Tectonic environment and geodynamic significance of the Neo-Cimmerian Donqiao ophiolite, Bangong-Nujiang suture zone, Tibet
J. GirardeauJ. MarcouxClaude J. AllègreJean-Paul BassoulletTang YoukingXiao XuchangZao YougongWang Xibin
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Flysch
Pillow lava
Sequence (biology)
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Rotacja tektoniczna plaszczowin fliszowych Polskich Karpat Zewnetrznych
Clockwise rotation in the pile of nappes forming the Outer Flysch Belt of the Western Carpathian's is evidenced by the relation of the nappes to the margin of the Foreland Platform, by the relation of the nappes to the northern front of the Outer Flysch Belt, and by rotation of segments of the Outer Flysch Belt contained between fault zones with sinistral strike-slip displacement. Seven major fault zones with sinistral strike-slip displacement are identified in the Polish Outer Carpathians.
Flysch
Clockwise
Vergence (optics)
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In this paper the stratigraphical, structural, geochemical and petrological features of the Mirdita (Albania) and Pindos, Vourinos, Koziakas, Othrys and Argolis (Greece) ophiolitic nappes are summarised and then compared. These ophiolitic nappes occur as a 700 km long belt running from Albania to Greece. These ophiolitic nappes are located between the west-verging imbricate stack of thrust sheets derived from the Adria plate continental margin to the west and the Pelagonian zone to the east. Each ophiolitic nappe is represented by several end-members represented by the sub-ophiolite melange, the ophiolite sequence( s) with their sedimentary oceanic cover and the supra-ophiolite deposits. The latter can be divided in syn- and post-emplacement deposits, the first ones are recognised only in Albania. All the described ophiolite sequences are characterised at their base by a well-developed metamorphic sole that represents a further end-member of the ophiolitic nappe. The comparison among the features of all the end-members recognised in the studied ophiolitic nappes allows providing further constraints for the geodynamic reconstructions of the Mesozoic Tethyan oceanic basin located eastwards of the Adria plate.
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Our fieldwork in the area of Kato Seli of Mt Vermion suggests that the Vermion Nappe is not only tectonically overlying the Maastrichtian flysch of the Pelagonian Zone, but also a Jurassic melange that overlies the Triassic-Jurassic marbles of the Pelagonian Zone. Moreover, between the Vermion Nappe and the underlying melange, tectonic slivers of meta-sandstones-meta-rudites are tectonically emplaced. This calls for a reassessment of the emplacement of the Vermion Nappe and its role in the geotectonic evolution of the area.
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In the underlying Miocene strata, randomly interstratified IfS (40-50%S) is observed. In the borehole Nowy Targ IGl (the southern part of the Magura nappe), randomly interstratified IfS varies irregularly from 72%S to 40%S, down to about 1000 m. Between 1000 m and 2500 m %S in IfS regularly decreases from 73%S to 22%S and ordering appears at about 1800 m. The illitization of the Podhale flysch in the borehole Skocznia IG 1 is advanced, only ordered IfS is present, and %S decreases gradually from 26%S to 12%S over 500 m from the top of the borehole. It appears that the diagenetic model of smectite illitization in Krak6w-Nowy Targ cross-section is more complicated then the diagenetic history known from a more eastern cross-section (Skole nappe, Paszowal-Kuzminal-Cisowal). Ordering apppears at shallower depths and the illitization profile in flysch seems to have been established before the thrusting of flysch over the Miocene strata. Przeglqd Geologiczny, vol. 45, nr 10, 1997
Flysch
Neogene
Paleogene
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Abstract In southern Lucania, from the Agri river south to Cetraro and the southwestern shore of the gulf of Tarento, and particularly near the Tyrrhenian (western) coast of Lucania, flysch of undetermined age and complex relationships is a major part of both autochthonous and allochthonous tectonic units. The fundamental problem is the paleogeography of different allochthonous flysch sequences of Mesozoic and Tertiary age. The second is the geographic origin of the flysch and the dolomitic limestone. Third is the mechanism and time of emplacement of nappes. The nappes of dolomitic limestones and the Cetraro gneiss plates behaved tectonically as rigid elements, quite differently from the plastic nappes of the allochthonous flysch. The fourth great problem is differentiating Mesozoic allochthonous flysch from that of Miocene-Pliocene age. Some of the allochthonous flysch may have come from the Tyrrhenian basin to the west.
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The aim of this work is to the present geological structure of the Krynica Subunit of the Magura Nappe in southern part of the Gorce and Beskid S1decki Mountains and along the Pieniny Klippen Belt (PKB). Formal lithostratigraphic units were distinguished on the basis of mapping. The lithostratigraphic units are the age of Middle Paleocene – Middle Eocene age. Flysch deposits were classified as the Szczawnica Formation with the yczanow Member, Zarzecze Formation and Piwniczna Member of the Magura Formation in the investigated area. Strike-slip faults and faulted formations complicate the geological structure of the described region. The creation some of these faults is connected with andesite intrusions. Strong faulted strata occurs in the southern part of the region along the overthrust of the Pieniny Klippen Belt on the Magura Nappe. The contact line between the Pieniny Klippen Belt and Paleogene of the Magura Nappe is heterogeneous. The evidences of it are outcrops of klippen, which occur within the Szczawnica Formation and the Zarzecze Formation.
Flysch
Paleogene
Lithostratigraphy
Outcrop
Geologic map
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Eocene thin-bedded flysch, widespread in the Alpine Tethys ocean, is present within the Magura Nappe, the largest Outer Carpathian unit in Poland and Slovakia. Thin-bedded flysch sedimentation accompanied by hemipelagic shales took place accross the entire Magura Basin during Eocene times. The lithostratigraphic position of these deposits has been a subject of considerable discussion. Different names, such as the Hieroglyphic Beds, Hieroglyphic Formation, Łabowa Shale Formation, Grzechynia Sandstones and Beloveža Beds, Beloveža Formation have been used in the Outer Carpathians literature. We show a striking resemblance of the Beloveža Beds (Formation) from its type locality to the Hieroglyphic Beds from the Beskid Wysoki area and to typical Beloveža Beds from the Hańczowa Mts. We propose to the name Beloveža Formation should be applied to thin-bedded flysch within both Bystrica and Rača units of Magura Nappe and the name Hieroglyphic Formation should be restricted to the Skole Unit. The original type locality in Beloveža near Bardejov in Slovakia is selected as type section of the Beloveža Formation.
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Type locality
Paleogene
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The paleostress analysis was applied at 16 sites in the
Mesozoic limestones, which are tectonically incorporate into
the Cretaceous and the Paleogene strata on the front of the
Western Carpathian Flysch nappes (South Moravia, Czech
Republic). 25 solutions were obtained. These solutions can be
divided into two groups. First group represents the paleostress
field with predominantly NW-SE compression and NE-SW extension
connected with the Early Neogene movements of the Ždanice
nappe. The azimuth of eigenvector of acceptable compression
axes varies from 97 up to 167. This variability can be
explained by rotation of individual tectonic slices of the
Ždanice nappe during the movement this nappe. The different
tectonic scales rotated probably in different sense
(anticlockwise rotation in the case of some scales, clockwise
rotation in the case of other scales). Second group of
solutions represents the paleostress field with NE-SW
compression and NW-SE extension.
Flysch
Clockwise
Neogene
Paleogene
Molasse
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The Magura Nappe is the innermost tectonic unit of the Western Flysch Carpathians and is linked with the Rheno-Danubian flysch of the Eastern Alps. Toward the east this unit runs as an arc from Austria through the Czech Republic, Slovakia and Poland, and then narrows in Eastern Slovakia before disappearing east of Uzhhorod (Trans-Carpathian Ukraine). The Magura Nappe is dominated by Paleogene deposits. In the Ukrainian Carpathians, SE of the Latorica River, the position of the Magura Nappe is occupied by the Marmarosh Flysch Zone. Two facies-tectonic units have been distinguished in this zone - the external Vezhany and the internal Monastyrets' units. Both the Magura Nappe and Marmarosh Flysch revealed the same geotectonic position, lithofacies development and a similar diachronic distribution of Eocene/Oligocene facies in the basins. The Vezhany succession could be regarded as the equivalent of the Fore-Magura thrust sheet in Poland, whereas the Monastyrets resembles the Rača development of the Magura Nappe in Poland and Slovakia.
Flysch
Paleogene
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Cretaceous strata are involved in almost all of the East Carpathian nappes; however, only the Ceahlau, Bobu, Teleajen, Macala, and Audia nappes are composed mainly of Cretaceous flysch. In all of these nappes, the presence of reservoir rocks has been established. Seeps occurring in the Teleajen nappe and shows obtained from the Macala nappe suggest the presence of effective hydrocarbon source rocks. Structural traps are present in all nappes. Stratigraphic trapping conditions apparently are restricted to the Teleajen nappe. the Telkeajen nappe involves 40-400-m-thick black Hauterivian shales (source rock), 500 m of Barremian-Aptian shaly-sandy flysch (source rock), 2000 m of Albian shaly-sandy or sandy-shaly flysch (possible source rock), up to 1000 m of Vraconian-Cenomanian sandy flysch (possible source rock). Particularly in the external parts of the Teleajen nappe, the sandy flysch grades laterally into shaly-sandy flysch, thus providing for potential stratigraphic traps. Reservoir rocks are involved in folds and structures controlled by reverse faults. In the outcropping part of the Teleajen nappe, such structures are deeply eroded to the degree that potential seals are breached. However, in the western parts of the Teleajen nappe, such structures are sealed by the more internal Ceahlau and Bobu nappes. We conclude that hydrocarbonmore » prospects do still exist on the internal, underthrusted parts of the Teleajen nappe.« less
Flysch
Outcrop
Cenomanian
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