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EN
We present evidence for the uppermost Jurassic-lowest Cretaceous interval in Crimea, coastal southern Ukraine. Three facies zones are distinguished in the upper Dvuyakornaya and the Mayak formations of the eastern Crimean Peninsula: basinal, slope and toe-of-slope zones. In this interval we identify the lowest Berriasian Jacobi and Grandis subzones of authors, in expanded form, exceeding 160 metres in thickness. We present new magnetostratigraphic interpretations, and identify two normal and two reversed polarity intervals, assigned to M19n, M18r, M18n and M17r, with M19n2n, M19n1r and M19n1n identified in the uppermost Dvuyakornaya Formation. In the Mayak Formation we record the top of M19n.1n, with M18r, M18n and a thick M17r above. In these two formations component calpionellid species have been identified which characterise the Alpina, Ferasini and Elliptica subzones (Calpionella Zone). In M19n, the FADs of the calcareous nannofossils Hexalithus strictus, Cruciellipsis cuvillieri, Nannoconus wintereri, N. steinmannii minor and N. kamptneri minor are found, which is consistent with other Tethyan regions. N. steinmannii steinmannii and N. kamptneri kamptneri first appear in M18r at Ili Burnu . Specimens of the apparently Tithonian foraminiferan index Anchispirocyclina lusitanica are found, but in the Berriasian lower Mayak Formation.
EN
The lower and middle Berriasian sedimentary succession of the Sidi Kralif Formation has been a subject of biostratigraphic study in two key sections in Central Tunisia. Our contribution is an attempt to better define the basal Berriasian interval, between the Berriasella jacobi Zone and the Subthurmannia occitanica Zone. Zonal schemes are established using ammonites and calpionellids, and these permit correlation with other regions of Mediterranean Tethys and beyond. The use of biomarkers afforded by microfossil groups has allowed characterization and direct correlation with four widely accepted calpionellid sub-zones, namely Calpionella alpina, Remaniella, Calpionella elliptica and Tintinopsella longa. The two ammonite zones of Berriasella jacobi and of Subthurmannia occitanica are recognised on the basis of their index species. The parallel ammonite and calpionellid zonations are useful as a tool for correlation and calibration in time and space, thus allowing a better definition of a J/K boundary. The presence of four Berriasian calpionellid bioevents is recognised: (1) the ‘explosion’ of Calpionella alpina, (2) the first occurrence of Remaniella, (3) the first occurrence of Calpionella elliptica and (4) the first occurrence of Tintinopsella longa. The last is here documented as coeval with the presence of Subthurmannia occitanica, which marks the lower/middle Berriasian boundary.
EN
Status and correlation of Andean ammonite biozones are reviewed. Available calpionellid, nannofossil, and radiolarian data, as well as radioisotopic ages, are also considered, especially when directly related to ammonite zones. There is no attempt to deal with the definition of the Jurassic–Cretaceous limit. Correlation of the V. mendozanum Zone with the Semiforme Zone is ratified, but it is open to question if its lower part should be correlated with the upper part of the Darwini Zone. The Pseudolissoceras zitteli Zone is characterized by an assemblage also recorded from Mexico, Cuba and the Betic Ranges of Spain, indicative of the Semiforme–Fallauxi standard zones. The Aulacosphinctes proximus Zone, which is correlated with the Ponti Standard Zone, appears to be closely related to the overlying Windhauseniceras internispinosum Zone, although its biostratigraphic status needs to be reconsidered. On the basis of ammonites, radiolarians and calpionellids the Windhauseniceras internispinosum Assemblage Zone is approximately equivalent to the Suarites bituberculatum Zone of Mexico, the Paralytohoplites caribbeanus Zone of Cuba and the Simplisphinctes/Microcanthum Zone of the Standard Zonation. The C. alternans Zone could be correlated with the uppermost Microcanthum and “Durangites” zones, although in west central Argentina it could be mostly restricted to levels equivalent to the “Durangites Zone”. The Substeueroceras koeneni Zone ranges into the Occitanica Zone, Subalpina and Privasensis subzones, the A. noduliferum Zone could be equivalent to the Dalmasi Subzone, Occitanica Zone, to lower part of the Boissieri Zone, and the S. damesi Zone could range through the upper part of the Boissieri Zone to the lower part of the Pertransiens Zone. Division of the Substeueroceras koeneni Zone and a precise correlation between the Andean ammonite zones and the international standard require new systematic and stratigraphic studies.
EN
Detailed bed-by-bed sampling on an outcrop of the La Casita and Taraises formations in northeastern Mexico (San José de Iturbide, Nuevo León State) allows the delimitation of the Jurassic/Cretaceous boundary. The Late Tithonian was determined by the presence of the Crassicollaria Zone (Colomi Subzone). Underlying subzones (Remanei and Brevis) were not identified due to the scarcity and poor preservation of calpionellids. The Jurassic/Cretaceous boundary was defined by the acme of the small and spherical form of the species Calpionella alpina Lorenz in sample IT-120. The Berriasian was divided into two zones and five subzones: the Calpionella Zone (Alpina, Ferasini and Elliptica subzones) and the Calpionellopsis Zone (Simplex and Oblonga subzones). The facies studied indicate that deposition during the Tithonian occurred in a toe of slope environment with occasional deep shelf incursions. Near the Jurassic/Cretaceous boundary, a sea level drop is recorded and the facies indicate a slope environment with the occurrence of a breccia level. A general deepening of the environments recorded within the frame of the Elliptica Subzone where the deposits pass into basinal facies
EN
Integrated bio- and magnetostratigraphic data from the Lower to Upper Berriasian of the pelagic succession at Barlya (Western Balkan, Bulgaria) are presented. The investigated interval, 24 m thick, covers the top of the Calpionella elliptica, Calpionellopsis simplex and Calpionellopsis oblonga subzones. Magnetozones from the upper part of M17r up to M16n were identified. The boundary between the Elliptica and Simplex subzones correlates with the lower part of M16r, while the boundary between the Simplex and Oblonga subzones is situated in the lower part of M16n. The magnetic susceptibility reveals an increasing trend from the middle part of M16r which accounts for the increasing supply of fine clastic sediments to the basin.
EN
A calpionellid zonal scheme is proposed for the Tithonian through Valanginian pelagic carbonates of the Western Balkan Unit, based on the vertical ranges of 57 chitinoidellid and calpionellid species recognized. This zonal scheme consists of calpionellid zones that are widely accepted in the Mediterranean Realm, such as the zones of Chitinoidella, Praetintinnopsella, Crassicollaria, Calpionella, Calpionellopsis, Calpionellites and Tintinnopsella. Subzonal divisions are comparable to those in the Carpathians. Direct correlations between ammonite and calpionellid ranges suggest that the base of the Upper Tithonian corresponds to the FO of Chitinoidella boneti; that of the Upper Berriasian to the FO of the genus Calpionellopsis; and the base and top of the Lower Valanginian to the FO and LO of the genus Calpionellites respectively. Correlations of the calpionellid zonation in the study area with zonations in other areas are discussed.
EN
The Upper Jurassic strata of the Krížna Unit in the Tatra Mts. comprises pelagic, fine-grained and well-oxygenated deposits. They are represented by red radiolarites and radiolarian limestones (Czajakowa Radiolarites Formation), red nodular limestones (Czorsztyn Limestones Formation) and wavy, platy or nodular light grey and reddish limestones and marlstones (Jasenina Formation). These deposits are mainly wackestones characterized by a succession of the following microfacies: radiolarian, filament-Saccocoma, Saccocoma and Globochaete–Saccocoma. The section comprises four calcareous dinoflagellate zones, i.e. the Late Kimmeridgian Moluccana Zone, and the Early Tithonian Borzai, Pulla and Malmica zones. In the uppermost part of the studied section, the Early Tithonian Dobeni Subzone of the Chitinoidella Zone has been identified. Using these biostratigraphic data, the sedimentation rate for the Late Kimmeridgian (Borzai Zone) and Early Tithonian (Dobeni Subzone of the Chitinoidella Zone) interval is estimated as 3.7 m/my. This is in accordance with the general trend of increasing sedimentation rate through the Tithonian and Berriasian. The increased supply of clastic material in the Jasenina Formation may have been caused by climate changes and continental weathering. The sedimentation was controlled mainly by eustatic changes and fluctuations in ACD and CCD levels.
EN
The Veliky Kamenets section in the eastern part of the Pieniny Klippen Belt in the Ukrainian Carpathians shows a well exposed, 83 m thick succession composed of Jurassic and lowermost Cretaceous (Berriasian) deposits. The terrigenous part of the section includes: gravels with a sandy matrix (unit 1A), massive grey-green sandstones (unit 1B) and shales with intercalations of siltstones/sandstones and oyster/gastropod lumachelles (unit 2). Organic-walled dinoflagellates document the Toarcian-Aalenian age of the siliciclastic deposits of unit 2. The carbonate part of the succession embraces: stromatactis mud-mounds interfingering with crinoidal limestones (unit 3A), lower nodular limestones (unit 3B), cherty limestones (unit 3C), upper nodular limestones (unit 3D), pink pelitic limestones (unit 3E), limestones with a volcanogenic bed (unit 5) and limestone breccia limestones (unit 6). This succession has yielded abundant ammonites from the Bathonian, Oxfordian and Kimmeridgian (with a stratigraphical hiatus covering the Callovian and Lower Oxfordian), as well as calcareous dinoflagellates (from the Upper Oxfordian towards the top of the succession), and calpionellids (in the Tithonian and Berriasian). Detailed stratigraphical study of the succession based both on ammonites and microfossils has resulted in the recognition of biostratigraphical units and their correlation with the chronostratigraphical scale.The microfacies recognized in the pelagic part of the succession include: the “filament” (Bositra) microfacies (Bathonian), the planktonic foraminifer microfacies (Oxfordian), the Saccocoma microfacies (Kimmeridgian to Upper Tithonian), and the calpionellid microfacies (Upper Tithonian–Berriasian). The volcanogenic rocks (lava flows and volcanic ash) appear in the topmost part of the succession (units 4 to 6) and this volcanic event is very precisely located in the Elliptica-Simplex chrons of the Middle and Late Berriasian.
EN
Early Cretaceous calpionellid samples were collected at the ammonoid-bearing Hochkogellocality in the southern most part of the Reichraming Nappe (Ebenforst Syncline, Northern Calcareous Alps). The microfossil fauna sampled from limestone parts of the Rossfeld Formation indicates an early Valanginian age. The standard Calpionellites Zone (with darderi and major subzones) coincides with the early Valanginian ammonoid zones of Busnardoites campylotoxus and Tirnovella pertransiens. The deposition of the limestones in this area occurred in an unstable environment disturbed by gravitational transport which accounts for the different sedimen tary components and accompanying fossils in the accumulated layers, transported from a source area situated to the south.
EN
The Veliky Kamenets quarry is an essential locality in stratigraphical and palaeomagnetical studies of the Jurassic and lowermost Cretaceous in eastern part of the Pieniny Klippen Belt. The carbonate succession, about 40 m thick, has been subdivided into 6 major lithostratigraphical units (A, B, C, D, DE and E) which biostratigraphy was based mainly on the ammonite fauna (Lewandowski et al. 2005); these deposits are overlain by about 13 m thick complex unit of carbonates (fossiliferous limestones and calcareous sedimentary breccias composed mainly of micritic limestone clasts) alternating with volcanogenic rocks (basalt lava flows, and pyroclastic deposits). The studied succession yielded abundant and well preserved microfossils which enable detailed stratigraphical interpretation of the deposits in question. The lowest part of the Upper Jurassic succession (upper part of unit B) is represented by lower Ammonitico Rosso limestones rich in planktonic foraminifers Globuligerina. The ammonites are indicative of the Plicatilis Zone and Transversarium/or Bifurcatus Zone of Middle, and possibly lowermost Upper Oxfordian, whereas calcareous dinoflagellates found at the top of the unit indicate the Parvula Zone of the Upper Oxfordian. The overlying cherty limestones (unit C) yielded the Kimmeridgian ammonites found in their uppermost part; the deposits of the unit are rich in rests of planktonic crinoids Saccocoma. The younger ammonite assemblage coming from the lower part of the upper Ammonitico Rosso unit (unit D) is indicative of the Acanthicum Zone of the Upper Kimmeridgian. These deposits are characterized by Saccocoma-Globochaete microfacies, and yielded calcareous dinocysts indicative of the Moluccana Zone of the Kimmeridgian. The Kimmeridgian/Tithonian boundary runs in the middle of the discussed Ammonitico Rosso unit (unit D) as evidenced by occurrence of calcareous dinocyst Carpistomiosphaera tithonica. The upper part of the unit yielded calpionellids and calcareous dinocysts indicative of the Praetintinnopsella Zone located at the turn of the Middle and Upper Tithonian. The topmost part of the unit, as well as the lower part of overlying partly nodular micritic limestones (unit E/D) yielded already calpionellids and calcareous dinocysts indicative of the Crassicolaria Zone of the Upper Tithonian. The deposits are dominated by the Crassicolaria-Globochaete microfacies. The Jurassic/Cretacous boundary runs in the middle of the partly nodular micritic limestone unit (D/E). Here appears assemblage dominated by spherical forms of Calpionella alpina indicating the lowermost part of the Calpionella Zone of the Lower Berriasian. This zone ranges up at least to the upper part of massive micritic limestones (unit E) where the calpionellids of the Ferasini Subzone have been recognized. The microfacies of the Globochaete-Calpionella type, locally enriched in radiolarians prevail. The carbonates of the topmost part of the succession covering the basalt lava flows, as well as limestones alternating with pyroclastic layers yielded calpionellids of the Calpionellopsis Zone of the Upper Berriasian indicating both the Simplex Subzone, and the Oblonga Subzone. The breccias contain i.a. the clasts of the Upper Tithonian micritic limestones with calpionellids of the Crassicolaria Zone and of volcanic rocks. The carbonates correspond to the ?ysa Limestone Fm., including the Walentowa Breccia Member of this formation (see Birkenmajer 1977).
EN
The Rogoża Coquina Member (Pieniny Klippen Belt, Carpathians, Poland) develped as red micritic ammonite coquinas covers the stratigraphical interval from Kimmeridgian to Upper Tithonian as indicated by microfossils study (calcareous dinocysts and calpionellids) in the type-section of the unit, in the Rogoźnik Quarry. These deposits are overlain by white micritic limestones attributed to the Sobótka Limestone Member of Lower to Middle Berriasian.
PL
Czerwone muszlowce amonitowe odsłonięte w nieczynnym kamieniołomie w Rogoźniku stanowią wzorzec litostratygraficzny dla ogniwa muszlowców z Rogoży (dawniejsza nazwa "czerwone muszlowce rogoźnickie" - Birkenmajer 1962, 1963, 1977). Pozycja chronostratygraficzna tych utworów i ich związek ze słynnymi muszlowcami ogniwa muszlowców z Rogoźnika (dawna nazwa "białe muszlowce rogoźnickie" - Birkenmajer 1962, 1963, 1977) pozostawały przez dłuższy czas nie w pełni wyjaśnione. Pierwotnie (Birkenmajer 1977), sądzono, że ogniwo muszlowców z Rogoży jest starsze od ogniwa muszlowców z Rogoźnika; później (Kutek & Wierzbowski 1986), wyrażono opinię, że ogniwa te są równowiekowe - czerwone mikrytowe muszlowce z Rogoży zastąpione są obocznie przez muszlowce z Rogoźnika o silnie zrekrystalizowanym matryksie przekształconym w dużym stopniu w grubokrystaliczny kalcyt. Przeprowadzone obecnie szczegółowe badania płytek cienkich z prób zebranych w profilu muszlowców z Rogoży w kamieniołomie w Rogoźniku (fig. 1 i 2, pl. 1-3) pozwoliły na pełne przedstawienie charakterystyki mikrofacjalnej i określenie pozycji chronostratygraficznej tych utworów w oparciu o cysty wapiennych Dinoflagellata oraz kalpionelle. Widoczne w profilu muszlowce mają miąższość około 11 metrów (spąg ogniwa muszlowców z Rogoży jest tu nieodsłonięty) i wykształcone są w niższej części jako czerwone wapienie typu wackestone i packstone o mikrofacji sakkokomowo-globochetowej, a w części wyższej - jako czerwonawe i różowe wapienie typu wackestone o mikrofacji kalpionellowo-radiolariowej. Pozycja chronostratygraficzna niższej części muszlowców zawiera się w przedziale od kimerydu i dolnego tytonu (poziomy dinoflagellatowe: Parvula, Moluccana, Borzai oraz Pulla-Tithonica w klasyfikacji Rehakowej 2000) do środkowego tytonu/najniższego górnego tytonu (poziomy kalpionellowe: Chitinoidella oraz Praetintinnopsella w klasyfikacji Rehakowej i Michalika 1997). Datowania te pokazują, że omawiane utwory obejmują przedział stratygraficzny, odpowiadajacy rozwiniętym w klasycznej postaci muszlowcom z Rogoźnika w profilu skałek Rogoży (por. Kutek i Wierzbowski 1986). Wyższa część ogniwa muszlowców z Rogoży w badanym profilu zawiera liczne kalpionelle wskazujące na górnotytoński poziom Crassicolaria i jego wszystkie trzy podpoziomy: Remanei, Brevis i Colomi (por. Reháková i Michalik 1997). Utwory bezpośrednio nadścielające muszlowce z Rogoży w profilu kamieniołomu w Rogoźniku reprezentowane są przez białe i biało-szare wapienie typu wackestone, a lokalnie też mudstone, wykształcone w mikrofacji radiolariowo-kalpionellowej lub kalpionellowej. Obecne tu zespoły kalpionelli wskazują na dolny i środkowy berias (poziom Calpionella), przy czym jak wydaje się, najniższa część tego poziomu, odpowiadająca podpoziomowi Alpina, jest tu nieobecna lub silnie zredukowana miąższościowo. Może to wskazywać na istnienie luki stratygraficznej pomiędzy ogniwem muszlowców z Rogoży, a omawianymi nadległymi wapieniami, które swoim charakterem litologicznym, a także swoją pozycją stratygraficzną, wyraźnie nawiązują do ogniwa wapienia z Sobótki w schemacie litostratygraficznym Birkenmajera (1977).
EN
The radiolarian and calpionellid microfacies are characteristic for the latest Tithonian–Early Berriasian limestones of the Guasasa Formation in the Sierra del Infierno, western Cuba. The limestones of the uppermost part of the El Americano Memberbelongto the Late Tithonian Crassicollaria intermedia Subzone, Crassicollaria Standard Zone, and to the basal part of the Early Berriasian Calpionella alpina Subzone. The lower part of the Tumbadero Member is assigned to the C. alpina Subzone of the Calpionella Standard Zone. A heteromorph ammonite assemblage (Protancyloceras-Vinalesites) crosses the Crassicollaria/Calpionella Zones boundary. The studied limestones belong to three nannoconid assemblages of latest Tithonian–Early Berriasian age assigned to Nannoconus wintereri Subzone, N. steinmannii minor Subzone and N. steinmannii steinmannii Zone. Radiolarian taxa identified in thin sections are consistent with the lower part of D2 radiolarian zone from Western Tethys. The investigated deposits have been probably accumulated in the dysaerobic zone. At the Tithonian–Berriasian (J/K) boundary, dysaerobic to anaerobic conditions could be widespread in the deeper waters of the northwestern Proto-Caribbean basin.
PL
W niniejszej pracy zostały zbadane dwa profile obejmujące wapienie najwyższego tytonu i dolnego beriasu w Sierra del Infierno, na zachód od Vifiales w zachodniej części Kuby (Fig. 1A-C). Wapienie najwyższej części ogniwa El Americano formacji Guasasa (Tab. 1) należą do podpoziomu Crassicollaria intermedia poziomu standardowego Crassicollaria (górny tyton) i najniższej części podpoziomu Calpionella alpina (dolny berias) poziomu standardowego Calpionella (Fig. 2, 3). Dolna część ogniwa Tumbadero została zaliczona do podpoziomu C. alpina. W wapieniach najwyższej części ogniwa El Americano (Fig. 4A) i dolnej części ogniwa Tumbadero (Fig. 4B) charakterystyczne są mikrofacje kalpionellidowa (Fig. 5A) i radiolariowa (Fig. 6A). Pelmikrosparyty (Fig. 5B) i laminowane biomikryty (Fig. 6B) również są spotykane w dolnym beriasie. Kalpionellidy (Fig. 7A-I) są reprezentowane przez pojedyncze okazy do bardzo licznych zespołów (Tab. 2); zwykle są one słabo zachowane. Jest to już wcześniej opisana cecha kalpionellidów obecnych w wapieniach późnego tytonu i beriasu sukcesji Sierra de los Organos (Pop, 1976). Badane wapienie zawierają również nannokonidy (Fig. 8, 9A-H) zaliczone tutaj do podpoziomów Nannoconus wintereri i N. steinmannii minor oraz do poziomu N. steinmannii steinmannii (Tab. 3). Granica ogniw El Americano i Tumbadero znajduje się w obrębie podpoziomu N. steinmannii minor. Radiolarie oznaczone w płytkach cienkich (Fig. 10A-J, 11) odpowiadają dolnej części poziomu radio-lariowego D2 ustalonego w formacji Maiolica zachodniej Tetydy (Jud, 1994). Niektóre rodzaje (Ristola, Mirifusus) są często spotykane w badanych profilach. Obecność juwenilnych amonitów rozwiniętych: Protancyloceras gr. hondense (Imlay) (Fig. 12A), Protancyloceras sp. i Vinalesites sp. (Fig. 12B) została stwierdzona w niektórych płytkach cienkich wykonanych z wapieni (Tab. 4). Zespół tych amonitów przekracza granicę poziomów kalpionellidowych Crassicollaria i Calpionella (Tab. 5). Szare, ciemnoszare i czarne wapienie najwyższej części ogniwa El Americano i dolnej części ogniwa Tumbadero zostały osadzone prawdopodobnie w strefie dysaerobowej, w której fauna bentosowa była bardzo nieliczna (Fig. 12C). Ławice wapieni zazwyczaj nie zawierają struktur wskazujących na intensywną działalność organizmów ryjących w osadzie. W pobliżu granicy tytonu i beriasu (J/K), warunki dysaerobowe (lub nawet anaerobowe) mogły być rozprzestrzenione w głębszych wodach północno-zachodniej części basenu Protokaraibskiego. Takie warunki wskazująna raczej słabą cyrkulację w głębszych wodach tego dosyć wąskiego w tym czasie basenu.
EN
The studied sections of the Tithonian-Hauterivian deposits of the Branisko Succession in the Polish part of the Pieniny Klippen Belt (Figs 1-7) yielded micro-, nanno- and macrofossils, which allowed to elaborate more detailed stratigraphy of these strata, especially in the lowermost Cretaceous interval of the Pieniny Limestone Formation. The calpionellids, radiolarians and other microfossils (mainly calcareous dinoflagellate cysts) were studied in thin sections, whereas the calcareous nannofossils were analysed under SEM. The Berriasian-Hauterivian ammonites are described and illustrated. In the Kapuśnica I section, the Upszar Limestone Member of the Czorsztyn Limestone Formation seems to be exclusively of Tithonian age. At present, the Upper Tithonian deposits of the Crassi- collaria Standard Zone are missing in the studied section. In the Łysonka Klippe, the Lower Berriasian limestones are subdivided on the basis of the Nannoconus assemblages. The ammonites of the Jacobi Zone occur in the limestones of the N. steinmannii steinmannii Zone. In the Kapuśnica I section, the sedimentation rate of the limestones assigned to the Elliptica Subzone was about 1.3 m/Ma. The Oblonga Subzone (sensu lato) coincides with the marly deposition episode in this section; the Łysonka Marl Bed is assigned to the lower interval of this subzone. However, the overall sedimentation rate during the Late Berriasian Oblonga Subzone was low (about ~1.7 m/Ma). Presence of the ammonite Tirnovella otopeta Zone was documented in the Kapuśnica II and Łysonka sections. In the Kapuśnica II section, the minimum value of sedimentation rate of the radiolarian-calpionellid limestones assigned to the Lower Valanginian Calpionellites Zone is about 4.1 m/Ma. The Tintinno- psella Zone of the uppermost Lower Valanginian-Hauterivian is represented by a limestone succe- ssion about 51 m thick. In the Łysonka section, the Upper Valanginian limestones of this zone are probably older than those exposed in the Zaskale section. In the latter section, some ammonites are indicative for the Upper Valanginian Criosarasinella furcillata Zone. In the upper part of the Kapuśnica II section, the limestones of the Tintinnopsella Zone yielded Olcostephanus sp. and Neolissoceras desmoceratoides (Wiedmann) found 4.5 m below the top of this section. These ammonites indicate the Early Hauterivian age of the sparsely fossiliferous limestones. The Upper Hauterivian deposits may be represented in the topmost limestones of the Kapuśnica II section.
PL
Niektóre tylko zdarzenia tytonu-hoterywu, udokumentowane w sukcesji reglowej dolnej Tatr, można skorelować jednoznacznie ze zdarzeniami wyróżnionymi wcześniej na obszarze Karpat Zachodnich. W profilach tatrzańskich, turbidyty ogniwa z Krytej formacji margli z Kościeliskiej (fm.) dokładnie odpowiadają zdarzeniu orawickiemu dolnego walanżynu. W Tatrach Zachodnich została stwierdzona koincydencja walanżyńskiego zdarzenia izotopowego ?13C z wyraźnie niższą zawartością mikroplanktonu, a zwłaszcza radiolarii, w wapieniach osadzonych na przełomie dolnego i górnego walanżynu. Podobnie jak walanżyńskie zdarzenie izotopowe, ekspansja otwornic planktonicznych w górnym hoterywie (najwyższa część poziomu Tintinnopsella) miała zasięg ponadregionalny, daleko wykraczający poza obszar Zachodnich Karpat. W głębokowodnym basenie kriżniańskim korelacja zdarzeń biotycznych i innych tytonu-hoterywu z eustatycznymi zmianami poziomu morza, chociaż prawdopodobna, nie we wszystkich przypadkach może być uznana za w pełni udowodnioną.
EN
In the Tithonian-Hauterivian deposits of the Lower Subtatric succession of the Tatra Mountains (Western Carpathians), only a few events of biotic, sedimentary and isotopic character can be correlated with those recently proposed for the whole West Carpathian area. In the Western Tatra Mts, the turbidites of the Kryta Member (Kościeliska Marl Formation) correlate well with the Early Valanginian Oravice event. The Valanginian isotopic carbon event coincided with a minimum of microplankton content (especially radiolarians) in limestones deposited at the Lower/Upper Valanginian boundary. Expansion of planktonie foraminifers during the Late Hauterivian was another widespread event observed in the Tatra Mts, other areas of the Western Carpathians and outside these mountains. Correlation of the Tithonian-Hauterivian events with eustatic sea-level changes, although probable, has not been fully documented as for cerns some events recognised in the deep-water Kriźna basin.
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PL
W autochtonicznej serii wierchowej, w Tatrach Zachodnich, w rejonie Osobitej, występuje dolnokredowa brekcja składająca się z różnowiekowych okruchów wapiennych o różnym typie litologicznym, spojona spoiwem węglanowym. Na podstawie występujących kalpionellidów określono wiek sedymentacji poszczególnych typów litologicznych jako późnotytoński i wczesnoberiaski. Wiek brekcji określono jako późniejszy od wczesnego beriasu. Wyróżnione typy litologiczne wykazują podobieństwo do osadów węglanowych z wyższej części formacji wapieni z Raptawickiej Turni odsłaniającej się w polskiej części Tatr Zachodnich.
EN
The uppermost part of the Sobótka Limestone Member in the High-Tatric Succession is represented by Lower Cretaceous breccia. This breccia consists of limestone fragments of different lithology. The clasts within the breccia are cemented by calcium carbonate. On the base of the described calpionellid fauna, the sedimentation episode was identified as Late Thithonian and Early Berriasian. The breccia was formed later than the Early Berriasian. All the lithological types of clasts occurring in the breccia are similar to those of the upper part of Raptawicka Turnia Limestone Fm. located in the Polish part of Western Tatra Mts.
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