prism built by structural-material complexes of the Greater Caucasus marginal seaside.This factor determines peculiarities of both surface and deep structure of the orogen, reflected in geological mapping, seismic and electrical prospecting activities, as well as gravitational and magnetometric observations in Azerbaijan.The paper describes the peculatities of the surface and deep geological structure that defines the modern seismic and geodynamic activity.
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Prospecting
Riphean
Geologic map
Accretionary wedge
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Clockwise
Neogene
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The Alpine tectonic evolution of the Danube Basin and its northern periphery (southwestern Slovakia)
Abstract The tectonic evolution of the pre-Cenozoic basement, as well as the Cenozoic structures within the Danube Basin (DB) and its northern periphery are presented. The lowermost portion of the pre-Cenozoic basement is formed by the Tatricum Unit which was tectonically affected by the subduction of the Vahicum / Penninicum distal continental crust during the Turonian. Tectonically disintegrated Tatricum overlaid the post-Turonian to Lower Eocene sediments that are considered a part of the Vahicum wedge-top basin. These sediments are overthrust with the Fatricum and Hronicum cover nappes. The Danube Basin Transversal Fault (DBTF) oriented along a NW–SE course divided the pre-Neogene basement of the DB into two parts. The southwestern part of the DB pre-Neogene basement is eroded to the crystalline complexes while the Palaeogene and Mesozoic sediments are overlaid by the Neogene deposits on the northeastern side of the DBTF. The DBTF was activated as a dextral fault during the Late Oligocene – Earliest Miocene. During the Early Miocene (Karpatian – Early Badenian) it was active as a normal fault. In the Middle – Late Miocene the dominant tectonic regime with NW – SE oriented extension led to the disintegration of the elevated pre-Neogene basement under the simple and pure shear mechanisms into several NE – SW oriented horst and graben structures with successive subsidence generally from west to east. The extensional tectonics with the perpendicular NE – SW orientation of the S hmin persists in the Danube Basin from the ?Middle Pleistocene to the present.
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Horst
Paleogene
Alpine orogeny
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Horst and graben
Basin modelling
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Heat flow data from the Eastern Mediterranean region indicates an extensive province of low heat flow, spreading over the whole basin of the Mediterranean to the east of Crete (Levantine Sea), Cyprus, and Northern Egypt. Surface geology of East Anatolia is complex because of recent active tectonic and volcanic activity. The region is composed of major tectonic units of Pontides, the Anatolid-Tauride Belt and Bitlis Suture Zone, North and East Anatolian faults. Ophiolitic and young volcanic rocks can be observed in many parts of East Anatolia. The Black Sea is surrounded by the Alpine-Himalayan Orogenic Belt of Crimea, Greater Caucasus, Pontides, Rhodope-Stranja Massif, Eastern Srednegorie, North Dobrogea and older tectonic units of different origins and ages such as the Precambrian East European Craton, Moesian Platform, Istanbul Zone and Adzhar-Trialet Folded System. Low heat flow density dominates in the Black Sea. The lowest (less•30 mW/m2 ) values have been recorded in central parts of the Western and Eastern Black Sea basins with maximal sedimentary thickness. Geothermal studies within the territories of Ukraine have been under way since sixties. Many important features of the thermal field remain unstudied. This applies in particular to the Ukrainian Shield and to the southern part of the Carpathian region. In general, the territory of Alpine folding within Turkey, Marmara and Aegean seas, Caucasus is characterized by high heat flow. The anomaly of its highest values (above 100 –150 mW/m2 ) exists within western Turkey, where tectonic conditions of extension prevail and underground steam is used to produce electricity. Three heat flow density profiles crossing the studied region and heat flow map were compiled.
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African Plate
Eurasian Plate
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The Madrid basin is intracratonic and triangular in form, being bounded on its three sides by Tertiary mountain ranges: the Spanish Central System in the north, the Toledo mountains in the south, and the Iberian and Altomira ranges in the east. The Altomira range separates the Loranca basin from the Madrid basin (Fig. 1). Each of these mountain ranges has a different structure and Tertiary geological evolution. The kinematic history of each of these borders of the Madrid basin reflects differences in the transmission of stresses from the active Iberian plate boundaries where the Betic and Pyrenean chains themselves had distinctive kinematic histories.
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