The studied Cretaceous flysch succession of the Pieniny Klippen Belt in the Orava territory is si... more The studied Cretaceous flysch succession of the Pieniny Klippen Belt in the Orava territory is similar to the Kysuca Unit where the lower, sandstone flysch (Snežnica Beds) and the upper, conglomerate flysch (Sromowce Formation) were distinguished (Andrusov and Samuel, 1985). Although the studied flysch successions at the Zemianska Dedina locality show sequences similar to the other localities in the Orava territory, there are some differences, mainly in the bed thickness, sandstones/claystones ratio, as well as in the presence of thick slump and slide matrix-supported conglomerate bodies. The sedimentological and stratigraphical evaluations of the section revealed mostly thinto medium-rhythmic turbiditic development. The cyclicity of the thickening-upward sequences, relatively high lateral stability of the beds, their smaller thickness, presence of the Bouma´s intervals and the assemblage of ichnofossils point to a deposition at the slope toe, within the central to outer part of deep-sea fans, rarely dissected by migrating feeding channels filled with upward-fining graded conglomerates and sandstones. The thick matrix-supported conglomerate bodies represent a result of slump and slides on steep submarine slopes transformed to debris-flows and mud-flows that transported sedimentary loads as far as the distal part of the turbiditic fans.
This paper brings results of the first systematic heavy-mineral analysis of the oldest exotics-be... more This paper brings results of the first systematic heavy-mineral analysis of the oldest exotics-bearing units in the Western Carpathians. Samples the Klape Unit, Poruba Formation (Tatric and Fatric units), Manín Unit and Orava Unit were analyzed. Most samples are dominated by chrome-spinels, zircon, tourmaline, apatite and rutile in various ratios. Garnet occurs in small amounts but there is considerable enrichment in a few samples. Titanite, kyanite, monazite and epidote occur only rarely; sillimanite and staurolite are very rare. There is also a local enrichment in blue amphiboles, pyroxenes, garnet and kyanite in some samples. The analyzed spinel grains predominantly match the harzburgite field, with some overlap to the fields of podiform chromitites and cumulates in the Mg/(Mg + Fe 2+) vs. Cr/(Cr + Al) diagram. The TiO 2 vs. Al 2 O 3 diagram indicates the predominant origin of spinels from the supra-subduction zone peridotites for most of the analyses, whereas the other, aluminium-depleted and higher-titanium grains best match the arc volcanic field. The analyzed blue amphiboles are glaucophanes to ferroglaucophanes and were most likely derived from HP/UHP metamorphosed basaltic rocks in a subduction zone. Pyroxenes are mostly represented by orthopyroxenes (enstatite) and less by clinopyroxenes (augite, diopside). Their common euhedral shape and fresh appearance indicate that they were probably not derived from the same ophiolitic source as the Cr-spinels and blue amphiboles, but rather from some adjacent and nearly coeval volcanics which might be of calc-alkaline provenance. Detrital tourmaline grains in the analyzed samples were mostly unzoned except of some grains; some even possessed a complex intergrowing pattern with a mosaic appearance. Most of the grains were derived from various sorts of metasediments. Almost all tourmaline grains from Havranský vrch Hill were likely derived from Li-poor granitoid rocks. The results indicate input of minerals of dominantly ophiolitic provenance, such as Cr-spinels, blue amphiboles, and eventually mosaic tourmaline. Zircon, rest of the tourmaline and rutile were likely derived from older sediments. Garnet, staurolite, kyanite, sillimanite occurring in relatively small amounts were mostly derived from metamorphic rocks of various degrees of metamorphism. No significant differences were observed among the individual units which most likely shared the same source.
Turonian to Maastrichtian exotics-bearing deposits from the Pieniny Klippen Belt (Klape and Kysuc... more Turonian to Maastrichtian exotics-bearing deposits from the Pieniny Klippen Belt (Klape and Kysuca units) and from the Považský Inovec Mts. (Western Carpathians) were analyzed for heavy minerals and compared with similar, yet older Albian-Cenomanian deposits. The Turonian to Maastrichtian deposits are petrographically more variable in composition in the entire range, from quartz arenites to litharenites. Percentages of the main heavy minerals are similar on both stratigraphic levels, i.e., they are dominated by chrome-spinels, zircon, tourmaline, apatite, and rutile. Garnet is more common in the Turonian to Maastrichtian samples, while titanite, kyanite, monazite, hornblende, blue amphibole, pyroxenes, epidote, staurolite, and sillimanite are quite rare. Statistical factor analysis indicates dominance of ophiolites and older sediments in the source areas. One important factor is an influx of garnet, with the weakest factor being related to the influx of tourmaline and apatite, which may indicate low-grade metamorphics. Spinels were derived from harzburgites (supra-subduction peridotites). The majority of tourmalines were derived from metasediments, Fe 3+-rich quartztourmaline rocks, calc-silicate rocks, and metapelites and granitoids. Some had complex zonation with two phases of tourmaline (schorl-dravite and bosiite), or tourmaline intergrown with quartz. These were likely derived from ophiolitic sources. Garnets are predominantly almandinic and derived from rocks that had been metamorphosed up to the amphibolite facies, or magmatic rocks. Common pyrope-almandinic garnets indicate their source from granulites and eclogites. The main change after the Albian-Cenomanian period is the more expressed presence of the continental crust segments in the source area in comparison with ophiolites.
Recent submarine caves are inhabited by endemic faunas adapted to oligotrophism, darkness and a t... more Recent submarine caves are inhabited by endemic faunas adapted to oligotrophism, darkness and a tranquil environment. Many of their representatives are archaic types of animals resembling fossils from very early times in evolution. This article compares fossil fauna from Jurassic neptunian dykes (originally sea bed clefts) from the Western Carpathians with the Recent cave-dwelling fauna. The ostracods Pokornyopsis feifeli are particularly important. In the Western Carpathians, these were exclusively found in the Middle/Late Jurassic fissure fillings, but in the non-Tethyan Germanic Jurassic this species was found in deep-marine claystones. They are phylogenetic forerunners of the recent genus Danielopolina inhabiting both anchialine caves and deep seas. This indicates a Jurassic migration of deepmarine fauna to cryptic habitats. Other examples of cryptic communities include the Upper Jurassic cavity-dwelling fauna dominated by serpulids and scleractinian corals. Associated suspension feeders include thecideidine brachiopods, oysters, bryozoans, sponges, crinoids and sessile foraminifers. Serpuliddominated bioconstructions have recent analogies in the Mediterranean and Carribean seas. Different type of dyke communities represent the Late Jurassic fauna of small sized ammonites which originated from both Tethyan and Boreal paleobioprovinces. It has not been established whether these amonites were juvenile, dwarfed specimens adapted to limited cave space or size-sorted adult specimens.
Pieniny Klippen Belt is a mélange zone situated between the internides and externides of the West... more Pieniny Klippen Belt is a mélange zone situated between the internides and externides of the Western Carpathians. This complex zone consists of blocks of sedimentary rocks of various provenance. Most of them belonged to a crustal segment called Oravicum, which was surrounded by branches of Ligurian-Penninic-Vahic Ocean (Pieniny and Magura basins). The Pieniny Klippen Belt underwent several compressional and transpressional phases that caused expressive crustal shortening and mixing of blocks belonging to different tectonic units. At Revišné, in Orava sector of the Pieniny Klippen Belt, a klippe including Bajocian crinoidal limestones (Smolegowa and Krupianka limestone formations), accompanied with synsedimentary Krasín Breccia was found. These formations belong to the Czorsztyn Unit which was the shallowest of all the Oravic units. Occurrences of this unit are rare in the Orava territory and the occurrence of Krasín Breccia is the first outside the middle Váh Valley. The lower part of the klippe is formed by tectonically overturned succession ranging from Kimmeridgian red nodular limestone (Czorsztyn Limestone Formation), Lower Tithonian greenish-grey nodular limestone (Revišné Limestone), through Upper Tithonian to Hauterivian marly white Calpionella-Nannoconus limestone (Pieniny Limestone Formation) and Barremian-Aptian grey spotted marls (Kapuśnica Formation) up to Lower Albian marly shales (Wronine Formation). This succession does not fit to the Czorsztyn Unit which characteristically lacks Hauterivian to Aptian strata due to emersion and karstification. Lithology of this part of the klippe, together with strong condensation of the succession indicates that it may belong to the externmost, deep-water Grajcarek Unit which was deposited north of the Czorsztyn Unit. Contact of these two units is most likely tectonic. The Czorsztyn Unit is thrust onto the Grajcarek Unit providing two possible ways of interpretation: 1) Grajcarek Unit was thrust onto the Czorsztyn Unit and later both were overturned, 2) Czorsztyn Unit was thrust over the overturned Grajcarek Unit.
Geologia / Akademia Górniczo-Hutnicza im. Stanisława Staszica w Krakowie, 2009
Treae: W celu rozpoznania sk³adu minera³ów ciê¿kich rodkowojurajskich piasków i piaskowców, anali... more Treae: W celu rozpoznania sk³adu minera³ów ciê¿kich rodkowojurajskich piasków i piaskowców, analizie poddano utwory tego wieku z kilku ods³oniêae okolic Krakowa (Dêbnik, Dêbnik-Czatkowice, Rac³awice, Paczó³towice). Wykazano w ich obrêbie wysoki udzia³ minera³ów z grupy granatu, wska-zuj¹c na du¿e podobieñstwo do minera³ów tego typu znanych z zewnêtrznych Karpat Zachodnich. Tym niemniej bezporednie wskazanie obszaru ród³owego tych minera³ów nie jest mo¿liwe, a stwierdziae mo¿na jedynie, ¿e ten enigmatyczny region obfitowa³ w granulity, eklogity i perydotyty.
South-American table-top mountains (tepuis) are formed by quartzites and sandstones of Matauí For... more South-American table-top mountains (tepuis) are formed by quartzites and sandstones of Matauí Formation belonging to the Roraima Supergroup (Lower to Middle Proterozoic). Field observations in the northern part of Akopán Tepui in Venezuela revealed that unlike the beds with flat bedding, the cross-bedded layers are commonly affected by selective weathering, expressed by depressions, shelters, and even small caves. All the arenites are finegrained; most of them are likely of aeolian origin. Hardness measurements confirmed that the cross-bedded layers are softer than the flat-bedded or structureless beds occurring above and below them. Petrographic analysis showed that the rocks are mostly fine-grained quartzites to quartz sandstones, with original sand grains overgrown by syntaxial quartz cement and bearing signs of compaction manifested by local pressure solution. Some intergranular spaces are filled by newly-formed phyllosilicates (paragonite, locally intergrown with muscovite). In the overlying beds, no porosity was observed by microscopic study and under SEM, whereas in the underlying rocks signs of slight weathering and etching of phyllosilicates was observed, together with locally widened spaces along the grain-to-grain boundaries. The samples from cross-bedded layers display weathering, the degree of which depends on the present access of flowing water. Where water has periodical access to the arenite, it shows dissolution of quartz cement (arenization), together with complete leaching and removal of the phyllosilicates due to lateritization. The intergranular spaces are considerably widened and quartz grains bear signs of strong skeletal etching and pitting. Samples from the sites where the water access
The Czorsztyn Succession is the shallowest Pienidic unit of the West Carpathian Pieniny Klippen B... more The Czorsztyn Succession is the shallowest Pienidic unit of the West Carpathian Pieniny Klippen Belt. After the Valanginian, a hiatus encompassing almost the whole Hauterivian, Barremian and Aptian occurred in this unit. The Tithonian-Lower Cretaceous limestones are overlain by pelagic Albian-Cenomanian marlstones, marly limestones and cherts (Chmielowa and Pomiedznik Formations). The nature of this hiatus was so far unclear, either representing a submarine non-deposition and erosion, or subaerial exposure. The paper brings provides a summary of data collected from the literature and new data from 5 re-examined sites and 5 new sites: Dolný Mlyn, Vrsatec (3 sites), Horne Sŕnie, Lednica, Jarabina, Kamenica (all Slovakia), Czerwona Skala Klippe (Poland) and Vilki Dil (Ukraine). At two sites, the Albian marlstones and limestones overlie rocks older than Tithonian or Neocomian. In Jarabina, the Barremian-Aptian erosion reached the level of Kimmeridgian red micritic limestones, though clasts of limestones with "filamentous" microfacies indicate that Bathonian-Callovian limestones were also exposed and eroded. At Horne Sŕnie, the Albian deposits overlie Bajocian crinoidal limestones. The Bathonian to Hauterivian sediments are missing, which indicates that this part of the Czorsztyn sedimentary area experienced the deepest erosion. Unequivocal indicators of subaerial exposure and karstification, e.g. karren landform with vertical drainage grooves, small cavities in the bottom rock filled with younger sediment, bizarre fractures and veinlets filled with calcite, were revealed mainly at Horne Sŕnie and Lednica sites. The emersion was followed by pelagic of pelagic Albian marlstones and limestones. At this time, the palaeokarst surface was bored by bivalves and encrusted by deep-water Fe-Mn to phosphatic stromatolites. This suggests a very rapid relative sea-level rise, causing marine ingression. There were two transgression pulses in the Late Aptian and Albian, separated by a temporary emersion and karstification. The Upper Aptian sediments are still organodetrital with crinoids and other benthic fauna, whereas those of the Albian contain exclusively pelagic planktonic fauna.
D. Plašienka, J. Michalík, J. Soták & R. Aubrecht comment: In their recent paper, Golonka... more D. Plašienka, J. Michalík, J. Soták & R. Aubrecht comment: In their recent paper, Golonka et al. (2015) described the Cretaceous and Palaeogene olistostromes and other types of mass-transport deposits occurring within the Pieniny Klippen Belt (PKB) of the Western Carpathians. After a short introduction into the olistostrome concept and an overall description of the PKB structure, the authors presented their views on the composition and evolution of the PKB with olistostromes as the leading phenomenon. Although novel in some aspects, the model they present is largely oversimplified and partly erroneous in our opinion. In the following, we shall comment on the several most disputable statements and interpretations offered in the discussed paper.
The Pieniny Klippen Belt (boundary between the Central and Outer Western Carpathians) is a tecton... more The Pieniny Klippen Belt (boundary between the Central and Outer Western Carpathians) is a tectonic melange of various Mesozoic sedimentary units. In the shallowest unit, a Czorsztyn Succession, syntectonic Middle Jurassic (Bajocian) sedimentary breccia to megabreccia was discovered. It resulted from extensional tectonic movements tied to Jurassic Neotethys rifting. The breccia was investigated by standard petrographic methods, cathodoluminescence, microfacies analysis and isotope analysis (C, O). It represents the whole spectrum from crackled breccia, through mosaic breccia to mixed rubble breccia. All of them consist mostly of crinoidal limestone clasts. The crackled breccias are penetrated by a network of radiaxial fibrous calcite; the mosaic breccias have interstitial pores mostly filled with a younger generation of crinoidal limestone. The rubble breccia usually possesses the most complex filling. As a rule, the clasts are coated by at least one generation of stromatolite and then cemented by radiaxial fibrous calcite. The stromatolites may appear at various levels of the breccia diagenesis (most of them are cryptic stromatolites). The remaining void filling starts with the crinoidal detritus which indicates that the breccia was formed due to synsedimentary tectonics occurring during the deposition of crinoidal limestones (Bajocian). The rest was filled by micritic limestone with bfilamentousQ microfacies (Bathonian-Callovian), which also contained local planktonic foraminifers, Globuligerina sp. The latest sedimentary filling is represented by sterile micrite containing a few allochems and fauna of cavity-dwelling ostracods Pokornyopsis sp. The latest cement is represented by clear blocky calcite filling veinlets cutting the whole rock. Numerous instances of disturbance, resedimentation and recementation are evident in the breccia. The isotope composition of some early generations of stromatolites, local etching of the clasts and early cements, together with some earlier generations of blocky-calcite veinlets, possibly indicate a presence of freshwater diagenesis.
According to earlier concepts, the Czorsztyn Unit (Oravic Superunit, Pieniny Klippen Belt, Wester... more According to earlier concepts, the Czorsztyn Unit (Oravic Superunit, Pieniny Klippen Belt, Western Carpathians) sedimented on the isolated Czorsztyn Swell which existed in the Middle Jurassic-Late Cretaceous time in the realm of the Outer Western Carpathians. This paper brings new data providing an alternative interpretation of its Cretaceous evolution. They are based on heavy mineral analysis of the Upper Aptian/Lower Albian sediments of the Czorsztyn Unit. They rest upon a karstified surface after a Hauterivian-Aptian emersion and are represented by condensed, red marly organodetritic limestones with some terrigenous admixture (Chmielowa Formation). The heavy mineral spectrum is dominated by spinels, followed by garnet, with lesser amounts of zircon, rutile and tourmaline. The composition of the majority of the detrital garnets shows that they were derived from primary HP/UHP parental rocks which were recrystallized under granulite and amphibolite facies conditions. The garnets were most probably derived directly from the magmatic and metamorphic rocks of the Oravic basement, as the high-pyrope garnets are known to be abundant in Mesozoic sediments all over the Outer Western Carpathians. The presence of spinels is surprising. According to their chemistry, they were mostly derived from mid-oceanic ridge basalts (MORB) peridotites, supra-subduction zone peridotites (harzburgites) and transitional lherzolite/ harzburgite types. Only a lesser amount of spinels was derived from volcanics of BABB composition (back-arc basin basalts). The presence of this ophiolitic detritus in the Czorsztyn Unit is difficult to explain. Ophiolitic detritus appeared in the Aptian/Albian time only in the units which were considered to be more distant, because they were situated at the boundary between the Central and the Outer Western Carpathians (Klape Unit, Tatric and Fatric domains). The hypothetical Exotic Ridge which represented an accretionary wedge in front of the overriding Western Carpathian internides was considered to be a source of the clastics. In previous paleogeographical reconstructions, the Czorsztyn Unit was situated north of the Pieniny Trough (considered to be one of the branches of the Penninic-Vahic Ocean). In the trough itself, the ophiolitic detritus appeared as late as in the Senonian and there was no way it could reach the Czorsztyn Swell which was considered to be an isolated elevation. The new results presented herein show that these reconstructions do not fit the obtained data and infer a possibility that the Czorsztyn sedimentary area was not isolated in the Cretaceous time and it was situated closer to the Central Carpathian units than previously thought. A new paleogeographical model of the evolution of the Pieniny Klippen Belt is presented in the paper: Oravic segment was derived from the Moldanubian Zone of the Bohemian Massif by the Middle Jurassic rifting which caused block tilting where most of the Oravic units were arranged north of the Czorsztyn Swell. The Oravic segment was situated in the lateral continuation of the Central and Inner Western Carpathians from which it was detached by later clockwise rotation. The Oravic segment was then laterally shifted in front of the Central Western Carpathians, together with remnants of the Meliatic suture zone which represented a source for the exotics to the Klape, Tatric, Fatric and Oravic units.
Through out the Cre ta ceous, Tethyan oce anic branches grad u ally closed, and var i ous ophioli... more Through out the Cre ta ceous, Tethyan oce anic branches grad u ally closed, and var i ous ophiolites be came obducted and eroded. Their rem nants, how ever, pro vide an abun dance of ex otic clasts of un known or i gin. Sand stone sam ples from the old est, Albian exotics-bear ing strata of the Pieniny Klippen Belt and Cen tral West ern Carpathians were ana lysed for heavy min er als. These sam ples were dom i nated by a high con tent of chrome-spi nels, zir con, tour ma line, ap a tite and rutile. Ti tan ite, kyan ite, monazite, epidote, sillimanite and staurolite were much less abun dant. Gar net was gen er ally also rare; how ever, it was lo cally com mon, as were blue am phi boles, py rox enes and kyan ite. The spi nels found in the sam ples were pre dom inantly de rived from harzburgites (su pra-subduction peri dot ites and vol ca nic rocks). The blue am phi boles rep re sented glaucophanes to ferroglaucophanes, and were de rived from HP/LT metabasites. Py rox enes (en sta tite, less com monly augite and di op side) most likely came from co eval volcanics. Most of the tour ma lines were de rived from metasedimentary rocks and lo cally from granitoids. Fur ther more, some have a com plex zonation with two phases of tour ma line, or tour ma line intergrown with quartz. These were likely de rived from ophiolitic sources. The re sults from our anal y sis in di cate a dom i nance of ophiolites and older sed i ments with lo cal in put of con ti nen tal crust meta mor phic rocks. A re sult ing palaeogeographic recon struc tion in volves sec ond ary dou bling of the Neotethys su ture zone and its lat eral shift north of the Cen tral West ern Carpathians, which formed a com mon source for exotics in the Pieniny Klippen Belt and the Cen tral West ern Carpathians.
Four occurrences of Jurassic stromatactis mud-mounds were found in the Czorsztyn Unit of the Pien... more Four occurrences of Jurassic stromatactis mud-mounds were found in the Czorsztyn Unit of the Pieniny Klippen Belt (Western Carpathians)in western Slovakia (Slavnické Podhorie, Babiná), and in the Transcarpathian Ukraine (Priborzhavskoe and Veliky Kamenets). Their stratigraphic range is from Bajocian to Callovian. The mounds consist of micropeloidal mudstones, wackestones to packstones with a fauna including pelecypods, brachiopods, ammonites and crinoids. Spicules and skeletons of siliceous sponges are abundant in every section. All of the mounds contain networks of stromatactis cavities that are partially filled with radiaxial fibrous calcite (RFC) and locally by internal sediments. At Slavnické Podhorie, the sparry masses that fill stromatactis cavities are weathered out and show casts of sponges. Parallel study of the weathered casts and their cross-sections in slabs showed that they bear all the signs of stromatactis (relatively flat bottoms and digitate upper parts, RFC initial fillings and eventual blocky calcite later filling). Almost no original sponge structures were preserved. This strongly supports the possible sponge-related origin for stromatactis cavities.
The studied Cretaceous flysch succession of the Pieniny Klippen Belt in the Orava territory is si... more The studied Cretaceous flysch succession of the Pieniny Klippen Belt in the Orava territory is similar to the Kysuca Unit where the lower, sandstone flysch (Snežnica Beds) and the upper, conglomerate flysch (Sromowce Formation) were distinguished (Andrusov and Samuel, 1985). Although the studied flysch successions at the Zemianska Dedina locality show sequences similar to the other localities in the Orava territory, there are some differences, mainly in the bed thickness, sandstones/claystones ratio, as well as in the presence of thick slump and slide matrix-supported conglomerate bodies. The sedimentological and stratigraphical evaluations of the section revealed mostly thinto medium-rhythmic turbiditic development. The cyclicity of the thickening-upward sequences, relatively high lateral stability of the beds, their smaller thickness, presence of the Bouma´s intervals and the assemblage of ichnofossils point to a deposition at the slope toe, within the central to outer part of deep-sea fans, rarely dissected by migrating feeding channels filled with upward-fining graded conglomerates and sandstones. The thick matrix-supported conglomerate bodies represent a result of slump and slides on steep submarine slopes transformed to debris-flows and mud-flows that transported sedimentary loads as far as the distal part of the turbiditic fans.
This paper brings results of the first systematic heavy-mineral analysis of the oldest exotics-be... more This paper brings results of the first systematic heavy-mineral analysis of the oldest exotics-bearing units in the Western Carpathians. Samples the Klape Unit, Poruba Formation (Tatric and Fatric units), Manín Unit and Orava Unit were analyzed. Most samples are dominated by chrome-spinels, zircon, tourmaline, apatite and rutile in various ratios. Garnet occurs in small amounts but there is considerable enrichment in a few samples. Titanite, kyanite, monazite and epidote occur only rarely; sillimanite and staurolite are very rare. There is also a local enrichment in blue amphiboles, pyroxenes, garnet and kyanite in some samples. The analyzed spinel grains predominantly match the harzburgite field, with some overlap to the fields of podiform chromitites and cumulates in the Mg/(Mg + Fe 2+) vs. Cr/(Cr + Al) diagram. The TiO 2 vs. Al 2 O 3 diagram indicates the predominant origin of spinels from the supra-subduction zone peridotites for most of the analyses, whereas the other, aluminium-depleted and higher-titanium grains best match the arc volcanic field. The analyzed blue amphiboles are glaucophanes to ferroglaucophanes and were most likely derived from HP/UHP metamorphosed basaltic rocks in a subduction zone. Pyroxenes are mostly represented by orthopyroxenes (enstatite) and less by clinopyroxenes (augite, diopside). Their common euhedral shape and fresh appearance indicate that they were probably not derived from the same ophiolitic source as the Cr-spinels and blue amphiboles, but rather from some adjacent and nearly coeval volcanics which might be of calc-alkaline provenance. Detrital tourmaline grains in the analyzed samples were mostly unzoned except of some grains; some even possessed a complex intergrowing pattern with a mosaic appearance. Most of the grains were derived from various sorts of metasediments. Almost all tourmaline grains from Havranský vrch Hill were likely derived from Li-poor granitoid rocks. The results indicate input of minerals of dominantly ophiolitic provenance, such as Cr-spinels, blue amphiboles, and eventually mosaic tourmaline. Zircon, rest of the tourmaline and rutile were likely derived from older sediments. Garnet, staurolite, kyanite, sillimanite occurring in relatively small amounts were mostly derived from metamorphic rocks of various degrees of metamorphism. No significant differences were observed among the individual units which most likely shared the same source.
Turonian to Maastrichtian exotics-bearing deposits from the Pieniny Klippen Belt (Klape and Kysuc... more Turonian to Maastrichtian exotics-bearing deposits from the Pieniny Klippen Belt (Klape and Kysuca units) and from the Považský Inovec Mts. (Western Carpathians) were analyzed for heavy minerals and compared with similar, yet older Albian-Cenomanian deposits. The Turonian to Maastrichtian deposits are petrographically more variable in composition in the entire range, from quartz arenites to litharenites. Percentages of the main heavy minerals are similar on both stratigraphic levels, i.e., they are dominated by chrome-spinels, zircon, tourmaline, apatite, and rutile. Garnet is more common in the Turonian to Maastrichtian samples, while titanite, kyanite, monazite, hornblende, blue amphibole, pyroxenes, epidote, staurolite, and sillimanite are quite rare. Statistical factor analysis indicates dominance of ophiolites and older sediments in the source areas. One important factor is an influx of garnet, with the weakest factor being related to the influx of tourmaline and apatite, which may indicate low-grade metamorphics. Spinels were derived from harzburgites (supra-subduction peridotites). The majority of tourmalines were derived from metasediments, Fe 3+-rich quartztourmaline rocks, calc-silicate rocks, and metapelites and granitoids. Some had complex zonation with two phases of tourmaline (schorl-dravite and bosiite), or tourmaline intergrown with quartz. These were likely derived from ophiolitic sources. Garnets are predominantly almandinic and derived from rocks that had been metamorphosed up to the amphibolite facies, or magmatic rocks. Common pyrope-almandinic garnets indicate their source from granulites and eclogites. The main change after the Albian-Cenomanian period is the more expressed presence of the continental crust segments in the source area in comparison with ophiolites.
Recent submarine caves are inhabited by endemic faunas adapted to oligotrophism, darkness and a t... more Recent submarine caves are inhabited by endemic faunas adapted to oligotrophism, darkness and a tranquil environment. Many of their representatives are archaic types of animals resembling fossils from very early times in evolution. This article compares fossil fauna from Jurassic neptunian dykes (originally sea bed clefts) from the Western Carpathians with the Recent cave-dwelling fauna. The ostracods Pokornyopsis feifeli are particularly important. In the Western Carpathians, these were exclusively found in the Middle/Late Jurassic fissure fillings, but in the non-Tethyan Germanic Jurassic this species was found in deep-marine claystones. They are phylogenetic forerunners of the recent genus Danielopolina inhabiting both anchialine caves and deep seas. This indicates a Jurassic migration of deepmarine fauna to cryptic habitats. Other examples of cryptic communities include the Upper Jurassic cavity-dwelling fauna dominated by serpulids and scleractinian corals. Associated suspension feeders include thecideidine brachiopods, oysters, bryozoans, sponges, crinoids and sessile foraminifers. Serpuliddominated bioconstructions have recent analogies in the Mediterranean and Carribean seas. Different type of dyke communities represent the Late Jurassic fauna of small sized ammonites which originated from both Tethyan and Boreal paleobioprovinces. It has not been established whether these amonites were juvenile, dwarfed specimens adapted to limited cave space or size-sorted adult specimens.
Pieniny Klippen Belt is a mélange zone situated between the internides and externides of the West... more Pieniny Klippen Belt is a mélange zone situated between the internides and externides of the Western Carpathians. This complex zone consists of blocks of sedimentary rocks of various provenance. Most of them belonged to a crustal segment called Oravicum, which was surrounded by branches of Ligurian-Penninic-Vahic Ocean (Pieniny and Magura basins). The Pieniny Klippen Belt underwent several compressional and transpressional phases that caused expressive crustal shortening and mixing of blocks belonging to different tectonic units. At Revišné, in Orava sector of the Pieniny Klippen Belt, a klippe including Bajocian crinoidal limestones (Smolegowa and Krupianka limestone formations), accompanied with synsedimentary Krasín Breccia was found. These formations belong to the Czorsztyn Unit which was the shallowest of all the Oravic units. Occurrences of this unit are rare in the Orava territory and the occurrence of Krasín Breccia is the first outside the middle Váh Valley. The lower part of the klippe is formed by tectonically overturned succession ranging from Kimmeridgian red nodular limestone (Czorsztyn Limestone Formation), Lower Tithonian greenish-grey nodular limestone (Revišné Limestone), through Upper Tithonian to Hauterivian marly white Calpionella-Nannoconus limestone (Pieniny Limestone Formation) and Barremian-Aptian grey spotted marls (Kapuśnica Formation) up to Lower Albian marly shales (Wronine Formation). This succession does not fit to the Czorsztyn Unit which characteristically lacks Hauterivian to Aptian strata due to emersion and karstification. Lithology of this part of the klippe, together with strong condensation of the succession indicates that it may belong to the externmost, deep-water Grajcarek Unit which was deposited north of the Czorsztyn Unit. Contact of these two units is most likely tectonic. The Czorsztyn Unit is thrust onto the Grajcarek Unit providing two possible ways of interpretation: 1) Grajcarek Unit was thrust onto the Czorsztyn Unit and later both were overturned, 2) Czorsztyn Unit was thrust over the overturned Grajcarek Unit.
Geologia / Akademia Górniczo-Hutnicza im. Stanisława Staszica w Krakowie, 2009
Treae: W celu rozpoznania sk³adu minera³ów ciê¿kich rodkowojurajskich piasków i piaskowców, anali... more Treae: W celu rozpoznania sk³adu minera³ów ciê¿kich rodkowojurajskich piasków i piaskowców, analizie poddano utwory tego wieku z kilku ods³oniêae okolic Krakowa (Dêbnik, Dêbnik-Czatkowice, Rac³awice, Paczó³towice). Wykazano w ich obrêbie wysoki udzia³ minera³ów z grupy granatu, wska-zuj¹c na du¿e podobieñstwo do minera³ów tego typu znanych z zewnêtrznych Karpat Zachodnich. Tym niemniej bezporednie wskazanie obszaru ród³owego tych minera³ów nie jest mo¿liwe, a stwierdziae mo¿na jedynie, ¿e ten enigmatyczny region obfitowa³ w granulity, eklogity i perydotyty.
South-American table-top mountains (tepuis) are formed by quartzites and sandstones of Matauí For... more South-American table-top mountains (tepuis) are formed by quartzites and sandstones of Matauí Formation belonging to the Roraima Supergroup (Lower to Middle Proterozoic). Field observations in the northern part of Akopán Tepui in Venezuela revealed that unlike the beds with flat bedding, the cross-bedded layers are commonly affected by selective weathering, expressed by depressions, shelters, and even small caves. All the arenites are finegrained; most of them are likely of aeolian origin. Hardness measurements confirmed that the cross-bedded layers are softer than the flat-bedded or structureless beds occurring above and below them. Petrographic analysis showed that the rocks are mostly fine-grained quartzites to quartz sandstones, with original sand grains overgrown by syntaxial quartz cement and bearing signs of compaction manifested by local pressure solution. Some intergranular spaces are filled by newly-formed phyllosilicates (paragonite, locally intergrown with muscovite). In the overlying beds, no porosity was observed by microscopic study and under SEM, whereas in the underlying rocks signs of slight weathering and etching of phyllosilicates was observed, together with locally widened spaces along the grain-to-grain boundaries. The samples from cross-bedded layers display weathering, the degree of which depends on the present access of flowing water. Where water has periodical access to the arenite, it shows dissolution of quartz cement (arenization), together with complete leaching and removal of the phyllosilicates due to lateritization. The intergranular spaces are considerably widened and quartz grains bear signs of strong skeletal etching and pitting. Samples from the sites where the water access
The Czorsztyn Succession is the shallowest Pienidic unit of the West Carpathian Pieniny Klippen B... more The Czorsztyn Succession is the shallowest Pienidic unit of the West Carpathian Pieniny Klippen Belt. After the Valanginian, a hiatus encompassing almost the whole Hauterivian, Barremian and Aptian occurred in this unit. The Tithonian-Lower Cretaceous limestones are overlain by pelagic Albian-Cenomanian marlstones, marly limestones and cherts (Chmielowa and Pomiedznik Formations). The nature of this hiatus was so far unclear, either representing a submarine non-deposition and erosion, or subaerial exposure. The paper brings provides a summary of data collected from the literature and new data from 5 re-examined sites and 5 new sites: Dolný Mlyn, Vrsatec (3 sites), Horne Sŕnie, Lednica, Jarabina, Kamenica (all Slovakia), Czerwona Skala Klippe (Poland) and Vilki Dil (Ukraine). At two sites, the Albian marlstones and limestones overlie rocks older than Tithonian or Neocomian. In Jarabina, the Barremian-Aptian erosion reached the level of Kimmeridgian red micritic limestones, though clasts of limestones with "filamentous" microfacies indicate that Bathonian-Callovian limestones were also exposed and eroded. At Horne Sŕnie, the Albian deposits overlie Bajocian crinoidal limestones. The Bathonian to Hauterivian sediments are missing, which indicates that this part of the Czorsztyn sedimentary area experienced the deepest erosion. Unequivocal indicators of subaerial exposure and karstification, e.g. karren landform with vertical drainage grooves, small cavities in the bottom rock filled with younger sediment, bizarre fractures and veinlets filled with calcite, were revealed mainly at Horne Sŕnie and Lednica sites. The emersion was followed by pelagic of pelagic Albian marlstones and limestones. At this time, the palaeokarst surface was bored by bivalves and encrusted by deep-water Fe-Mn to phosphatic stromatolites. This suggests a very rapid relative sea-level rise, causing marine ingression. There were two transgression pulses in the Late Aptian and Albian, separated by a temporary emersion and karstification. The Upper Aptian sediments are still organodetrital with crinoids and other benthic fauna, whereas those of the Albian contain exclusively pelagic planktonic fauna.
D. Plašienka, J. Michalík, J. Soták & R. Aubrecht comment: In their recent paper, Golonka... more D. Plašienka, J. Michalík, J. Soták & R. Aubrecht comment: In their recent paper, Golonka et al. (2015) described the Cretaceous and Palaeogene olistostromes and other types of mass-transport deposits occurring within the Pieniny Klippen Belt (PKB) of the Western Carpathians. After a short introduction into the olistostrome concept and an overall description of the PKB structure, the authors presented their views on the composition and evolution of the PKB with olistostromes as the leading phenomenon. Although novel in some aspects, the model they present is largely oversimplified and partly erroneous in our opinion. In the following, we shall comment on the several most disputable statements and interpretations offered in the discussed paper.
The Pieniny Klippen Belt (boundary between the Central and Outer Western Carpathians) is a tecton... more The Pieniny Klippen Belt (boundary between the Central and Outer Western Carpathians) is a tectonic melange of various Mesozoic sedimentary units. In the shallowest unit, a Czorsztyn Succession, syntectonic Middle Jurassic (Bajocian) sedimentary breccia to megabreccia was discovered. It resulted from extensional tectonic movements tied to Jurassic Neotethys rifting. The breccia was investigated by standard petrographic methods, cathodoluminescence, microfacies analysis and isotope analysis (C, O). It represents the whole spectrum from crackled breccia, through mosaic breccia to mixed rubble breccia. All of them consist mostly of crinoidal limestone clasts. The crackled breccias are penetrated by a network of radiaxial fibrous calcite; the mosaic breccias have interstitial pores mostly filled with a younger generation of crinoidal limestone. The rubble breccia usually possesses the most complex filling. As a rule, the clasts are coated by at least one generation of stromatolite and then cemented by radiaxial fibrous calcite. The stromatolites may appear at various levels of the breccia diagenesis (most of them are cryptic stromatolites). The remaining void filling starts with the crinoidal detritus which indicates that the breccia was formed due to synsedimentary tectonics occurring during the deposition of crinoidal limestones (Bajocian). The rest was filled by micritic limestone with bfilamentousQ microfacies (Bathonian-Callovian), which also contained local planktonic foraminifers, Globuligerina sp. The latest sedimentary filling is represented by sterile micrite containing a few allochems and fauna of cavity-dwelling ostracods Pokornyopsis sp. The latest cement is represented by clear blocky calcite filling veinlets cutting the whole rock. Numerous instances of disturbance, resedimentation and recementation are evident in the breccia. The isotope composition of some early generations of stromatolites, local etching of the clasts and early cements, together with some earlier generations of blocky-calcite veinlets, possibly indicate a presence of freshwater diagenesis.
According to earlier concepts, the Czorsztyn Unit (Oravic Superunit, Pieniny Klippen Belt, Wester... more According to earlier concepts, the Czorsztyn Unit (Oravic Superunit, Pieniny Klippen Belt, Western Carpathians) sedimented on the isolated Czorsztyn Swell which existed in the Middle Jurassic-Late Cretaceous time in the realm of the Outer Western Carpathians. This paper brings new data providing an alternative interpretation of its Cretaceous evolution. They are based on heavy mineral analysis of the Upper Aptian/Lower Albian sediments of the Czorsztyn Unit. They rest upon a karstified surface after a Hauterivian-Aptian emersion and are represented by condensed, red marly organodetritic limestones with some terrigenous admixture (Chmielowa Formation). The heavy mineral spectrum is dominated by spinels, followed by garnet, with lesser amounts of zircon, rutile and tourmaline. The composition of the majority of the detrital garnets shows that they were derived from primary HP/UHP parental rocks which were recrystallized under granulite and amphibolite facies conditions. The garnets were most probably derived directly from the magmatic and metamorphic rocks of the Oravic basement, as the high-pyrope garnets are known to be abundant in Mesozoic sediments all over the Outer Western Carpathians. The presence of spinels is surprising. According to their chemistry, they were mostly derived from mid-oceanic ridge basalts (MORB) peridotites, supra-subduction zone peridotites (harzburgites) and transitional lherzolite/ harzburgite types. Only a lesser amount of spinels was derived from volcanics of BABB composition (back-arc basin basalts). The presence of this ophiolitic detritus in the Czorsztyn Unit is difficult to explain. Ophiolitic detritus appeared in the Aptian/Albian time only in the units which were considered to be more distant, because they were situated at the boundary between the Central and the Outer Western Carpathians (Klape Unit, Tatric and Fatric domains). The hypothetical Exotic Ridge which represented an accretionary wedge in front of the overriding Western Carpathian internides was considered to be a source of the clastics. In previous paleogeographical reconstructions, the Czorsztyn Unit was situated north of the Pieniny Trough (considered to be one of the branches of the Penninic-Vahic Ocean). In the trough itself, the ophiolitic detritus appeared as late as in the Senonian and there was no way it could reach the Czorsztyn Swell which was considered to be an isolated elevation. The new results presented herein show that these reconstructions do not fit the obtained data and infer a possibility that the Czorsztyn sedimentary area was not isolated in the Cretaceous time and it was situated closer to the Central Carpathian units than previously thought. A new paleogeographical model of the evolution of the Pieniny Klippen Belt is presented in the paper: Oravic segment was derived from the Moldanubian Zone of the Bohemian Massif by the Middle Jurassic rifting which caused block tilting where most of the Oravic units were arranged north of the Czorsztyn Swell. The Oravic segment was situated in the lateral continuation of the Central and Inner Western Carpathians from which it was detached by later clockwise rotation. The Oravic segment was then laterally shifted in front of the Central Western Carpathians, together with remnants of the Meliatic suture zone which represented a source for the exotics to the Klape, Tatric, Fatric and Oravic units.
Through out the Cre ta ceous, Tethyan oce anic branches grad u ally closed, and var i ous ophioli... more Through out the Cre ta ceous, Tethyan oce anic branches grad u ally closed, and var i ous ophiolites be came obducted and eroded. Their rem nants, how ever, pro vide an abun dance of ex otic clasts of un known or i gin. Sand stone sam ples from the old est, Albian exotics-bear ing strata of the Pieniny Klippen Belt and Cen tral West ern Carpathians were ana lysed for heavy min er als. These sam ples were dom i nated by a high con tent of chrome-spi nels, zir con, tour ma line, ap a tite and rutile. Ti tan ite, kyan ite, monazite, epidote, sillimanite and staurolite were much less abun dant. Gar net was gen er ally also rare; how ever, it was lo cally com mon, as were blue am phi boles, py rox enes and kyan ite. The spi nels found in the sam ples were pre dom inantly de rived from harzburgites (su pra-subduction peri dot ites and vol ca nic rocks). The blue am phi boles rep re sented glaucophanes to ferroglaucophanes, and were de rived from HP/LT metabasites. Py rox enes (en sta tite, less com monly augite and di op side) most likely came from co eval volcanics. Most of the tour ma lines were de rived from metasedimentary rocks and lo cally from granitoids. Fur ther more, some have a com plex zonation with two phases of tour ma line, or tour ma line intergrown with quartz. These were likely de rived from ophiolitic sources. The re sults from our anal y sis in di cate a dom i nance of ophiolites and older sed i ments with lo cal in put of con ti nen tal crust meta mor phic rocks. A re sult ing palaeogeographic recon struc tion in volves sec ond ary dou bling of the Neotethys su ture zone and its lat eral shift north of the Cen tral West ern Carpathians, which formed a com mon source for exotics in the Pieniny Klippen Belt and the Cen tral West ern Carpathians.
Four occurrences of Jurassic stromatactis mud-mounds were found in the Czorsztyn Unit of the Pien... more Four occurrences of Jurassic stromatactis mud-mounds were found in the Czorsztyn Unit of the Pieniny Klippen Belt (Western Carpathians)in western Slovakia (Slavnické Podhorie, Babiná), and in the Transcarpathian Ukraine (Priborzhavskoe and Veliky Kamenets). Their stratigraphic range is from Bajocian to Callovian. The mounds consist of micropeloidal mudstones, wackestones to packstones with a fauna including pelecypods, brachiopods, ammonites and crinoids. Spicules and skeletons of siliceous sponges are abundant in every section. All of the mounds contain networks of stromatactis cavities that are partially filled with radiaxial fibrous calcite (RFC) and locally by internal sediments. At Slavnické Podhorie, the sparry masses that fill stromatactis cavities are weathered out and show casts of sponges. Parallel study of the weathered casts and their cross-sections in slabs showed that they bear all the signs of stromatactis (relatively flat bottoms and digitate upper parts, RFC initial fillings and eventual blocky calcite later filling). Almost no original sponge structures were preserved. This strongly supports the possible sponge-related origin for stromatactis cavities.
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