Flysch Deposits Research Articles

Geological Features of the Eastern Sector of the Bangong Co‐Nujiang River Suture Zone: Tethyan Evolution

AbstractAccording to an analysis of the geological features in the eastern sector of the Bangong Co‐Nujiang River suture zone, the Tethyan evolution can be divided into three stages. (1) The Embryo‐Tethyan stage (Pz1): An immature volcanic arc developed in Taniantaweng (Tanen Taunggyi) Range, indicating the existence of an Embryo‐Tethyan ocean. (2) The Palaeo‐Tethyan stage (C‐T2: During the Carboniferous the northern side of the Taniantaweng Range was the main domain of the Palaeo‐Tethyan ocean, in which developed flysch sediments intercalated with bimodal volcanic rocks and oceanic tholeiite, and Pemian‐Early Triassic are granites were superimposed on the Taniantaweng magmatic are; on the southern side the Dêngqên‐Nujiang zone started secondary extension during the Carboniferous, in which the Nujiang ophiolite developed, and the Palaeo‐Tethyan ocean closed before the Middle Triassic. (3) The Neo‐Tethyan stage (T3‐E): During the Late Triassic the Dêngqên zone developed into a relatively matural ocean basin, in which the Dêngqên ophiolite was formed. By the end of the Triassic intraocean subduction occurred, and the ocean domain was reduced gradually, and collided and closed by the end of the Early Jurassic, forming the Yazong mélange; then the Tethyan ocean was completely closed.

Nanhua Rift: A Story of Continental Rift Related to Rodinia Break-up

The southern part of the Korean Peninsula preserves important records of the Paleozoic evolutionary history of East Asia. Here we present SHRIMP U–Pb ages of detrital zircon grains from Paleozoic metasedimentary successions (Okcheon and Joseon Supergroups, Yeoncheon Group, Taean Formation, and Pyeongan Supergroup) that are incorporated into the major Phanerozoic mountain belts (Okcheon and Hongseong-Imjingang Belts) in South Korea, providing new insights for provenances and paleotectonic evolution of the South Korean Peninsula during Paleozoic time. The zircon ages from our samples display two distinct spectra patterns in their presence/absence of Neoproterozoic and/or Paleozoic populations. Our results, together with the available data from the Korean Peninsula, suggest that: (1) the Early to Middle Paleozoic successions in the Okcheon Belt were deposited in continental margin setting(s) formed by Neoproterozoic intracratonic rifting, (2) the Middle Paleozoic metasedimentary rocks in the Imjingang belt can be interpreted as molasse and flysch sediments along an active continental margin, (3) the Late Paleozoic to Early Triassic Taean Formation along the western Gyeonggi Massif represents a syn- to post-collision deltaic complex of a remnant oceanic basin, and (4) the Late Paleozoic to possibly Early Triassic Pyeongan Supergroup in the Okcheon Belt might represent a wedge-top and/or foreland basin. The spatial and temporal discrepancy between the South Korean Peninsula and the Central China Orogenic Belt during Paleozoic might reflect lateral variations in crustal evolution history along the East Asian continental margin during the Paleo-Tethyan Ocean closure.

Caesium contamination and vertical distribution in undisturbed soils in Croatia

The deposition and vertical distribution of 137 Cs and 134 Cs in the first 25 cm of undisturbed soil profiles were studied at more than 50 locations in Croatia. Relative contributions of fallout from weapon-testing and the Chernobyl accident-derived fallout to the total 137 Cs deposition were estimated on the basis of the 137 Cs/ 134 Cs activity ratio. Total weapon-testing-derived deposition can be generally treated as uniform. Significant variation of contamination caused by Chernobyl accident can be explained by relatively short contamination period and great variability in activity and quantity of rainfall. The changes of caesium activity through vertical soil profiles are described by a general equation. Caesium penetrates fastest into deeper soil layers of siltous soils, slowest in the soils developed on flysch sediments. The vertical migration and distribution of Chernobyl-derived 137 Cs are practically the same in terra rossa and loam-podzol soils two and half months after contamination. The average 134 Cs activities of about 1.1 Bq were found in terra rossa, loam podzol and siltous soils in the soil layer between 7.5 and 8.7 cm. Soil samples were collected in July 1986 and both Chernobyl-derived caesium isotopes had only short time to migrate downwards. In soils developed on flysch sediments, loam-podzol and terra rossa weapon-testing-derived caesium activity decreases throughout the whole profile, while in siltous soils it increases in the first 3 cm of soil depth. The soil type influences the rate of vertical caesium migration downward soil profile. The results obtained reveal the following order of caesium vertical migration rate: siltous soil>terra rossa>loam-podzol>soils developed on flysch sediments.

Mineralogical and geochemical indicators of the polygenetic nature of terra rossa in Istria, Croatia

Terra rossa in Istria is situated on the Jurassic–Cretaceous–Paleogene carbonate plain and is considered a polygenetic reddish soil which bears typical terra rossa Fe-oxide characteristics (e.g., Fe d and Fe d/Fe t). The difference in particle size, mineralogy and geochemistry observed between terra rossa and the insoluble residue of limestones and dolomites clearly indicates that the additions of external materials might have diminished the influence of insoluble residue of limestones and dolomites as the primary parent material of terra rossa in Istria. Terra rossa is clay and silty clay composed of quartz, plagioclase, K-feldspar, micaceous clay minerals (illitic material and mica), kaolinites (Kl D and Kl), chlorite, vermiculite, low-charge-vermiculite or high-charge smectite, mixed-layer clay minerals (other than illitic material), hematite, goethite and XRD-amorphous inorganic compound. Calcite, dolomite and boehmite are sporadically present and are of local importance. Kaolinites and illitic material are dominant clay mineral phases in the clay fraction of all terra rossa from Istria. Kaolinite which does not form intercalation compounds with dimethylsulfoxide (DMSO) is the dominant mineral phase in fine clay and is considered predominantly authigenic rather then inherited from parent materials. Neither the content and particle size distribution nor the bulk and clay mineralogy of the insoluble residue of limestone and dolomite support development of terra rossa entirely by dissolution of carbonate rock. If terra rossa has developed only from the insoluble residue of limestone and dolomite, its clay content, due to weathering should be higher than that in the insoluble residues which is not the case. Plagioclase was found only in one insoluble residue while all terra rossa samples contain this mineral. Moreover, insoluble residues do not contain vermiculite which was observed in small amounts in clay fraction of all terra rossa samples. (Na 2O/K 2O)×100, Zr/Nb and (Zr/Ti)×1000 ratios in the majority of terra rossa samples are much higher than in the insoluble residue of limestones and dolomites which also supports external material influence in the genesis of terra rossa. Materials other than the insoluble residue of limestones and dolomites which might have contributed to terra rossa are loess sediments, whose deposition was very important recurrent process in Istria probably since the early Middle Pleistocene, and flysch sediments which extended much more southwards from its present position. Analyses performed indicate that both loess older than that of the Upper Pleistocene age and flysch might have contributed in the genesis of terra rossa.

A zoophycos group trace fossil from miocene flysch in Southern Turkey: Evidence for a U‐shaped causative burrow

Echinospira isp., a relatively small, lobate, trace fossil of the Zoophycos group, occurs in Miocene flysch deposits of the Cingöz Formation of southern Turkey. It displays a burrow system which contains U‐shaped Rhizocorallium‐like elements. The burrow system resulted from successive lateral shifts of a causative U‐shaped burrow, which reworked most of the previously formed ones. More and less systematic patterns of sediment reworking by the trace fossil producer were observed. The trace fossil occurs in a low diversity ichnoassemblage related to environmental stress conditions probably caused by frequent turbiditic deposition and lithological changes. In comparison, Echinospira pauciradiata occuring in pelagic sediments of the same age is much larger and displays a more regular pattern, related to more stable environmental conditions.

Structural framework of the Bashkirian anticlinorium, SW Urals

The Bashkirian anticlinorium of the southwestern Urals shows a much more complex structural architecture and tectonic evolution than previously known. Pre-Uralian Proterozoic extensional and compressional structures controlled significantly the Uralian tectonic convergence. A long-lasting Proterozoic rift process created extensional basement structures and a Riphean basin topography which influenced the formation of the western fold-and-thrust-belt with inversion structures during the Uralian deformation. A complete orogenic cycle during Cadomian times, including terrane accretion at the eastern margin of the East European platform, resulted in a high-level Cadomian basement complex, which controlled the onset of Uralian deformation, and resulted in intense imbrication and tectonic stacking in the subjacent footwall of the Main Uralian fault. The Uralian orogenic evolution can be subdivided into three deformation stages with differently oriented stress regimes. Tectonic convergence started in the Late Devonian with ophiolite obduction, tectonic accretion of basin and slope units and early flysch deposits (Zilair flysch). The accretionary complex prograded from the SE to the NW. Continuous NW/SE-directed convergence resulted finally in the formation of an early orogenic wedge thrusting the Cadomian basement complex onto the East European platform. The main tectonic shortening was connected with these two stages and, although not well constrained, appears to be of Late Devonian to Carboniferous age. In the Permian a final stage of E–W compression is observed throughout the SW Urals. In the west the fold-and-thrust-belt prograded to the west with reactivation of former extensional structures and minor shortening. In the east this phase was related to intense back thrusting. The East European platform was subducted beneath the Magnitogorsk magmatic arc during the Late Paleozoic collision. The thick and cold East European platform reacted as a stable rigid block which resulted in a narrow zone of intense crustal shortening, tectonic stacking and high strain at its eastern margin. Whereas the first orogenic wedge is of thick-skinned type with the involvement of crystalline basement, even the later west-directed wedge is not typically thin-skinned as the depth of the basal detachment appears below 15 km and the involvement of Archean basement can be assumed.

40 Ar/ 39 Ar Thermochronology west of the Main Uralian fault, southern Urals, Russia

West of the Main Uralian fault, the main suture in the southern Urals, 40Ar/39Ar apparent ages of amphibole, muscovite and potassium feldspar are interpreted as cooling ages. A fast exhumation of the metamorphic complex of Kurtinsky during Upper Carboniferous time is indicated by the small age difference (15 Ma) between cogenetic amphibole and muscovite. Differentiated movement in the footwall of the Main Uralian fault along strike is indicated by the age difference of 70 Ma between the metamorphic complexes of Kurtinsky (north) and Maksyutov (south). No Upper Paleozoic (Uralian) medium- to high-temperature event is recorded in 40Ar/39Ar data from the metamorphic complex of Beloretzk (MCB). An amphibole age of 718±5 Ma and the occurrence of mafic intrusions might signal the break-up of Rodinia and therefore indicate the rifting period followed by the separate movement of the "Beloretzk terrane". Muscovite ages of approximately 550±5 Ma, the unique pre-Ordovician tectonometamorphic evolution of the MCB and the Late Vendian sedimentary history of the western Bashkirian Megaanticlinorium (BMA) imply the existence of a Neoproterozoic orogeny at the eastern margin of Baltica. This orogeny might have been initiated by the accretion of the "Beloretzk terrane". The metamorphic grade of the overlain Silurian shales and the K/Ar microcline ages from the "Beloretzk terrane" give evidence for a new thermal event at approximately 370 Ma. A microcline age of 530–550 Ma obtained for the Vendian conglomerate in the western BMA suggests that a maximum temperature of approximately 200°C was reached in Cambrian or Vendian times. An orthoclase age (590–630 Ma) of the Vendian Zigan flysch deposits might be inherited from the eastern source area, the Cadomian orogen. An orthoclase age (910–950 Ma) from the Riphean Zilmerdak conglomerate coincides with a documented decrease in the subsidence rate of the Upper Riphean basin.

Deformation bands and the history of folding in the Magura nappe, Western Outer Carpathians (Poland)

Deformation bands ( db) which are indicative for soft-sediment deformation during the folding of flysch sediments are widespread within the Eocene strata of the Magura nappe. Four types of db have been distinguished: (1) db with no cataclasis of detrital sand grains; (2) db with traces of feldspar cataclasis; (3) db with strong cataclasis of detritic feldspar grains; and (4) db with feldspar and quartz cataclasis. In all types of db, calcite cementation occurred after the formation of the deformation bands. No calcite cataclasis was observed in the deformation bands. The bands developed progressively, from (1) to (4), during and after regional folding. Folding occurred when the host strata were poorly indurated and/or under low confining pressure. The earliest db (bands with no cataclasis) formed contemporaneously with water-escape sheets. We conclude that regional folding started not later than during the deposition of the host strata. Calcite mineralization was introduced into the host strata and into the db along cross-fold joints after the completion of regional folding. Within the studied portion of the Magura nappe, regional folding started not later than during Eocene time. Folding was completed when the host strata were not yet fully indurated, most probably still during the Eocene.

A revised model for the relationship between joint spacing and layer thickness

Hobbs' model [Hobbs, D. W. (1967) The formation of tension joints in sedimentary rocks: on explanation. Geological Magazine 104, 550–556.] has been cited as one of the theories for interpretation of the linear relationship between saturated joint spacing ( s) and bed thickness ( t) in interbedded sedimentary rocks. However, this model is based on an assumption that the shear stress in the bounding non-jointing layers decreases linearly from the maximum value at the layer matrix interface to zero at a distance exactly equal to the jointing layer thickness from the interface. We provide a revised analytical model which takes into account the non-linear decay of the shear stress and the effects of bounding bed thickness ( d). The model shows that s − η√ td for the competent beds bounded by two incompetent layers nearly identical in thickness. The constant η depends on both material properties of rocks (i.e. the Young's modulus, tensile strength and fracture saturation strain of the competent bed, and the shear modulus of the incompetent layers) and decay modes of the shear stress in the bounding layers. If the ratio of d to t is constant, the relationship between s and t is linear. If d is constant, the joint spacing increases as a function of the square root of t. Complex t d variations from Cambrian flysch sediments at Plage Victor in the Saint-Jean Port-Joli area of the Quebec Appalachians, however, result in a statistically linear relationship between s and t.

Differentiating glacio‐eustacy and tectonics; a case study involving dinoflagellate cysts from the Eocene–Oligocene transition of the Pindos Foreland Basin (NW Greece)

In an attempt to discriminate between tectonically induced sea‐level changes and glacio‐eustacy, the Ekklissia and Arakthos sections (Epirus, NW Greece) are examined, applying (dinocyst) palynology, sedimentology and magnetostratigraphy. The sections, located in the Pindos Foreland Basin, both comprise the transition from pelagic limestones to hemipelagic silty clays and turbidite sandstones, reflecting the onset of flysch sedimentation as a result of the Pindos thrust activity. Despite an overall tectonic overprint, relative changes of sea level can be reconstructed, using (i) continental/marine palynomorph ratios, (ii) relative abundance of inshore and offshore dinoflagellate cysts, and (iii) taxa indicative of relatively cold and warm sea‐surface temperature, that can be calibrated against the Global Polarity Time Scale (GPTS). Increased fluxes of marginal marine and continental palynomorphs coincide with colder periods on a ‘third‐order’ scale, which thus appear to be related to glacio‐eustatic trends in sea‐level. The larger scale is attributed to the increasing effect of tectonics and acts on a ‘second‐order scale’.

Geotechnical assessment of overburdens applied to the timing of building of the central Apennines (Italy)

In order to state the exact value of the maximum overburden undergone by a sediment, a geotechnical method based on preconsolidation pressure was set up. It was applied to a region of the central Apennines where late Miocene flysch sediments occupy elongated depressions separating mountains of carbonate rocks. These depressions are commonly interpreted as the remains of different foredeeps built between the late Miocene and the early Pliocene, migrating from SW to NE. This flysch is part of a terrigenous sequence that has started in the Tortonian and superimposed with continuity and conformity on a carbonate platform sequence. The geotechnical analyses of 39 undisturbed clay samples, chiefly collected near the base of the terrigenous sequence, surprisingly show that the original thicknesses of this sequence were constant among the different basins: 5900 m. We therefore suppose that the terrigenous sequence sedimented in an unique subsiding basin, whose bottom remained very flat until about 1.1 million years ago, when the sequence lasted to be deposited with continuity. We suggest that the main Apennines tectogenesis could not have taken place before that time: later on, the carbonate platform tilted, quickly slided towards the Adriatic trench and broke into fragments separated by depressions, where the terrigenous sequence was driven in.

Alpine geodynamic evolution of passive and active continental margin sequences in the Tauern Window (eastern Alps, Austria, Italy): a review

The Penninic oceanic sequence of the Glockner nappe and the foot-wall Penninic continental margin sequences exposed within the Tauern Window (eastern Alps) have been investigated in detail. Field data as well as structural and petrological data have been combined with data from the literature in order to constrain the geodynamic evolution of these units. Volcanic and sedimentary sequences document the evolution from a stable continent that was formed subsequent to the Variscan orogeny, to its disintegration associated with subsidence and rifting in the Triassic and Jurassic, the formation of the Glockner oceanic basin and its consumption during the Upper Cretaceous and the Paleogene. These units are incorporated into a nappe stack that was formed during the collision between a Penninic Zentralgneis block in the north and a southern Austroalpine block. The Venediger nappe and the Storz nappe are characterized by metamorphic Jurassic shelf deposits (Hochstegen group) and Cretaceous flysch sediments (Kaserer and Murtorl groups), the Eclogite Zone and the Rote Wand–Modereck nappe comprise Permian to Triassic clastic sequences (Wustkogel quartzite) and remnants of platform carbonates (Seidlwinkl group) as well as Jurassic volcanoclastic material and rift sediments (Brennkogel facies), covered by Cretaceous flyschoid sequences. Nappe stacking was contemporaneous to and postdated subduction-related (high-pressure) eclogite and blueschist facies metamorphism. Emplacement of the eclogite-bearing units of the Eclogite zone and the Glockner nappe onto Penninic continental units (Zentralgneis block) occurred subsequent to eclogite facies metamorphism. The Eclogite zone, a former extended continental margin, was subsequently overridden by a pile of basement-cover nappes (Rote Wand–Modereck nappe) along a ductile out-of-sequence thrust. Low-angle normal faults that have developed during the Jurassic extensional phase might have been inverted during nappe emplacement.

On the provenance of flysch deposits in the External Hellenides of mainland Greece: results from heavy mineral studies

The terrigenous materials of the flysch deposits of the External Hellenides of mainland Greece have been characterized by their heavy mineral assemblages, based on 194 samples. Three major source types were distinguished. (1) A metamorphic source is shown by abundant garnet accompanied by traces of staurolite and chloritoid. In the source of the Pindos and Ionian zones, blueschist complexes were incorporated within the metamorphic terrains, demonstrated by the frequent occurrence of blue amphiboles. (2) The existence of ophiolitic sources is indicated by the occurrence chrome spinel. Pyroxenes, green amphiboles and partly epidote are related to volcanic/metavolcanic complexes. High ophiolitic detritus was especially found in Mid-Cretaceous turbiditic layers supplied from internal terrains. (3) Granitoid and gneiss source terrains are indicated, predominantly represented by zircon, tourmaline and apatite. This type of source is characteristic for Mid-Cretaceous turbidites sampled in western parts of the Pindos zone. In the terminal flysch deposits, granitoid detritus played only a subordinate role. An extensive recycling of Pindos Flysch material into the younger Western Hellenic Flysch can be excluded. Stratigraphic trends in the heavy mineral distribution of the terminal Pindos Flysch give insights into the changing tectonic situation of the source terrains. A regional east–west trend with changing ophiolitic detritus, observed in the Parnassos-Ghiona Flysch, points to a complex feeder system.

Upper crustal structure in the Potenza area (Southern Apennines, Italy) using Sp converted wave

In this paper we analyse the records of the two Potenza seismic sequences (Southern Apennines, Italy) which occurred in 1990 and 1991, in order to obtain information on the upper crustal structure in this area. The hypocentral depths are mainly concentrated below 10 km which is the supposed upper limit of the crystalline basement. The seismograms recorded at temporary arrays deployed during the two sequences clearly show on the vertical component, an intermediary phase between the P and S waves. For the investigated epicentral distances (less than 30 km) the delay between this secondary phase and the direct S wave arrival is almost constant at each station, suggesting that the observed intermediary phase might be an S to P conversion at a discontinuity shallower than the hypocentral depth. This interpretation has been supported by polarisation analysis and numerical modelling results. Considering the regional geological structure, these latter have also shown that the interface generating strong converted waves could be the top of the Apulian carbonate platform overlaid with recent clay deposits and flysch sediments. 1D inversion of the travel-time data was performed in order to evaluate a local vertical upper crustal profile.

Discovery and significance of Cretaceous fossils from the Xigaze Forearc Basin, Tibet

The Xigaze Cretaceous forearc basin located between the Lhasa Block and Indus-Yarlung Suture was filled with flysch deposits during the mid-Cretaceous, as the Tethys oceanic crust was being subducted underneath Eurasia. The flysch comprises the Xigaze Group, dominated by the Angren Formation. Well preserved, newly discovered foraminifera within the Angren Formation constrain its age to late Albian to late Coniacian. Radiometric dating of the ophiolite belt impinging on the southern edge of the forearc basin yielded an age of 120+10 Ma, which implies that the deposition in the forearc basin occurred shortly after initiation of the subduction of the Neotethys.

Molasse-Delta-Flysch Continuum of the Himalayan Orogeny and Closure of the Paleogene Katawaz Remnant Ocean, Pakistan

Molasse strata on the Indo-Pakistan subcontinent and modern Indus delta-submarine fan sediments in the northern Indian Ocean were derived from the Himalaya. Earliest molasse sedimentation started around the late Paleocene, soon after formation of the early Himalayan orogenic highlands. However, turbidite sedimentation of the modern Indus fan did not begin until the early Miocene, and occurred even later on the Bengal fan in the modern Indian Ocean. Paleogene deltaic and flysch sediments that are missing from the Indian Ocean are preserved as the Khojak Formation in the Katawaz basin and the Makran area, Pakistan. This implies that the Katawaz remnant ocean was the main depocenter of early Himalayan marine sediments prior to deposition in the Indian Ocean, the Neogene depocenter. The Katawaz remnant ocean, a southwestern extension of the Neo-Tethys, was closed by the end of early Miocene time and the Paleogene delta-flysch sediments were incorporated into the Indo-Pakistan subcontinent.

Tectonic history of the metamorphic basement rocks of the Sierra del Carmen, Coahuila, Mexico

The Ouachita interior zone, arching through central Texas into the Big Bend region of the Rio Grande, has been defined chiefly on the basis of well samples and its associated gravity high. The only known exposure of rocks of the interior zone lies at the base of the Sierra del Carmen normal fault escarpment under approximately 1100 m of Lower Cretaceous carbonates in northern Coahuila, Mexico. These lower greenschist facies metamorphic rocks are thinly interlayered graphitic muscovite schist, graphitic marble, and minor quartzite with abundant quartz veins. The dominant structures shown by the metamorphic rocks are isoclinal folds (F2) that have a well-defined axial planar foliation (S2). Earlier (F1) folds refolded by F2 are locally preserved. At the microscopic scale, S2 is a crenulation cleavage of the S1 foliation that has been enhanced by pressure solution. Feldspar porphyroblasts overgrow a folded graphitic S1 foliation. Throughout the area a second crenulation cleavage (S3) is present on the S2 foliation surface as an intersection lineation (L3). Subsequent Laramide regionalto outcrop-scale folds and associated thrusts overprint these ductile structures. Lower Cretaceous carbonates form a large, east-verging overturned to recumbent anticline-syncline fold pair with a northwest-trending fold axis. The S2 metamorphic foliations define an antiform that is nearly coincident in trend to that of the fold in the overlying carbonates, indicating that the metamorphic rocks were also folded by this regional structure. A Basin and Range normal fault is interpreted to have reactivated the Laramide thrust fault responsible for the contractional deformation. One to two normal faults cut the carbonates and metamorphic rocks and truncate the anticline-syncline fold pair. The maximum offset along the normal fault is 1600 m. Rb/Sr data from the muscovite schist gives a six-point, mineralÐwhole-rock isochron age of 277 ± 10 Ma, indicating that polyphase deformation and metamorphism occurred during the late Paleozoic Ouachita orogeny. An initial Sr ratio of 0.721 suggests an ancient source for these metasediments. Common Pb ratios of the metamorphic whole rock and galena from the Puerto Rico Mine are isotopically distinct from those of the North American craton, suggesting that they were derived from a nonÐNorth American source and thus may be equivalent to unmetamorphosed Ouachita flysch sediments. This indicates that the metamorphic rocks of the Ouachita interior zone were derived from an ancient allochthonous source that was deformed and metamorphosed during the late Paleozoic Ouachita orogeny.

The Development of the Eocene Platform Carbonates from Wells in the Middle Adriatic Off-Shore Area, Croatia

In the Middle Adriatic deep off-shore wells the following sedimentary faciess exist: fenestral and Charophyte limestone facies (X); facies of foraminiferal wackestone-packstone, ostracod marls and fine grained breccia conglomerate (A): facies of foraminiferal packstonegrainstone (B) and miliolidal mudstone-wackestone (C): facies of porous limestone?, grainstone? (Y): facies of fossiliferous mudstonepackstone (D); algal bound stone/bindstone and wackestone facies (E): facies of the foraminiferal mudstone-packstone (F); Nummulites - Discocyclina floatstone-packstone and grainstone-rudstone facies (G). The sediments were deposited close to the carbonate platform margin. Beds of facies X have an uncertain stratigraphic position; younger than the Cretaceous but older than the Cuisian. A transgressive sequence that is composed of facies A, B, C and Y was formed during the Cuisian, whereas the others belong to Lutetian (and Biarritzian). At the end of the Middle Eocene they were tectonically compressed and covered by flysch deposits. Good stratigraphic correlation between the wells along the Dinaric strike strongly suggests that the facics are laterally extensive in this direction. Perpendicular to the trend they arc considerably reduced. Oil shows in the Kate- I well originated from the Lower Cretaceous so surce rocks (evaporite complex).

The pre-flysch and the basal shaly flysch deposition in Osios Loukas and Distomo areas, central Parnassus, central Greece, during the late Paleocene to the early Eocene

The pre-flysch and the basal shaly flysch deposition in Osios Loukas and Distomo areas, central Parnassus, central Greece, during the late Paleocene to the early Eocene

Paleomagnetism of Carboniferous sediments from the West Sudetes (SW Poland)

The studied Carboniferous flysch and molasse sediments from the Intra-Sudetic Basin correspond to the period from Middle Visean to Early Autunian. Main magnetic minerals carrying the natural remanent magnetization (NRM) are goethite, magnetite, maghemite and hematite, all usually secondarily formed and/or remagnetized due to several tectonometamorphic events. In most samples several NRM components were isolated. One of them is usually a Jurassic-Triassic overprint. Some others define the Westphalian-Early Permian segment of the declination and inclination trajectory for the Sudetes calculated according to the reference apparent polar wander path for the Baltica plate. The Sudetic path is slightly shifted to the east compared to the reference path, suggesting the possibility of independent movements of the Sudetes during this time. The majority of isolated NRM components are secondary and related to the Sudetic orogenic phase and later tectonometamorphic activity.