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Chokrakian
Middle and Upper Miocene Deposits and Facies of Northern Ustyurt (Western Kazakhstan)
Schematic map of distribution of the Tarkhanian-Chokrakian facies and thick...
Neogene Paratethyan succession in Turkey and its implications for the palaeogeography of the Eastern Paratethys
Abstract The Neogene marginal succession of the Eastern Paratethys (EP) crops out along the southern Black Sea coast and in the Marmara region of Turkey, and provides important clues to the tectono-sedimentary and palaeoceanographic conditions. In the Tarkhanian stage, the southern margin of the EP basin was largely a carbonate platform covered by warm, marine waters. From the end of the Tarkhanian to the Early Chokrakian there was an overall emergence throughout the basin, which is indicated by an influx of siliciclastic sediments. The fossil assemblage indicates that normal marine conditions persisted during most of this period, except for a salinity reduction towards the end due to an eustatic isolation of the basin, which in turn led to anoxic bottom water conditions. The Late Chokrakian isolation became even more severe during the Karaganian as indicated by the endemic fossil assemblage indicating brackish-marine conditions. Carbonate platform conditions prevailed in the northern Pontides during this time. In the Early Konkian, the basin was reconnected briefly with the world ocean by a transgression from the Indo-Pacific Ocean. In the Late Konkian there was a return to brackish-marine conditions. Lower Sarmatian sediments are absent in the southern margin of the EP, but elsewhere in the basin this stage is characterized by a widespread marine transgression. In the Middle-Late Sarmatian, the EP basin was partially isolated with freshening and anoxic bottom-water conditions. During this time there was a brief marine transgression from the Mediterranean into the Marmara region, but it did not reach the Paratethyan basin. The Pontian is characterized by an extensive transgression from the EP that inundated the Marmara and northeastern Aegean regions. The connection with the Marmara Basin was cut off during the Kimmerian and re-established during the Late Akchagylian, when the EP basin was inundated by the Mediterranean waters via the Sea of Marmara as a result of increased North Anatolian Fault activity and a short-term global sea level rise.
Schematic map of distribution and facies of middle Miocene (younger than th...
Abstract The Kura foreland fold–thrust belt is located in the northern part of the active collisional Lesser Caucasus orogenic belt associated with Arabia–Eurasia convergence. This belt is the best example of mountain-building processes in late Alpine time. Seismic reflection profiles show that the Kura foreland fold–thrust belt of the eastern Caucasus is an active thin-skinned fold–thrust belt and is represented by fault-bend folds, fault-propagation folds and duplexes. Analysis of growth strata in seismic profiles and oil well data from the Kura foreland fold–thrust belt documents that the evolution of deformation has been continuing during the last c . 14–15 myr (since the Middle Miocene), together with the thrust system kinematics. The geometry of the growth strata is associated with footwall synclines and piggy-back basins. Compressional deformation on the Kura foreland began in the Middle Miocene (Chokrakian) and reached its maximum rate at the end of the Miocene ( c . 5 Ma).
Lithological log of the Maikop Group and concentrations and ratios of selec...
Lithological log of the Maikop Group exposed along the Belaya River togethe...
A geologic profile along А–B and B–C lines on the northern Ustyurt chink in...
The sensitivity of middle Miocene paleoenvironments to changing marine gateways in Central Europe
Late Cenozoic deformation of the Kura fold-thrust belt, southern Greater Caucasus
The type section of the Maikop Group (Oligocene–lower Miocene) at the Belaya River (North Caucasus): Depositional environment and hydrocarbon potential
Evaporites of Ukraine: a review
Abstract The results of geological and lithological–geochemical investigations of the Devonian, Permian, Jurassic and Miocene evaporite deposits of Ukraine are presented in review. The main regions of evaporite distribution are the Dnipro–Donets depression, Carpathian (Forecarpathians, Transcarpathians) and Foredobrogean regions. The data on tectonics and stratigraphy are presented and information on lithology, the mineralogical and geochemical study of gypsum, anhydrite, rock and potash salts are summarized. The rich mineral composition of the Miocene evaporites in the Carpathian Foredeep (more than 20 salt minerals) is demonstrated, and the unique superimposed hydrothermal mineralization in the rock salt of salt domes from the Dnipro–Donets depression is presented (containing about 40 high- and mid-temperature hydrothermal minerals). In particular, the results of brine inclusion studies in evaporite minerals suggest that seawater was the main source of most of the salts. The brines in both the Miocene and Permian evaporite basins are classified as the Na–K–Mg–Cl–SO 4 (SO 4 -rich) chemical type and the Jurassic and Devonian belong to the Na–K–Mg–Ca–Cl (Ca-rich) type. Temperature of solutions during halite precipitation shifted from 25 to 43 °C, while during the stage of potash salt sedimentation it apparently increased to 40–83 °C.
Source potential and depositional environment of Oligocene and Miocene rocks offshore Bulgaria
Abstract Oligo-Miocene (‘Maikopian’) deposits are considered the main source rocks in the Black Sea area, although only a few source-rock data are available. Geochemical logs from nine wells are used together with age constraints provided by calcareous nannoplankton, well and seismic data to determine vertical and lateral changes of the source potential. Oligocene rocks overlie Eocene deposits with a major unconformity on the western Black Sea shelf in Bulgaria. A west–east-trending erosional structure (the Kaliakra canyon) developed during Lower Oligocene time and was filled with Oligo-Miocene deposits. Potential source rocks are present in different stratigraphic units, but the most prolific intervals accumulated during time intervals when the isolation of the Paratethys resulted in oxygen-depleted, brackish environments with high bioproductivity. These include Lower Solenovian rocks related to blooms of calcareous nannoplankton, which form an extensive layer outside the Kaliakra canyon. This unit hosts a good potential to generate oil and gas. Diatom-rich, very good oil-prone source rocks accumulated during a second isolation event in the Kozakhurian. Thick sections of these diatom-rich rocks occur within the canyon and are present in thin layers outside of it. High productivity of siliceous organisms is attributed to upwelling within the canyon. All studied units are thermally immature on the shelf.
Why are there no Messinian evaporites in the Black Sea?
Abstract The tectonic and geological evolution of Georgia and the Caucasus, on the whole, are largely determined by its position between the still converging Eurasian and Africa–Arabian lithosphere plates, within the wide zone of a continent–continent collision. The region in the Late Proterozoic–Early Cenozoic belonged to the now-vanished Tethys Ocean and its northern (Eurasian) and southern (Africa–Arabian) margins. Within this convergence zone there existed a system of island arcs, intra-arc rifts, back-arc basins characteristic of the pre-collisional stage. During syncollisional (the Oligocene–Middle Miocene) and post-collisional (the Late Miocene–Quaternary) stages, at the place of back-arc basins were formed fold and thrust belts of the Greater and Lesser Caucasus separated by the Transcaucasian intermontane lowland. Starting from the Late Miocene and as far as the end of the Pleistocene, in the central part of the region, simultaneously with formation of molassic basins and accumulation of coarse molasses there took place volcanic eruptions in subaerial conditions. According to the numerous data obtained during past decades we present a review on the lithological and structural characteristics of these collisional basins and on the coeval magmatic events.
VOLHYNIAN (EARLY SARMATIAN SENSU LATO) FISHES FROM TSUREVSKY, NORTH CAUCASUS, RUSSIA
Postcollisional tectonics and seismicity of Georgia
ABSTRACT During the Oligocene, marine Tethyan basins were replaced by euxinic basins, which are considered to represent the beginning of syncollisional development between the Arabian and Eurasian plates in Georgia. Ongoing collision during Miocene–Pleistocene times caused inversion of topography such that fold-and-thrust mountain belts of the Great and Lesser Caucasus, and the intermontane foreland basins in between the two mountain belts, were formed where intra-arc and back-arc basins had been. Analysis of seismic sections showing growth strata in intermountain foreland basins indicates that the thrust system in Georgia was active ca. 4 to 3.5 Ma. Beginning in the late Miocene, coeval with molasse deposition in the foreland basins, subaerial volcanic eruptions occurred, characterized by intensively fractionated magma of suprasubduction-type calc-alkaline series from basalts to rhyolites. Outcrops of the magmatic rocks are exposed along the boundaries of the main tectonic units of the region. Pyroclastic rocks of the first volcanic stage (Goderdzi Formation) contain Upper Miocene–Lower Pliocene petrified subtropical wood and other floral remnants. Marine deposits of the Goderdzi Formation are represented by sandy diatomite, which hosts Upper Miocene nanoplankton. In addition to volcanism, earthquakes indicate active tectonics in Georgia. Some of the major earthquakes have proven to be devastating; i.e., the Racha earth-quake of 29 April 1991, with Ms = 6.9, was the strongest ever recorded in Georgia. The fault plane solution data for 130 earthquakes show that the territory of Georgia is currently under latitudinal compression, longitudinal extension, and an overall crustal thickening. A complex network of faults divides the region into a number of separate blocks. The boundary zones between these terrains represent maximum geodynamic activity. Three principal directions of active faults compatible with the dominant, near N-S compressional stress produced by northward displacement of the Arabian plate can be distinguished: one longitudinal, trending WNW-ESE or W-E, and two transversal, trending NE-SW and NW-SE. The first group (WNW-ESE), the so-called “Caucasian” strike, is composed of compressional structures, including reverse faults, thrusts, thrust slices, and strongly deformed fault-propagation folds. The transversal faults are also mainly compressional structures, but they contain considerable strike-slip components as well. The tensional nature of submeridional faults is associated with intensive Neogene–Quaternary volcanism in the Transcaucasus. The NE-SW left-lateral strike-slip faults are the main seismoactive structures in the western Transcaucasus, while right-lateral strike-slip faults are developed in the southeastern Transcaucasus. Considerable shortening and deformation of Earth’s crust have taken place via compressional structures, as well as lateral tectonic escape. The geometry of the tectonic features is largely determined by the wedge-shaped rigid Arabian block (indentor) and by the configuration of the oceanic-suboceanic lithosphere (resistant domains) of the eastern Black Sea and south Caspian Sea, all of which cause bending of the main morphological and tectonic structures of the region around the indenting, resistant domains.
Abstract Three fundamental stages of the Cretaceous–Neogene tectonic evolution of the Odessa Shelf and Azov Sea (northern margins of western and eastern Black Sea basins, respectively) have been documented from the analysis of reinterpreted regional seismic profiling and one-dimensional (1-D) subsidence analysis of 49 wells, for which the stratigraphic interpretation was recently revised. (1) An initial active rifting stage began within the Early Cretaceous (not later than Aptian–Albian times) and continued until the end of the Santonian in the Late Cretaceous ( c . 128–83 Ma). A system of half-grabens with mainly south-dipping normal faults developed on the Odessa Shelf at this time. The most profound faulting, accompanied by volcanic activity, occurred in the NE–SW orientated Karkinit-Gubkin rift basin at the boundary between the Eastern European and Scythian platforms. The footwalls of half-grabens were exposed above sea level and subject to erosion at this time. Active extensional processes affected the western part of Azov Sea and, while the onset and cessation of these cannot be tightly constrained, they are compatible with the well constrained results from the Odessa Shelf. (2) The second tectonic stage is one of passive post-rift thermal subsidence that lasted from the Campanian (Late Cretaceous) until the end of the Middle Eocene (83–38.6 Ma). (3) The third stage of basin evolution is one of inversion tectonics in a compressional setting. Discrete inversion events occurred at the end of the Middle Eocene, during the Late Eocene, during the Early Miocene and at Middle Miocene times ( c . 38.6 Ma, c . 35.4 Ma, c . 16.3 Ma, c . 10.4 Ma, respectively) and typical inversion structures developed on the Odessa Shelf, some parts of which were uplifted and significantly eroded (down to the Lower Cretaceous succession). The southern part of the Azov Sea, opening into the northernmost eastern Black Sea basin, subsided rapidly during this time; thereafter, until the Quaternary, rapid subsidence was limited to its southeastern part, which was incorporated into the Indolo-Kuban foreland basin of the Greater Caucasus orogen.