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Šamajová, Lenka, Jozef Hók, Tamás Csibri, Miroslav Bielik, František Teťák, Bibiana Brixová, Ľubomír Sliva, and Branislav Šály. "Geophysical and geological interpretation of the Vienna Basin pre-Neogene basement (Slovak part of the Vienna Basin)." Geologica Carpathica 70, no. 5 (October 1, 2019): 418–31. http://dx.doi.org/10.2478/geoca-2019-0024.
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Abstract The Vienna Basin is situated at the contact of the Bohemian Massif, Western Carpathians, and Eastern Alps. Deep borehole data and an existing magnetotelluric profile were used in density modelling of the pre-Neogene basement in the Slovak part of the Vienna Basin. Density modelling was carried out along a profile oriented in a NW–SE direction, across the expected contacts of the main geological structures. From bottom to top, four structural floors have been defined. Bohemian Massif crystalline basement with the autochthonous Mesozoic sedimentary cover sequence. The accretionary sedimentary wedge of the Flysch Belt above the Bohemian Massif rocks sequences. The Mesozoic sediments considered to be part of the Carpathian Klippen Belt together with Mesozoic cover nappes of Alpine and Carpathian provenance are thrust over the Flysch Belt creating the third structural floor. The Neogene sediments form the highest structural floor overlying tectonic contacts of the Flysch sediments and Klippen Belt as well as the Klippen Belt and the Alpine/Carpathians nappe structures.
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Środoń, Jan. "Diagenetic history of the Podhale flysch basin." Geotourism/Geoturystyka 13, no. 1 (2008): 45. http://dx.doi.org/10.7494/geotour.2008.13.45.
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Kranner, Matthias, Mathias Harzhauser, Fred Rögl, Stjepan Ćorić, and Philipp Strauss. "Biostratigraphic constraints for a Lutetian age of the Harrersdorf Unit (Rhenodanubian Zone): Implication for basement structure of the northern Vienna Basin (Austria)." Geologica Carpathica 70, no. 5 (October 1, 2019): 405–17. http://dx.doi.org/10.2478/geoca-2019-0023.
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Abstract The formations underlying the Neogene infill of the Vienna Basin are still poorly documented. Until now correlation of subsurface lithostratigraphic units with those of the Rhenodanubian nappe system and the Magura nappe system, outcropping at the basin margins, has been based on extrapolations. A recent drilling campaign in the Bernhardsthal oil field of the northern Vienna Basin in Austria reached the pre-Neogene basement and provided cuttings for biostratigraphic and paleoecological analyses. Based on these data, acquired by using detailed micro- and nanno-paleontological analyses, a Lutetian age (middle Eocene) and a bathyal depositional environment for the Flysch of the Harrersdorf Unit was documented. The lithological similarity of the drilling with the Steinberg Flysch Formation of the Greifenstein Nappe and its Lutetian age suggests, that the middle Eocene part of the Harrersdorf Unit represents a continuation of the Greifenstein Nappe of the Rhenodanubian Flysch, rather than a frontal part of the Rača Nappe of the Magura Flysch as previously thought.
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Hnylko, O. M. "GEODYNAMICS." GEODYNAMICS 1(10)2011, no. 1(10) (June 28, 2011): 47–57. http://dx.doi.org/10.23939/jgd2011.01.047.
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The tectonic units of the Carpathians are considered in terms of the terrain analysis. Carpathathian orogen is build up of three main elements: microcontinental terrains, sutures and flysch-molasse accretionary prism. There are two main terrains: a northern ALCAPA and a southern Tisza-Dacia. Sutures (Fore-Marmarosh suture, Pieniny Klippen Belt and others), marking the ancient oceanic basins, bound these terrains. The Flysch Carpathians are regarded as the Cretaceous-Neogene accretionary prism. Growing the prism was caused by the Alpine subduction of the Carpathian Flysch basin basement beneath both the ALCAPA and Tisza-Dacia terrains.
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GOLONKA, JAN, MICHAŁ KROBICKI, ANNA WAŚKOWSKA, MAREK CIESZKOWSKI, and ANDRZEJ ŚLĄCZKA. "Olistostromes of the Pieniny Klippen Belt, Northern Carpathians." Geological Magazine 152, no. 2 (July 25, 2014): 269–86. http://dx.doi.org/10.1017/s0016756814000211.
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AbstractThe olistostromes form two belts within the Pieniny Klippen Belt (PKB) in the Northern Carpathians. They mark an early stage of the development of the accretionary prism. The first belt was formed during Late Cretaceous time as a result of subduction of the southern part of the Alpine Tethys. The fore-arc basin originated along this subduction zone, with synorogenic flysch deposits. Huge olistoliths deposited within the Cretaceous–Palaeogene flysch of the Złatne Basin, presently located in the vicinity of the Haligovce village (eastern Slovakia), provide a good example of the fore-arc olistostrome setting. The second belt is related to the movement of the accretionary prism, which overrode the Czorsztyn Ridge during Late Cretaceous–Paleocene time. The destruction of this ridge led to the formation of submarine slumps and olistoliths along the southern margin of the Magura Basin. The Upper Cretaceous – Paleocene flysch sequences of the Magura Basin constitute the matrix of olistostromes. The large Homole block in the Jaworki village represents the best example of the Magura Basin olistolith. Numerous examples of olistoliths were documented in western Slovakia, Poland, eastern Slovakia and Ukraine. The olistostromes formed within the Złatne and Magura basins orginated during the tectonic process, forming the olistostrome belts along the strike of the PKB structure.
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D’errico, Marco, Angelida Di Staso, Annamaria Fornelli, Domenico Guida, Francesca Micheletti, Vincenzo Perrone, and Giuliana Raffaelli. "The Numidian Flysch: a guide formation for the reconstruction of the paleogeography and tectono-sedimentary evolution of southern Apennines." Bulletin de la Société Géologique de France 185, no. 5 (May 1, 2014): 343–56. http://dx.doi.org/10.2113/gssgfbull.185.5.343.
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Abstract The Numidian Flysch shows constant lithological features from the strait of Gibraltar to central Italy. It is characterized by quartzarenites showing grains of monocrystalline, rounded and frosted quartz, and by kaolinitic mudstones. This research has pointed out that in the southern Apennines 1) the Numidian Flysch was deposited exclusively in the Campania-Lucania carbonate platform and in the Lagonegro-Molise basin, both located on the Apulian continental margin, and never is present in tectonic units originated from the oceanic area located west of that margin; 2) in the axial zone of the Lagonegro basin it stratigraphically follows a formation consisting of varicoloured clays (Argille Varicolori Auct.); 3) its age is limited to the early-middle Langhian, that is to say, it begins to sediment about 7 million years later than in the Maghrebian chain and deposited for a time span limited to 1–1.5 Ma. The thickness of the Numidian Flysch gradually decreases towards the north from about 600–1,000 meters to a few tens of meters and in some of the northeastern outcrops it is represented only by some layers of quartzarenites. This is accompanied by a decrease in size of the particles becoming more and more finer. In addition, northwards and frequently in the same section, a lower mineralogical and textural maturity (from quartzarenites to litharenites, and presence of abundant matrix, sub-angular, polycrystalline and deformed quartz grains) is well recognizable. In the Campania-Lucania carbonate platform the Numidian Flysch evolves to pelagic marly-clayey deposits, followed by mineralogically immature turbidite sandstones of Serravallian age. In the Lagonegro basin the Numidian Flysch replaces Cretaceous-lower Miocene turbidite deposits, consisting of limestones and red marls, on the western side of the basin, variegated clays in the axial zone and calcareous turbidites or variegated clays in the eastern side. Since the late Langhian, it evolves to pelagic sediments followed by lower Tortonian immature turbidite sandstones. In the successions of the Molise basin the Numidian Flysch is interbedded in a succession consisting of calcareous turbidites and pelagic limestones and marls, reaching the Messinian. The lithological features and the age of the Numidian Flysch in central-southern Apennines, therefore, point out an evolution different from that of the Numidian Flysch of the Maghrebian chain. During the early Miocene, a paleogeographic barrier or other unknown obstacles prevent Numidian sands from reaching the south-Apenninic domains. In the early Langhian, the disappearance of these obstacles allows sands to reach the deep basins located on the Apulian margin. In the late Langhian the Numidian sedimentation is canceled and replaced by mainly pelagic sediments, which will evolve to foredeep deposits in the Serravallian-Messinian time span. In addition, the significant presence of feldspathic and lithic grains testifies a double detrital supply: polycyclic quartzose sands and kaolinitic mudstones from the African craton and metamorphic and plutonic grains from the Hercynian or older rocks of the internal units of the southern Apennines. The Numidian Flysch of the southern Apennines allows to assign the tectonic units in which is present to the Campania-Lucania carbonate platform or to different zones of the Lagonegro-Molise basin and therefore is of great importance in the reconstruction of both the Mesozoic-Cenozoic paleogeography and a tectono-sedimentary evolution very difficult to decipher, given the convergence of sedimentary facies in the Apenninic deep basins since Cretaceous to Miocene, the presence of several tectonic phases and of out of sequence and back-thrusts.
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Thum, Laurent, Reto De Paoli, Gérard M. Stampfli, and Patrice Moix. "The Piolit, Pelat and Baiardo Upper Cretaceous flysch formations (western Alps): geodynamic implications at the time of the Pyrenean tectonic phases." Bulletin de la Société Géologique de France 186, no. 4-5 (July 1, 2015): 209–21. http://dx.doi.org/10.2113/gssgfbull.186.4-5.209.
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AbstractThe Piolit, Pelat (French Alps) and Baiardo (Italian Maritime Alps) units contain Upper Cretaceous carbonate turbidites formations, with minor siliciclastic components. They are flysch formations, linked with the Pyrenean compressive events through their ages and their “subbriançonnais” structural position. Sedimentological, mineralogical (heavy minerals), and geochemical analysis, point to a potential “Pyrenean signature” which would testify the Late Cretaceous collision between the Ibero-Briançonnais terrane and the European plate. A “Dauphinois” origin and basin inversion erosion is proposed for the zircon-tourmaline-rutile (ZTR) bearing Piolit flysch, deposited from the Coniacian to the Campanian. A Penninic origin with tectonic inversion and erosion of former tilted blocks of the European margin from the Turonian to the Paleocene is proposed for the ZTR bearing Pelat flysch. Comparison with the Niesen (Swiss Prealps) and La Ciotat (Provence) flysch depositional context, allows to better constrain the Pyrenean compressive event in the Alpine domain. The Senonian part of the Baiardo flysch, that contains a garnet-dominated heavy mineral association and distinct geochemical trends, is allotted to the Liguro-Piemontais domain and to the Alpine collision stricto sensu.
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Atouabat, Achraf, Sveva Corrado, Andrea Schito, Faouziya Haissen, Oriol Gimeno-Vives, Geoffroy Mohn, and Dominique Frizon de Lamotte. "Validating Structural Styles in the Flysch Basin Northern Rif (Morocco) by Means of Thermal Modeling." Geosciences 10, no. 9 (August 19, 2020): 325. http://dx.doi.org/10.3390/geosciences10090325.
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Vitrinite reflectance and a micro-Raman spectroscopy parameters data set have been acquired on dispersed organic matter of the Maghrebian flysch basin and the Tangiers unit across a NE-SW section in the north-western Rif belt (North Morocco). Thermal maturity shows increasing values from the hinterland to the external unit (from NE to SW). Paleo-thermal indicators show that the internal flysch basin (i.e., the Mauretanian unit) is less mature than the external one, (i.e., the Massylian unit), with Ro% and Ro eq. Raman values ranging from 0.64% to 1.02% (from early mature to late mature stages of hydrocarbon generation). 1D thermal modeling estimates the overburden now totally eroded ranging from 3.1 km to 6.0 km, and has been used as constraint to reconstruct the complete thrust wedge geometry in Miocene times. The reconstructed geometry accounts for high shortening (about 63%) due to the development of an antiformal stack in the frontal part of the wedge made up by the flysch succession. This stacking is interpreted as a consequence of the western translation of the Alboran Domain in the core of the Betic-Rif orogenic system.
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González-Bonorino, Gustavo. "Early development and flysch sedimentation in Ordovician Taconic foreland basin, west-central Newfoundland." Canadian Journal of Earth Sciences 27, no. 9 (September 1, 1990): 1247–57. http://dx.doi.org/10.1139/e90-133.
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During the Early to Late Ordovician the Taconic foredeep in west-central Newfoundland evolved from an underfilled to an overfilled state in response to cratonward advance, thickening, and erosion of the Taconic Orogen. Early orogen-derived sediment in the foreland basin consisted of middle(?) to lake Arenigian deep-water mudstones that accumulated on an inner (craton-facing) slope prism (uppermost parts of Shallow Bay and Green Point formations and correlative units). These deposits are interbedded with and overlie passive-margin slope sediments. In the middle Arenigian to early Llanvirnian, sand from the orogen formed several small, sand-rich submarine fans (Lower Head Formation and correlative units) on the lower reaches of the inner slope and basin plain. The fans may have been fed by closely spaced rivers draining the orogen, as presently occurs in western South America. Only proximal portions of these fans are now exposed. The flysch basin was narrow, constricted by the inner slope and the passive-margin slope, and located a short distance seaward from the buried hingeline of the proto-North American craton. As the orogen thickened sufficiently to override the crustal ramp, the carbonate shelf on the craton drowned, clastic depocentres migrated onto the foundered craton, and a thicker flysch (Mainland Sandstone) accumulated in Llanvirnian-Llandeilian time. In the Caradocian the foreland basin was overfilled with shallow-marine terrigenous sediments (Long Point Formation). Regional flysch dispersal was from a St. Lawrence promontory to a Quebec reentrant.
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Francírek, Michal, and Slavomír Nehyba. "Evolution of the passive margin of the peripheral foreland basin: an example from the Lower Miocene Carpathian Foredeep (Czech Republic)." Geologica Carpathica 67, no. 1 (February 1, 2016): 41–68. http://dx.doi.org/10.1515/geoca-2016-0003.
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Abstract The Karpatian deposits of the central part of the Carpathian Foredeep in Moravia, which are deeply buried under the Outer Western Carpathians, provide a unique opportunity to reconstruct the former evolutionary stages of this peripheral foreland basin and its paleogeography. A succession of three depositional units characterized by a distinct depositional environment, provenance, and partly also foreland basin depozone, have been identified. The first depositional unit represents a proximal forebulge depozone and consists of lagoon-estuary and barred coastline deposits. The source from the “local” crystalline basement played here an important role. The second depositional unit consists of coastline to shallow marine deposits and is interpreted as a forebulge depozone. Tidalites recognized within this unit represent the only described tide-generated deposits of the Neogene infill of the Carpathian Foredeep basin in Moravia. The source from the basin passive margin (the Bohemian Massif) has been proved. The third depositional unit is formed by offshore deposits and represents a foredeep depozone. The provenance from both passive and active basin margin (Silesian Unit of the Western Carpathian Flysch Zone) has been proved. Thus, both a stepwise migration of the foredeep basin axis and shift of basin depozones outwards/cratonwards were documented, together with forebulge retreat. The shift of the foreland basin depozones more than 50 km cratonward can be assumed. The renewed thrusting along the basin’s active margin finally completely changed the basin shape and paleogeography. The upper part of the infill was deformed outside the prograding thrust front of flysch nappes and the flysch rocks together with a strip of Miocene sediments were superposed onto the inner part of the basin. The width and bathymetric gradient of the entire basin was changed/reduced and the deposition continued toward the platform. The basin evolution and changes in its geometry are interpreted as a consequence of the phases of the thrust-sheet stacking and sediment loading in combination with sea-level change.
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Ananiadis, G., I. Vakalas, A. Zelilidis, and K. Stoykova. "PALAEOGRAPHIC EVOLUTION OF PINDOS BASIN DURING PALEOGENE USING CALCAREOUS NANNOFOSSILS." Bulletin of the Geological Society of Greece 36, no. 2 (July 23, 2018): 836. http://dx.doi.org/10.12681/bgsg.16831.
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A different basin evolution is suggested between the northern and southern parts of the Pindos basin, based on biostratigraphic dating results. Characteristic nannofossils showed that flysch sedimentation in the whole basin started in the Paleocene and generally finished during the Eocene, with the exception of the Konitsa and Milia areas where sedimentation lasted until Early Oligocene. Although, basin depth increased southwards, Kastaniotikos and Sperchios faults affected the geometry of Pindos basin, creating ridges and troughs within the basin. Due to this segmentation of the basin, the continuity of the sedimentation in the northern part of the study area until Oligocene is suggested. Calcareous nannofossils recovered from this northern part indicate a Paleocene NP5 to early Cligocene (NP20-21) age. On the other hand, in the southern part, sedimentation of flysch was lasted until middle Eocene. According this model, sedimentation in the southern part, stopped during the middle Eocene, was followed by subaerial exposure and the migration of clastic sedimentation to the western part of Pindos zones (Pindos foreland basin of Ionian zone). At this time, in the northern part, a small-restricted basin was continuously active as a piggyback basin from upper Eocene to lower Oligocene and shallow deposits (slope and submarine canyon deposits, delta fan deposits) accumulated.
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ΠΑΠΑΝΙΚΟΛΑΟΥ, Ι. Δ., and Ε. Λ. ΛΕΚΚΑΣ. "Φαινόμενα συνιζηματογενούς τεκτονισμού κατά τη μετάβαση από την ανθρακική στην κλαστική ιζηματογένεση στην Ιόνια ενότητα (περιοχή Μεσολόγγι)." Bulletin of the Geological Society of Greece 34, no. 1 (January 1, 2001): 191. http://dx.doi.org/10.12681/bgsg.17009.
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It is well-known that the sedimentation in the Ionian Unit between the limestones and the flysch succession continued without interruption leading to the formation of relatively thick transitional beds. In this paper, phenomena of syn-sedimentary tectonism are reported for the first time during this grading up from the limestones into the flysch, near the village of Kato Retsina in Mesolongi area. Although, a gradual progression from the limestones to the flysch is also observed, in certain locations there is an abrupt change in the sedimentation. Transitional marly beds are missing and faulting is present. Field evidence indicates that faulting in the area took place during the onset of the flysch deposition. These faults are related to the formation of the graben within the flysch basin and form a characteristic angular shape in the limestone-flysch boundary. As a result, there is a change of dip in the strata towards the boundary involving significant disturbance in the lower members of the flysch succession, where also olistoliths are observed. Similar phenomena have been reported from other geotectonic Units such as Tripoli and Parnassos Units. The latter phenomena are characterized by the transition from neritic carbonate to pelagic clastic sedimentation and partly resulted in immersion, erosion, karstification and emergence so as to receive the flysch sediments. However, the Ionian Unit experienced a pelagic carbonate sedimentation that did not lead to erosion and karstification processes. In that case, the theory of non-deposition is proposed, in a paleoenvironment of steep slopes and strong sea currents. These phenomena depict the influence of the neighboring neritic Gavrovo-Tripolis unit. Overall, the study area is located in tectonic blocks that represent the transition from the neritic platform of Gavrovo to the pelagic Ionian Unit.
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Mattern, Frank. "Mid-Cretaceous basin development, paleogeography, and paleogeodynamics of the western Rhenodanubian Flysch (Alps)." Zeitschrift der Deutschen Geologischen Gesellschaft 150, no. 1 (June 10, 1999): 89–132. http://dx.doi.org/10.1127/zdgg/150/1999/89.
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Francesco, Guerrera, Martín Manuel Martín, Martín-Pérez José A., Martín-Rojas Iván, Miclăuş Crina, and Serrano Francisco. "Tectonic control on the sedimentary record of the central Moldavidian Basin (Eastern Carpathians, Romania)." Geologica Carpathica 63, no. 6 (December 1, 2012): 463–79. http://dx.doi.org/10.2478/v10096-012-0036-0.
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AbstractThe sedimentary record of the Tarcău and Vrancea Nappes, belonging to the flysch accretionary zone of the Eastern Carpathians (Eastern Carpathian Outer Flysch), registered Cretaceous-Miocene events during the evolution of the Moldavidian Basin. Our biostratigraphic data indicate that the deposits studied are younger than previously reported. The comparison of sedimentary record studied with the Late Cretaceous-Early Miocene global eustatic curve indicates that eustatic factor played a secondary role, after the tectonic one. Four main stages of different processes influenced by tectonics are recognized in the sedimentary record: (1) Campanian-Maastrichtian-earliest Paleocene; (2) latest Ypresian-Lutetian; (3) late Chattian-earliest Aquitanian, and (4) late Aquitanian-early Burdigalian. The late Chattian- earliest Aquitanian and late Aquitanian-early Burdigalian records indicate a high tectonic influence. The first event was related to the foredeep stage of the sedimentary domain studied, and the second one to the deformation stage of the same domain. The sedimentary records of tectonic influence recognized during these stages are useful tools for geodynamic reconstructions. The stratigraphic correlation of Tarcău and Vrancea sedimentary records are used
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Sapunov, Ivo, Platon Tchoumatchenco, A. Atanasov, and A. Marinkov. "Central North Bulgaria during the Jurassic." Geologica Balcanica 21, no. 5 (October 30, 1991): 3–68. http://dx.doi.org/10.52321/geolbalc.21.5.3.
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During the Early-Middle Jurassic Central North Bulgaria belonged to the Moesian Early-Middle Jurassic Platform. Even as early as the Hettangian it gradually started sinking. As a result of this a marine ingression started over its lowermost grabens. Within limited areas the marine ingression was preceded by continental accumulation of swamp and lake sediments. The link between the marine basin and the Vardar Ocean was the strait along the Tundža Diagonal Early-Middle Jurassic Fault-Angle Valley (=tilt-block basin) which was orientated towards the southeast-northwest. The fault-angle valley demarcated the Thracian Massif in the west·from the West Pontids in the east, which were presented by the Zlatarski Exotic Ridge and by its northern shelf. Between the Zlatarski Ridge in the south and the Moesian Platform in the north lay the Matorian Early-Middle Jurassic Flysch Trough (Fig. 20). The Early-Middle Jurassic marine transgression gradually spread all over the Moesian Platform to reach its maximum at the end of Callovian. Thus the detached epicontinental basin became a place of terrigenous and terrigenous-carbonate sedimentation, the depths being within the limits of the shelf, i.e. down to about 200 m. From the beginning of Callovian in the marine basin started a stage of bathymetric diferentiation, which was a result of a notable rearrangement of paleotectonic structures. Thus the central part of the homogenous by that time Moesian Early-Middle Jurassic Platform faulted and sank. This led to the differentiation of two independent platforms – the Western Moesian Late Jurassic-Early Cretaceous Carbonate Platform and the Eastern Moesian Late Jurassic-Early Cretaceous Carbonate Platform which were separated by the Central Moesian Late Jurassic-Early Cretaceous Basin. The Niš-Trojan Late Callovian-Valanginian Flysch Trouglt was gradually formed south of them. During the Callovian the Tunža Fault-Angle Valley did not exist any more. As a result of that the Thracian Massif joined the West Pontids and the adjoining Matorids. All these together became a source land to the Niš-Trojan Flysch Trough (Fig. 25). By means of this trough the link to the east with the Vardar Ocean was realized. While over the carbonate platforms the environments were very shallow-water (depths of the order of 10–20 m), in the basin, where pelagic limestones deposited, the depths were of the order of 150–300 m. In the lowermost parts of the flysch trough the depths reached the lower part of the epibathyal, i.e. – 500-600 m.
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Środoń, J., M. Kotarba, A. Biroň, P. Such, N. Clauer, and A. Wójtowicz. "Diagenetic history of the Podhale-Orava Basin and the underlying Tatra sedimentary structural units (Western Carpathians): evidence from XRD and K-Ar of illite-smectite." Clay Minerals 41, no. 3 (September 2006): 751–74. http://dx.doi.org/10.1180/0009855064130217.
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AbstractDiagenesis in the Podhale and Orava Paleogene flysch basins and in the underlying Mesozoic structural units was studied by XRD measurement of the percent smectite in the mixedlayer illite-smectite from shales and K-Ar dating of the illite-smectite from bentonites, supported by XRD quantitative mineral analysis, grain density, and porosity measurements of the bulk shales. The diagenetic mineral reactions identified in the flysch shales include illitization of smectite (>60 to <5%S), dissolution of K-feldspar and kaolinite, crystallization of quartz, albite and chlorite. An unusually large amount of basin history information was obtained by combining the illite-smectite data from wells and from the present erosional surface of the basin.The rocks underwent burial diagenesis at a stable geothermal gradient similar to the present-day value of 21±2°C/km. The maximum burial temperatures were reached very quickly (high sedimentation rate) close to the basin inversion time, at ∼17 Ma in the western part and 18 Ma in the eastern part.The basin floor, which included the present-day Tatra Mts., was inclined towards the East. The thickness of the sedimentary filling of the basin ranged from 3.5–4.5 km in the western Tatra (removed entirely), to 5–6 km in the western Podhale (<3–4 km removed), to 6.5–7.5 km in the eastern Podhale (>4–5 km removed), and even more in the eastern Tatra and Spisská Magura close to the Ružbachy Fault. These data imply a major subsidence followed by uplift of the Podhale plus Tatra block along the Ružbachy Fault and the deposition of a thick sequence of Lower Miocene sediments over the entire area (latter removed by erosion).The Mesozoic rocks of all the structural units underlying the flysch basin underwent advanced diagenesis (maximum palaeotemperatures of 160–270°C) during an Upper Cretaceous tectonic burial event at ∼80–90 Ma. The tectonic overload was removed before the Eocene transgression (49–42 Ma).
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da Silva Guimarães, Ewerton, Romain Delunel, Fritz Schlunegger, Naki Akçar, Laura Stutenbecker, and Marcus Christl. "Cosmogenic and Geological Evidence for the Occurrence of a Ma-Long Feedback between Uplift and Denudation, Chur Region, Swiss Alps." Geosciences 11, no. 8 (August 12, 2021): 339. http://dx.doi.org/10.3390/geosciences11080339.
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We used concentrations of in situ cosmogenic 10Be from riverine sediment to quantify the basin-averaged denudation rates and sediment fluxes in the Plessur Basin, Eastern Swiss Alps, which is a tributary stream to the Alpine Rhine, one of the largest streams in Europe. We complement the cosmogenic dataset with the results of morphometric analyses, geomorphic mapping, and sediment fingerprinting techniques. The results reveal that the Plessur Basin is still adjusting to the landscape perturbation caused by the glacial carving during the Last Glacial Maximum c. 20,000 years ago. This adjustment has been most efficient in the downstream part where the bedrock comprises high erodibility North Penninic flysch and Bündnerschist, whereas glacial landforms are still prominently preserved in the upstream region, comprising low erodibility South Penninic and Austroalpine bedrock. This geomorphic observation is supported by the 10Be based denudation rate and sediment provenance analysis, which indicate a much faster sediment production in the flysch and schist lithologies. Interestingly, the reach of fast denudation has experienced the highest exhumation and rock uplift rates. This suggests that lithologic and glacial conditioning have substantially contributed to the local uplift and denudation as some of the driving forces of a positive feedback system.
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Elison, Mark W., and Robert C. Speed. "Structural development during flysch basin collapse: the fencemaker allochthon, East Range, Nevada." Journal of Structural Geology 11, no. 5 (January 1989): 523–38. http://dx.doi.org/10.1016/0191-8141(89)90085-0.
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Boncheva, Iliana, Ivan Zagorchev, and Emil Goranov. "New data on the Treklyano Group (Jurassic): sections Propast and Gorna Glogovitsa (Southwest Bulgaria)." Geologica Balcanica 34, no. 3-4 (December 30, 2004): 45–70. http://dx.doi.org/10.52321/geolbalc.34.3-4.45.
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The sections Propast and Gorna Glogovitsa exhibit the transitions between the axial parts (radiolariteshale interbedding) of the Treklyano Jurassic trough and its eastern boundary with the terrigenous-carbonate successions of "Balkanide" type. The section Propast has a complex imbricated structure, and the separate thrust sheets exhibit different basin environments. Rich radiolarian assemblages are determined, and their concurrent ranges allow for a more precise biostratigraphic analysis and chronostratigraphic conclusions. The lowermost parts of the Treklyano Group are referred to the upper parts of the Lower Jurassic and the lowermost parts of the Middle Jurassic. Important changes in the sedimentation regime probably began at the end of Callovian time and in Late Jurassic times with gradual influx (most pronounced in Kimmeridgian – Tithonian times) of gravity flows. The latter contain transported Middle Jurassic radiolarite-shale packets (olistolites). Thus, a transition from the evolution of the Treklyano trough towards the onset and evolution of the Late Jurassic – Early Cretaceous Nish-Troyan flysch trough has locally taken place. Laterally, the flysch trough has been superimposed over shallower zones of the Jurassic basin.
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Su, Wen, Shutong Xu, Laili Jiang, and Yican Liu. "Coesite from quartz-jadeitite in the Dabie Mountains, Eastern China." Mineralogical Magazine 60, no. 401 (August 1996): 659–62. http://dx.doi.org/10.1180/minmag.1996.060.401.12.
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The Dabie Mountains is a collisional orogen between the North China and Yantze Continental plates. It is composed, from south to north, of the foreland fold and thrust belt alternated with molasse basin, the subducted cover and basement of the Yangtze continental plate, the meta-ophiolitic melange belt, the forearc meta-flysch nappe (bounded by southward and northward thrust belts) in which there may be a buried volcanic arc and a relict back-arc basin (Fig. 1A) (Xu et al., 1992a, 1994).
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Nehyba, Slavomír, Marie Adamová, Jiří Faimon, Tomáš Kuchovský, Ivan Holoubek, and Josef Zeman. "Modern fluvial sediment provenance and pollutant tracing: a case study from the Dřevnice River Basin (eastern Moravia, Czech Republic)." Geologica Carpathica 61, no. 2 (April 1, 2010): 147–62. http://dx.doi.org/10.2478/v10096-010-0007-2.
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Modern fluvial sediment provenance and pollutant tracing: a case study from the Dřevnice River Basin (eastern Moravia, Czech Republic)Modern fluvial deposits of a small fluvial system were studied in the area of eastern Moravia (Czech Republic) with the aim of determining the provenance of the deposits and weathering processes. Identification of the source rocks and their alongstream variations were used for the evaluation of the natural or anthropogenic source of the heavy metals. Paleogene flysch sandstones, flysch mudstones and Quaternary loesses represent source rocks and reflect both the role of recycling and local sources. Provenance from sandstones dominate upstream whereas mudstones represent dominant source rock in the downstream part of the fluvial system. The contents of Pb and Zn are highly enhanced when compared with the natural background in the entire study area. Their anthropogenic source is connected with the rubber/shoe manufacturing industry and traffic. The contents of Cr, Co, Cu, Ni and V are usually lower in modern deposits than in the identified source rocks.
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Puglisi, Diego. "Tectonic evolution of the Sicilian Maghrebian Chain inferred from stratigraphic and petrographic evidences of Lower Cretaceous and Oligocene flysch." Geologica Carpathica 65, no. 4 (August 1, 2014): 293–305. http://dx.doi.org/10.2478/geoca-2014-0020.
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Abstract The occurrence of a Lower Cretaceous flysch group, cropping out from the Gibraltar Arc to the Balkans with a very similar structural setting and sedimentary provenance always linked to the dismantling of internal areas, suggests the existence of only one sedimentary basin (Alpine Tethys s.s.), subdivided into many other minor oceanic areas. The Maghrebian Basin, mainly developed on thinned continental crust, was probably located in the westernmost sector of the Alpine Tethys. Cretaceous re-organization of the plates triggered one (or more) tectonic phases, well recorded in almost all the sectors of the Alpine Tethys. However, the Maghrebian Basin seems to have been deformed by Late- or post-Cretaceous tectonics, connected with a “meso-Alpine” phase (pre-Oligocene), already hypothesized since the beginning of the nineties. Field geological evidence and recent biostratigraphic data also support this important meso- Alpine tectonic phase in the Sicilian segment of the Maghrebian Chain, indicated by the deformations of a Lower Cretaceous flysch sealed by Lower Oligocene turbidite deposits. This tectonic development is emphasized here because it was probably connected with the onset of rifting in the southern paleomargin of the European plate, the detaching of the so-called AlKaPeCa block (Auct.; i.e. Alboran + Kabylian + Calabria and Peloritani terranes) and its fragmentation into several microplates. The subsequent early Oligocene drifting of these microplates led to the progressive closure of the Maghrebian Basin and the opening of new back-arc oceanic basins, strongly controlled by extensional processes, in the western Mediterranean (i.e. Gulf of Lion, Valencia Trough, Provençal Basin and Alboran Sea).
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Tevelev, Al V., A. V. Tevelev, I. A. Prudnikov, A. O. Khotylev, E. E. Baraboshkin, and S. S. Popov. "Structural parageneses of flysch complexes in the central part of the Uralian Foreland basin." Moscow University Bulletin. Series 4. Geology, no. 3 (June 28, 2016): 11–16. http://dx.doi.org/10.33623/0579-9406-2016-3-11-16.
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In this work we reported the structural characteristics of the late Paleozoic flysch formation in the central part of the Uralian foreland basin. Three types of structural associations specific for thrust zones are established there. These include: 1) asymmetrical to recumbent west-vergent folds; 2) re-structured tectonic melange; 3) local thrusts, zone of schystosity, flat tectonic mirrors. Generally structural elements strike approximately parallel to the regional Karantrav thrust; orientation of striking ranges from the northwest to the northeast, accordingly to tectonic heterogeneity of the allochtone.
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Gregou, Sophia, Nikolaos Solakius, and Fotini Pomoni-Papaioannou. "The carbonate-flysch transition (late Maastrichtian-late Palaeocene) in the Arachova sequence of the Parnassus-Ghiona Zone, central Greece." Geological Magazine 131, no. 6 (November 1994): 819–36. http://dx.doi.org/10.1017/s0016756800012887.
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AbstractThe transition from the carbonate to the flysch facies in the Arachova sequence of the Parnassus-Ghiona Zone is represented by argillaceous limestone beds with flaser structures deposited during latest Maastrichtian-Palaeocene time in a pelagic carbonate environment with a periodic clastic influx. Deposition was continuous except for a short interruption during the K/T boundary interval and the earliest Palaeocene when the area was subaerially exposed. This interruption gave rise to the development of a brecciated carbonate horizon through soil-forming processes. The mineralogical composition of the clastic influx (i.e. quartz, feldspars, clay minerals, amorphous iron oxides, amorphous phosphatic compounds), in particular the clay mineral assemblages (i.e. illite, chlorite, irregularly interstratified illite-vermiculite), shows that the clastic supply represents erosional material that originated from a tectonically active continental setting of both carbonate and clastic rocks, presumably the Pelagonian Zone, as for the flysch of the Beotian and Sub-Pelagonian Zones. The arrival of the first clastic material in the Arachova area as early as latest Maastrichtian time, its Pelagonian origin and the persistence of pelagic conditions of sedimentation throughout the Palaeocene, indicate that the Arachova area was situated along the northeastern margin of the Parnassus platform and that it subsided into the Beotian basin. While the central areas of the platform remained tectonically stable during middle Palaeocene times and there was an extensive development of stromatolites, the northeastern marginal areas transitional to the Beotian basin continued to subside allowing pelagic carbonate sedimentation with periods of clastic influx. The total collapse of the platform in the late Palaeocene gave rise to the deposition of the flysch over the entire zone.
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Hnylko, O., V. Shevchuk, T. Bozhuk, M. Bogdanova, and S. Hnylko. "GEOLOGICAL/GEOTOURIST OBJECTS OF THE TRANSCARPATHIAN REGION AS A REFLECTION OF THE GEOLOGICAL HISTORY OF THE CARPATHIANS." Visnyk of Taras Shevchenko National University of Kyiv. Geology, no. 4 (87) (2019): 6–13. http://dx.doi.org/10.17721/1728-2713.87.01.
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Consideration is given to description of important geological objects (observation points) of the southern slope of the Carpathians as reflections of sedimentary, paleogeographic and paleogeodynamic history of the Carpathians formation. Method. Standard method of geological description of outcrops, elements of sedimentological analysis of structural and textural features of rocks, and micropaleontological method are used. Results. A number of key geological objects that reflect the important stages of the geological evolution of the Carpathians in the Transcarpathian region near highways is described. These objects (the observation points in the article) can be represented as geotourist ones. In the first location which is in Yablunytsa Pass, an outcrop of Oligocene "striped" Holovets Limestone; further, along the Trostyanets Stream – Jurrassic pillow-lavas in the front of the Burkut Nappe; along the Kamyanyi Potik Stream – Jurassic- Early Cretaceous volcanogenic-sedimentary succession of the Kamyanyi Potik Nappe; along the Kosivka River – Eocene marls of the Marmarosh Massif sedimentary cover and the Inner Carpathian flysch of the Monastyrets Nappe; in the area of Novoselytsya village in the basin of the Luzhanka River – the Jurassic-Paleogene deposits of the Pieniny Klippen Belt; along the riverbed Tereblya in Zabrid village – Cretaceous-Paleogene deposits of the Marmarosh Klippen Zone are traced. Scientific novelty. The characteristic of a number of geological objects of the Transcarpathian region is supplemented and detailed and their brief description as reflections of sedimentary, paleogeographic and paleogeodynamic history of the Carpathians is presented. These objects reflect subsequent geological events: the birth of the Carpathian sedimentary basin; the formation of sub-oceanic and oceanic crust of the Outer Carpathian Flysch Basin; the formation of Inner Eastern Carpathian nappes and their destruction due to the formation of Early Cretaceous olistostrome of the Maramorosh Klippen Zone; ForeMarmarosh and Pieniny Klippen Belt accretionary prisms growing; and the final Oligocene stage of the Outer Carpathian Basin development. In addition, the range of Paleocene-Eocene paleogeographic elements such as (from the East to the West): (a) the passive margin of the Tisza-Dacia – (b) the deep-water Inner Carpathian Flysch Basin – (c) the Pieniny active edge of the Alcapa Terrane is demonstrated. The route of the geological tour described in the article is recommended to get acquainted with the main features of Geology, Geodynamics and processes of formation of the Carpathians. It can be used for further development of geotourism in the Carpathians.
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Buzek, Ladislav. "Factors of Accelerated Erosion in the Southern Mountain Hinterland of the Ostrava Industrial Agglomeration." Geografie 101, no. 3 (1996): 211–24. http://dx.doi.org/10.37040/geografie1996101030211.
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Erosion of soils is becoming a serious problem in forested mountain areas where the natural and even the anthropogenic influences are favourable to this process (Flysch substratum, rainfalls, declivity of slopes and tractors and other machines for forest work). The regime of the suspended matter in the basins in the central and eastern parts of the Moravskoslezské Beskydy Mts. - the Upper Ostravice R. (72,96 km2) and in the Lomná R. (70,40 km2) were compared. The results show that the erosional processes in the basin of the Upper Ostravice R are more intensive than in the basin of the Lomná R., due to the prevailance of shales in the substratum of the basin of the Ostravice R.
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Yılmaz, Yücel. "Geological correlation between northern Cyprus and southern Anatolia." Canadian Journal of Earth Sciences 58, no. 7 (July 2021): 640–57. http://dx.doi.org/10.1139/cjes-2020-0129.
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The island of Cyprus constitutes a fragment of southern Anatolia separated from the mainland by left-oblique transtension in late Cenozoic time. However, a geological framework of offset features of south-central Anatolia, for comparison of Cyprus with a source region within and west of the southeastern Anatolian suture zone, has not yet been developed. In this paper, I enumerate, describe, and compare a full suite of potentially correlative spatial and temporal elements exposed in both regions. Northern Cyprus and south-central Anatolia have identical tectonostratigraphic units. At the base of both belts, crop out ophiolitic mélange – accretionary complex generated during the northward subduction of the Neo-Tethyan Oceanic lithosphere from the Late Cretaceous until the end of middle Eocene. The nappes of the Taurus carbonate platform were thrust above this internally chaotic unit during late Eocene. They began to move as a coherent nappe pile from that time onward. An asymmetrical flysch basin was formed in front of this southward-moving nappe pile during the early Miocene. The nappes were then thrust over the flysch basin fill and caused its tight folding. Cyprus separated from Anatolia in the Pleistocene–Holocene when transtensional oblique faults with dip-slip components caused the development of the Adana and Iskenderun basins and the separation of Cyprus from Anatolia.
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Martín-Martín, Manuel, Francesco Guerrera, Crina Miclăuș, and Mario Tramontana. "Similar Oligo-Miocene tectono-sedimentary evolution of the Paratethyan branches represented by the Moldavidian Basin and Maghrebian Flysch Basin." Sedimentary Geology 396 (February 2020): 105548. http://dx.doi.org/10.1016/j.sedgeo.2019.105548.
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LENAZ, DAVIDE, VADIM S. KAMENETSKY, and FRANCESCO PRINCIVALLE. "Cr-spinel supply in the Brkini, Istrian and Krk Island flysch basins (Slovenia, Italy and Croatia)." Geological Magazine 140, no. 3 (May 2003): 335–42. http://dx.doi.org/10.1017/s0016756803007581.
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In Late Cretaceous times, subduction of oceanic crust occurred to the north of the Adria plate and was followed by the formation of ophiolitic complexes. Continental collision in Alpine orogenic belts lasted from Late Cretaceous to Early Tertiary times. The progressive contraction of oceanic crust caused the uplift of previously rifted continental margin and platforms and the formation of foredeep flysch basins. Detrital Cr-spinels are widespread in Eocene sandstones of the Brkini, Istrian and Krk Island foredeep flysch basins. On the basis of their TiO2 content and FeO/Fe2O3 ratio, spinels derived from peridotites and mantle-derived magmatic rocks were distinguished. The first are statistically more abundant and are considered to have been derived from type I and II peridotites. The second appear to be mainly related to backarc basin products. These results suggest that Cr-spinels were derived from the erosion of the Internal Dinarides, where type II and III peridotites are present, and also from the Outer Dinarides, where type I peridotites crop out.
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Tchoumatchenco, Platon, and Ivo Sapunov. "Intraplate tectonics in the Bulgarian part of the Moesian Platform during the Jurassic." Geologica Balcanica 24, no. 3 (June 30, 1994): 3–12. http://dx.doi.org/10.52321/geolbalc.24.3.3.
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The Moesian Platform was built during the Early and Middle Jurassic by few block structures – grabens and horsts. It subsided slowly, which controlled a progressive marine transgression. In the beginning the sea ingressed in the negative structures, and at the end of the the Middle Jurassic it covered even the highest horsts. Shallow water terrigenous and terrigenous-carbonate sedimentation was ubiquitous. During the Late Callovian and the Late Jurassic a considerable reorganization in the structure of the platform began. Three big blocks were differentiated, and namely, the West and East Moesian Carbonate Platforms, separated by the Central Moesian Basin (with pelagic carbonate sedimentation). The Perimoesian Zone in the South was characterized by thinner continental crust. During the Early and the Middle Jurassic its eastern part was occupied by a flysch trough (the Matorids), and the Nis-Troyan Flysch Trough was differentiated in the Perimoesian Zone. The principal source of alimentation was the Thracian Massif.
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Putiš, Marián, Ondrej Nemec, Martin Danišík, Fred Jourdan, Ján Soták, Čestmír Tomek, Peter Ružička, and Alexandra Molnárová. "Formation of a Composite Albian–Eocene Orogenic Wedge in the Inner Western Carpathians: P–T Estimates and 40Ar/39Ar Geochronology from Structural Units." Minerals 11, no. 9 (September 9, 2021): 988. http://dx.doi.org/10.3390/min11090988.
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The composite Albian–Eocene orogenic wedge of the northern part of the Inner Western Carpathians (IWC) comprises the European Variscan basement with the Upper Carboniferous–Triassic cover and the Jurassic to Upper Cretaceous sedimentary successions of a large oceanic–continental Atlantic (Alpine) Tethys basin system. This paper presents an updated evolutionary model for principal structural units of the orogenic wedge (i.e., Fatricum, Tatricum and Infratatricum) based on new and published white mica 40Ar/39Ar geochronology and P–T estimates by Perple_X modeling and geothermobarometry. The north-directed Cretaceous collision led to closure of the Jurassic–Early Cretaceous basins, and incorporation of their sedimentary infill and a thinned basement into the Albian–Cenomanian/Turonian accretionary wedge. During this compressional D1 stage, the subautochthonous Fatric structural units, including the present-day higher Infratatric nappes, achieved the metamorphic conditions of ca. 250–400 °C and 400–700 MPa. The collapse of the Albian–Cenomanian/Turonian wedge and contemporary southward Penninic oceanic subduction enhanced the extensional exhumation of the low-grade metamorphosed structural complexes (D2 stage) and the opening of a fore-arc basin. This basin hemipelagic Coniacian–Campanian Couches-Rouges type marls (C.R.) spread from the northern Tatric edge, throughout the Infratatric Belice Basin, up to the peri-Pieniny Klippen Belt Kysuca Basin, thus tracing the south-Penninic subduction. The ceasing subduction switched to the compressional regime recorded in the trench-like Belice “flysch” trough formation and the lower anchi-metamorphism of the C.R. at ca. 75–65 Ma (D3 stage). The Belice trough closure was followed by the thrusting of the exhumed low-grade metamorphosed higher Infratatric complexes and the anchi-metamorphosed C.R. over the frontal unmetamorphosed to lowest anchi-metamorphosed Upper Campanian–Maastrichtian “flysch” sediments at ca. 65–50 Ma (D4 stage). Phengite from the Infratatric marble sample SRB-1 and meta-marl sample HC-12 produced apparent 40Ar/39Ar step ages clustered around 90 Ma. A mixture interpretation of this age is consistent with the presence of an older metamorphic Ph1 related to the burial (D1) within the Albian–Cenomanian/Turonian accretionary wedge. On the contrary, a younger Ph2 is closely related to the late- to post-Campanian (D3) thrust fault formation over the C.R. Celadonite-enriched muscovite from the subautochthonous Fatric Zobor Nappe meta-quartzite sample ZI-3 yielded a mini-plateau age of 62.21 ± 0.31 Ma which coincides with the closing of the Infratatric foreland Belice “flysch” trough, the accretion of the Infratatricum to the Tatricum, and the formation of the rear subautochthonous Fatricum bivergent structure in the Eocene orogenic wedge.
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Ivanik, О. M. "GEOLOGICAL-GEOMORPHOLOGICAL FACTORS OF LANDSLIDE FORMATION IN THE CHERNIY CHEREMOSH RIVER BASIN (FLYSCH CARPATHIANS)." Geological Journal, no. 1 (February 15, 2010): 97–107. http://dx.doi.org/10.30836/igs.1025-6814.2010.1.221190.
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Piper, J. D. A., M. T. Elliot, and B. C. Kneller. "Anisotropy of magnetic susceptibility in a Palaeozoic flysch basin: the Windermere Supergroup, northern England." Sedimentary Geology 106, no. 3-4 (November 1996): 235–58. http://dx.doi.org/10.1016/s0037-0738(96)00011-5.
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PIEŃKOWSKI, GRZEGORZ, and EWA WESTWALEWICZ-MOGILSKA. "Trace fossils from the Podhale Flysch Basin, Poland - an example of ecologically-based lithocorrelation." Lethaia 19, no. 1 (January 1986): 53–65. http://dx.doi.org/10.1111/j.1502-3931.1986.tb01900.x.
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Maurizot, Pierre. "First sedimentary record of the pre-obduction convergence in New Caledonia: formation of an Early Eocene accretionary complex in the north of Grande Terre and emplacement of the ‘Montagnes Blanches’ nappe." Bulletin de la Société Géologique de France 182, no. 6 (November 1, 2011): 479–91. http://dx.doi.org/10.2113/gssgfbull.182.6.479.
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Abstract New Caledonia lies at the northern tip of the Norfolk ridge, a continental fragment separated from the east Gondwana margin during the Late Cretaceous. Stratigraphic data for constraining the convergence that led to ophiolitic nappes being obducted over Grande Terre during the Eocene are both few and inaccurate. To try and fill this gap and determine the onset of the convergence, we investigated the lithology, sedimentology, biostratigraphy and geodynamic context of the Late Cretaceous – Palaeogene sedimentary cover-rock succession of northern New Caledonia. We were able to establish new stratigraphic correlations between the sedimentary units, which display large southwest-verging overfolds detached along a basal argillite series, and reinterpret their interrelationships. The sediments from the Cretaceous-Paleocene interval were deposited in a post-rift pelagic environment and are mainly biogenic with minimal terrigenous input. From the base up, they comprise black organic-rich sulphide-bearing argillite, black chert (silicified equivalent of the argillite), micritic with chert, and micrite rich in planktonic foraminifera. These passive-margin deposits are found regionally on the Norfolk Ridge down to New Zealand, and on the Lord Howe Rise, and were controlled primarily by regional or global environmental factors. The overlying Eocene deposits mark a change to an active-margin regime with distal calciturbidite and proximal breccia representing the earliest Paleogene flysch-type deposits in New Caledonia. The change from an extensional to a compressive regime marks the beginning of the pre-obduction convergence and can be assigned fairly accurately in the Koumac–Gomen area to the end of the Early Eocene (Late Ypresian, Biozone E7) at c 50 Ma. From this period on, the post-Late Cretaceous cover in northern New Caledonia was caught up and recycled in a southwest-verging accretionary complex ahead of which flysch was deposited in a flexural foreland basin. The system prograded southwards until the Late Eocene collisional stage, when the continental Norfolk ridge entered the convergence zone and blocked it. At this point the autochthonous and parautochthonous sedimentary cover and overlying flysch of northern New Caledonia was thrust over the younger flysch to the south to form a newly defined allochthonous unit, the ‘Montagnes Blanches’ nappe, that is systematically intercalated between the flysch and the obducted ophiolite units throughout Grande Terre.
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Cumberpatch, Zoë A., Ian A. Kane, Euan L. Soutter, David M. Hodgson, Christopher A.-L. Jackson, Ben A. Kilhams, and Yohann Poprawski. "Interactions between deep-water gravity flows and active salt tectonics." Journal of Sedimentary Research 91, no. 1 (January 31, 2021): 34–65. http://dx.doi.org/10.2110/jsr.2020.047.
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ABSTRACTBehavior of sediment gravity flows can be influenced by seafloor topography associated with salt structures; this can modify the depositional architecture of deep-water sedimentary systems. Typically, salt-influenced deep-water successions are poorly imaged in seismic reflection data, and exhumed systems are rare, hence the detailed sedimentology and stratigraphic architecture of these systems remains poorly understood.The exhumed Triassic (Keuper) Bakio and Guernica salt bodies in the Basque–Cantabrian Basin, Spain, were active during deep-water sedimentation. The salt diapirs grew reactively, then passively, during the Aptian–Albian, and are flanked by deep-water carbonate (Aptian–earliest Albian Urgonian Group) and siliciclastic (middle Albian–Cenomanian Black Flysch Group) successions. The study compares the depositional systems in two salt-influenced minibasins, confined (Sollube basin) and partially confined (Jata basin) by actively growing salt diapirs, comparable to salt-influenced minibasins in the subsurface. The presence of a well-exposed halokinetic sequence, with progressive rotation of bedding, beds that pinch out towards topography, soft-sediment deformation, variable paleocurrents, and intercalated debrites indicate that salt grew during deposition. Overall, the Black Flysch Group coarsens and thickens upwards in response to regional axial progradation, which is modulated by laterally derived debrites from halokinetic slopes. The variation in type and number of debrites in the Sollube and Jata basins indicates that the basins had different tectonostratigraphic histories despite their proximity. In the Sollube basin, the routing systems were confined between the two salt structures, eventually depositing amalgamated sandstones in the basin axis. Different facies and architectures are observed in the Jata basin due to partial confinement.Exposed minibasins are individualized, and facies vary both spatially and temporally in agreement with observations from subsurface salt-influenced basins. Salt-related, active topography and the degree of confinement are shown to be important modifiers of depositional systems, resulting in facies variability, remobilization of deposits, and channelization of flows. The findings are directly applicable to the exploration and development of subsurface energy reservoirs in salt basins globally, enabling better prediction of depositional architecture in areas where seismic imaging is challenging.
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Comeau, F. A., D. Kirkwood, M. Malo, E. Asselin, and R. Bertrand. "Taconian mélanges in the parautochthonous zone of the Quebec Appalachians revisited: implications for foreland basin and thrust belt evolution." Canadian Journal of Earth Sciences 41, no. 12 (December 1, 2004): 1473–90. http://dx.doi.org/10.1139/e04-083.
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In the Quebec Appalachians, disruption, imbrication, and thrusting of the Taconian foreland basin sequence are responsible for the development of chaotic units within the turbiditic sequence of the Caradocian Sainte-Rosalie Group, the main lithologic assemblage of the parautochthonous zone. These chaotic units have been termed olistostromes or tectonosomes on the basis of field criteria and following Pini's (1999) classification. Olistostromal units containing blocks of the middle mudstone (Utica Shale) and upper turbidite units (Ste-Rosalie Group) of the foreland basin and spanning the Caradocian N. gracilis, C. americanus, O. ruedemanni, and C. spiniferus graptolite zones were deposited and incorporated into the Sainte-Rosalie Group. Disruption of more competent beds of the flyschic sequence and fault stacking and slicing of older rock units occurred along major thrust faults and now form structurally aligned corridors or tectonosomes. Graptolites and new chitinozoan data from both olistostromes and tectonosomes indicate older ages (early Late Ordovician) than the flysch units of Sainte-Rosalie Group (mid Late Ordovocian). Lithological, stratigraphic, and structural criteria indicate that tectonosome slices are imbricated foreland basin rocks that are correlative to the Black River, Trenton, Utica, Sainte-Rosalie, and Lorraine groups of the Laurentian platform. Thermal maturation data indicates that disruption of the autochthonous sequence, and folding and thrusting of the entire foreland basin sequence, must have occurred shortly after their deposition. Contrary to what had been suggested, blocks in the olistostromes and tectonosomes were not derived from the allochthonous Chaudière thrust sheet, even though it presently marks the southern contact with the parautochthonous zone. Imbrication of the foreland basin sequence must have occurred before emplacement of the Chaudière thrust sheet.
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Prekopová, Marta, and Juraj Janočko. "Quantitative approach in environmental interpretations of deep-marine sediments (Dukla Unit, Western Carpathian Flysch Zone)." Geologica Carpathica 60, no. 6 (December 1, 2009): 485–94. http://dx.doi.org/10.2478/v10096-009-0035-y.
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Quantitative approach in environmental interpretations of deep-marine sediments (Dukla Unit, Western Carpathian Flysch Zone)In structurally complicated terranes with outcrops limited in number and extent, additional methods for interpreting depositional environments are required. Statistical analysis of bed thicknesses, in addition to conventional sedimentological analysis, is a quantitative way to refine environmental interpretations, interpretations that can be useful in predicting reservoir architecture. We analysed Paleogene deep-water sediments belonging to the Cisna, Sub-Menilite, and Menilite Formations of the Dukla Unit, Outer Carpathian Flysch Zone and, using two independent quantitative methods, tried to define their depositional environments. As a first approach we used Carlson & Grotzinger's model (2001), which suggests power law distribution of turbidite bed thicknesses. The second one is the lognormal mixture model of Talling (2001). Based on a quantitative approach, we suggest deposition of the lowermost Cisna Formation in the channel-levee environment. The overlying sediments of the Sub-Menilite Formation were deposited in a more distal, probably outer lobe environment. The uppermost Menilite Formation is interpreted as deposits from an outer lobe/basin plain environment.
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Drinia, Hara. "Palaeoenvironmental reconstruction of the Oligocene Afales Basin, Ithaki island, western Greece." Open Geosciences 1, no. 1 (January 1, 2009): 1–18. http://dx.doi.org/10.2478/v10085-009-0001-z.
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AbstractAssemblages of benthic foraminifera from one clastic succession in the Afales Basin (Ithaki Island, western Greece) were investigated to reconstruct palaeoenvironmental conditions during the Oligocene. The section consists of alternating hemipelagic marls and detrital deposits, designated as flysch-like beds, attributed to biostratigraphic Zones P20 and P21. Planktic percentages are mostly high (66–80%). Benthic foraminiferal assemblages comprise calcareous and agglutinated taxa (up to 15%). The prevalence of epifaunal foraminifera indicates good ventilation of the bottom water resulting from basin morphology, which enabled the undisturbed flow of water throughout the basin. Palaeodepth estimates imply bathyal deposition, from about 800 to 1200 m deep. The benthic foraminiferal fauna is of high diversity along the section, as is expected in deep marine environments. The abundances of the most common foraminiferal taxa (Cibicidoides spp., Oridorsalis umbonatus, Gyroidinoides spp., Stilostomella spp., Nodosariidae, Nuttallides umbonifera) are quite variable and imply generally oligotrophic to mesotrophic environmental conditions with variable organic flux.
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Egger, Hans, Mandana Homayoun, and Wolfgang Schnabel. "Tectonic and climatic control of Paleogene sedimentation in the Rhenodanubian Flysch basin (Eastern Alps, Austria)." Sedimentary Geology 152, no. 3-4 (October 2002): 247–62. http://dx.doi.org/10.1016/s0037-0738(02)00072-6.
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Vacondios, I., G. Konstantopoulou, and St Karadassi. "The contribution of clay minerals in the landslides occurrence within Pindos flysh formation." Bulletin of the Geological Society of Greece 40, no. 4 (January 1, 2007): 1741. http://dx.doi.org/10.12681/bgsg.17106.
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An engineering geological investigation of the "Potamouli" area located west of Grevena town, for a water dam foundation, has revealed some geotechnical problems related to landslide phenomena. Landslides are of limited extent in the reservoir area, but significant instabilities were identified within the broad catchment basin. The basin is built up mainly by the chaotic unit of Pindos flysch formation, which consists of a silty clayey matrix with heterogeneous inclusions of rock masses in diverse frequency and size. In order to investigate the major contributing factors to landslide occurrence, several physical properties were measured, with the results suggesting that the overall mechanical behaviour of the unit is determined by the clay matrix properties. The mineral composition of the less than two micron fraction of this material was determined by X-ray diffraction. The clay minerals present are illite and montmorillonite. The percentage of montmorillonite reaches the 10% of the matrix fraction and may exert great influence upon the Atterberg limits, swelling, water adsorption, and shrinkage of the matrix material. Montmorillonite absorbs water between its individual silicate layers with resulting high swelling and low frictional resistance becoming by itself a contributing factor to the failures. The presence of expandable clay minerals within the chaotic unit of the Pindos flysh, may indicate that the remove of loose soil cover from the slopes of the reservoir area during the construction of the dam, may be inadequate for preventing future landslides, and a sealing up process may be needed.
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ΛΥΚΟΥΔΗ, Ε. "Geomorphic evolution of the upper reaches of the drainage basin of Acheloos river." Bulletin of the Geological Society of Greece 34, no. 1 (January 1, 2001): 397. http://dx.doi.org/10.12681/bgsg.17333.
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The scope of this study work is to give an insight into the dynamic processes which shape the relief in the drainage basin of the upper reaches the Acheloos river, so that the geomorphological and geodynamical evolution of the region in the past can be approached, together with a possible prediction. For this reason, the relationships between the relief and the endogenic and exogenic factors are sought. The investigated area is made up of geological formations that belong to the zones: "Ionian" (inner Ionian zone), "Gavrovo", "Pindos" and "Hyperpindos". There are also younger rocks (postalpine formations), together with some volcanic rocks. The main stream segment of Acheloos river was formed in the Upper-Middle Miocene, after the deposition of the flysch of "Gavrovo" and the tectonism of the zone. The structures were cut to a large extent by trace-slip faults, striking ENE-WSW, during the Middle-Upper Miocene. At the same time (Lower Miocene - Plio-Quaternary), in NW-Greece, is observed a horizontal clockwise rotation (45°). Finally, the region shows an expanding movement from North to South. Due to the above tectonic activity, the drainage basin shows a monoclinic structure with a westward displacement of the drainage pattern. The displacement increases from North to South. The displacement of the drainage pattern is also favoured by the presence of erodible rocks in the western part (flysch of "Gavrovo") and the general eastward dip of the strata. Neotectonic activity controls the river up to date, as it is inferred from the orientation of the stream segments, which follow the tectonic structure (lithological boundaries, faults, thrusts). The drainage pattern appears to be in an early mature stage. According to the quantitative geomorphological analysis data, the drainage pattern (mainly the west part of it) is in an unstable dynamic status. During Plio-Quaternary there were a few rejuvenating episodes, due to tectonic and climate changes. The present rejuvenated stage, which is more obvious in the southwestern part of the investigated area, is supported by morphotectonic data. Among them, the most remarkable are: a)the steep slopes (30-60 %), b)the negative deviation of "cummulative" area compared to ideal values, c)the slope flexions, which separate the new lower level from the old higher one.
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Strzeboński, Piotr, Justyna Kowal-Kasprzyk, and Barbara Olszewska. "Exotic clasts, debris flow deposits and their significance for reconstruction of the Istebna Formation (Late Cretaceous – Paleocene, Silesian Basin, Outer Carpathians)." Geologica Carpathica 68, no. 6 (August 1, 2017): 562–82. http://dx.doi.org/10.1515/geoca-2017-0037.
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AbstractThe different types of calcareous exotic clasts (fragments of pre-existing rocks), embedded in the Paleocene siliciclastic deposits of the Istebna Formation from the Beskid Mały Mountains (Silesian Unit, Western Outer Carpathians), were studied and differentiated through microfacies-biostratigraphical analysis. Calcareous exotics of the Oxfordian- Kimmeridgian age prevail, representing a type of sedimentation comparable to that one documented for the northern Tethyan margin. The Tithonian exotic clasts (Štramberk-type limestones), which are much less common, were formed on a carbonate platform and related slope. The sedimentary paleotransport directions indicate the Silesian Ridge as a main source area for all exotics, which were emplaced in the depositional setting of the flysch deposits. The exotics constitute a relatively rare local component of some debrites. Proceedings of the sedimentological facies analysis indicate that these mass transport deposits were accumulated en-masse by debris flows in a deep-water depositional system in the form of a slope apron. Exotics prove that clasts of the crystalline basement and, less common, fragments of the sedimentary cover, originated from long-lasting tectonic activity and intense uplift of the source area. Mass transport processes and mass accumulation of significant amounts of the coarse-grained detrital material in the south facial zone of the Silesian Basin during the Early Paleogene was due to reactivation of the Silesian Ridge and its increased denudation. Relative regression and erosion of the emerged older flysch deposits were also forced by this uplift. These processes were connected with the renewed diastrophic activity in the Alpine Tethys.
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Waskowska, Anna. "Bulbobaculites gorlicensis n. sp. – a new agglutinated foraminifera from Eocene of flysch Carpathians." Micropaleontology 60, no. 5 (2014): 465–73. http://dx.doi.org/10.47894/mpal.60.5.03.
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A new foraminiferal species, Bulbobaculites gorlicensis n. sp., is described from the Bartonian (Middle Eocene) succession of the Hieroglyphic beds deposited in the Silesian Basin, Outer Carpathians (South Poland). It occurs in association with deep-marine bathyal and abyssal assemblages dominated by agglutinated forms. The test of Bulbobaculites gorlicensis is relatively large, free, and elongated, consisting of 3-4 spherical chambers quickly increasing in size and composed of coarse quartz sand grains. The initial part of the test is in low trochospiral coil, terminally uniserial with terminal aperture on the last, largest chamber.
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Hnylko, Oleh, Svitlana Hnylko, Maria Kulyanda, and Romana Marchenko. "Tectonic-sedimentary evolution of the frontal part of the Ukrainian Carpathian nappe structure." Geology and Geochemistry of Combustible Minerals 1-2, no. 183-184 (2021): 45–59. http://dx.doi.org/10.15407/ggcm2021.01-02.045.
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For the first time in the Ukrainian Carpathians, the depths and tectono-sedimentation processes in the north-eastern part of the Outer Carpathian Basin (Skyba and Boryslav-Pokuttya units) have been restored on the base of sedimentological and microfaunistic studies. It was established that in the Cretaceous-Eocene time, the deep-water (near Calcite Compensation Depth) turbidite and similar sedimentation (turbidites with Bouma textures, grainites, debris-flow deposits), which periodically alternated with (hemi)pelagic sedimentation (red, green and black shales) was dominant here. Sedimentation took place on the continental margin of the the Carpathian branch of the Tethys, where deep-water fans were formed. Cretaceous-Eocene background red and green shales are enriched in buried in situ benthic foraminifera which are similar in taxonomic composition and morphological features to the microfauna of the Carpathian-Alpine and Atlantic regions (deep-water agglutinated foraminifera), which indicate lower bathyal – abyssal depths of flysch sedimentation. Latest Eocene Globigerina Marl horizon contains the foraminiferal assemblage with plankton dominance, which indicates a general shallowing of the Outer Carpathian Basin (middle-upper bathyal conditions above a calcite compensation depth). Oligocene – lowermost Miocene Menilite-Krosno and Polyanytsia formations were accumulated in the Skyba and Boryslav-Pokuttya sub-basins. In the Miocene, shallow-water molasses were accumulated here. Probably, the tectonic uproot of flysch deposits from its substrate and their synsedymentary thrusting towards the platform caused a significant shallowing of the Skyba and Boryslav-Pokuttya sub-basins starting from the latest Eocene. These processes reflected the growth of the Carpathian frontal nappes at the final orogen formation stage.
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Nikolov, Todor, Nikolina Ruskova, and Khrischo Khrischev. "Principles of the Lower Cretaceous lithostratigraphy in Bulgaria." Geologica Balcanica 21, no. 6 (December 30, 1991): 3–47. http://dx.doi.org/10.52321/geolbalc.21.6.3.
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The Lower Cretaceous deposits are widespread in North Bulgaria: in the Fore-Balkan, the Transitional Zone, and the Moesian Platform. The scheme of the formal lithostratigraphic units includes 37 Formations and has been elaborated for all this territory on the basis of outcrops and numerous boreholes. Four Groups (West-Balkan Carbonatic Group, Central-Balkan Flysch Group, Vraca Urgonian Group and Loveč Urgonian Group) consist of 19 Formations, and the other 18 Formations are independent. A total of 15 Members has been introduced within 9 of the Formations. The composition and interrelations of tbe lithostratigraphic units reflect the inhomogeneities and the different tendencies of the development of tile Early Cretaceous basin. The most expressive facies boundary in the west-east direction is the so-called Jablanica Line. West of it, carbonatic and marly deposits predominate in the Fore-Balkan. The carbonatic Formations belong to the West-Balkan Carbonatic Group and the Vraca Urgonian Group. The Salaš Formation is built up of clayey limestones and marls, and is widespread in the West Fore-Balkan, as well as in the western part of .the Moesian Platform. The asymmetry of the basin with a dry land as source region to the south of it, is clearly outlined to the east of the Jablanica Line, within: the Central and East Fore-Balkan and the adjacent Transitional Zone. This character of the basin controlled a facies differentiation with development of predominantly terrigeneous units in the south, and of carbonatic and marly units, to the north. This difference is expressed at its best at the lower levels of the Lower Cretaceous where units of the Central-Balkan Flysch Group are interfingering with units of the West-Balkan Carbonatic Group. The lateral transition takes place within the Transitional Zone. At higher stratigrapic levels (Hauterivian - Aptian) the asymmetry is expressed into a horizontal transition of terrigenous non-flysch deposits (Kamchija Formation and Roman Formation) with predominantly marly deposits (Gorna-Orjahovica and Trâmbeš Formations) to the north. A specific feature is the presence of Urgonian deposits in the Transitional Zone (Loveč Urgonian Group). At both sides of its development area, fans of the terrigeneous deposits of the Roman Formation are traced towards north. They are bounded to the Iskar (at the west) and Etar (to the east) depressions. Urgonian limestones occur also within the Moesian Platform in the area of Ruse (Ruse Formation). The highest (Albian) levels of the Lower Cretaceous section have been observed only in northwest Bulgaria. They are represented by the marls of the Sumer Formation, the glauconitic predominantly sandy deposits of Malo Peštene Formation, and the marls of Rabiša Formation.
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Mohamed, Omar, and Michael Wagreich. "Organic-walled dinoflagellate cyst biostratigraphy of the Well Höflein 6 in the Cretaceous–Paleogene Rhenodanubian Flysch Zone (Vienna Basin, Austria)." Geologica Carpathica 64, no. 3 (June 1, 2013): 209–30. http://dx.doi.org/10.2478/geoca-2013-0015.
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Abstract Palynological analysis of the Rhenodanubian Flysch Zone section recovered from Well Höflein 6 north of Vienna allows the successful application of non-calcareous dinoflagellate biostratigraphy to the deep-water sediments of the Greifenstein Nappe. All 62 cuttings samples contained organic-walled dinoflagellate cysts (dinocysts) and some of them allow age-assessment. The results corroborated the presence of two thrust slices. The upper thrust unit A comprises a Campanian to Lower Eocene succession including, from old to young, the Röthenbach Subgroup, Perneck Formation, Altlengbach Formation and Greifenstein Formation. The lower thrust unit B contains in addition a pre- Campanian base, probably the Wolfpassing Formation of Early to mid-Cretaceous age.
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Miclăuş, Crina, Francesco Loiacono, Diego Puglisi, and Dorin Baciu. "Eocene-Oligocene sedimentation in the external areas of the Moldavide Basin (Marginal Folds Nappe, Eastern Carpathians, Romania): sedimentological, paleontological and petrographic approaches." Geologica Carpathica 60, no. 5 (October 1, 2009): 397–417. http://dx.doi.org/10.2478/v10096-009-0029-9.
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Eocene-Oligocene sedimentation in the external areas of the Moldavide Basin (Marginal Folds Nappe, Eastern Carpathians, Romania): sedimentological, paleontological and petrographic approachesThe Marginal Folds Nappe is one of the most external tectonic units of the Moldavide Nappe System (Eastern Carpathians), formed by Cretaceous to Tertiary flysch and molasse deposits, piled up during the Miocene closure of the East Carpathian Flysch basin, cropping out in several tectonic half-windows, the Bistriţa half-window being one of them. The deposits of this tectonic unit were accumulated in anoxic-oxic-anoxic conditions, in a forebulge depozone (sensuDeCelles & Giles 1996), and consist of a pelitic background sporadically interrupted by coarse-grained events. During the Late Eocene the sedimentation registered a transition from calcareous (Doamna Limestones) to pelitic (Bisericani Beds) grading to Globigerina Marls at the Eocene-Oligocene boundary, and upward during the Oligocene in deposits rich in organic matter (Lower Menilites, Bituminous Marls, Lower and Upper Dysodilic Shales) with coarsegrained interlayers. Seven facies associations were recognized, and interpreted as depositional systems of shallow to deeper water on a ramp-type margin. Two mixed depositional systems of turbidite-like facies association separated by a thick pelitic interval (Bituminous Marls) have been recognized. They were supplied by a "green schists" source area of Central Dobrogea type. The petrography of the sandstone beds shows an excellent compositional uniformity (quartzarenite-like rocks), probably representing a first cycle detritus derived from low rank metamorphic sources, connected with the forebulge relief developed on such a basement. The sedimentation was controlled mainly by different subsidence of blocks created by extensional tectonic affecting the ramp-type margin of the forebulge depozone.
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de Capoa, Paola, Angelida Di Staso, Francesco Guerrera, Vincenzo Perrone, Mario Tramontana, and Mohamed Najib Zaghloul. "The Lower Miocene volcaniclastic sedimentation in the Sicilian sector of the Maghrebian Flysch Basin: geodynamic implications." Geodinamica Acta 15, no. 2 (May 2002): 141–57. http://dx.doi.org/10.1080/09853111.2002.10510747.
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de Capoa, P. "The Lower Miocene volcaniclastic sedimentation in the Sicilian sector of the Maghrebian Flysch Basin: geodynamic implications." Geodinamica Acta 15, no. 2 (May 2002): 141–57. http://dx.doi.org/10.1016/s0985-3111(02)01085-9.
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