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1

Magnetostratigraphy of the Jurassic/Cretaceous boundary interval in the Western Tethys and its correlations with other regions: a review

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Grabowski J.

Volumina Jurassica

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2011

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tom Vol. 9, no. 1

105-128

EN

Magnetostratigraphy is an important method in regional and worldwide correlations across the Jurassic/Cretaceous boundary. The M-sequence of magnetic anomalies, embracing this boundary, provides an easily recognizable pattern which might be identified in biostratigraphically calibrated land sections. The polarity chrons between M21r and M16n are well correlated to calpionellid and calcareous nannofossil stratigraphy in the Tethyan Realm. This results in a very high precision of stratigraphic schemes of pelagic carbonates (ammonitico rosso and maiolica limestones), integrating the two groups of fossils with magnetostratigraphy. The main clusters of the reference sections are located in the Southern Alps and Apennines, but the database was recently enriched by sections from the Western Carpathians and Eastern Alps. Quite a few Jurassic/Cretaceous boundary sections with magnetostratigraphy are known in the Iberian Peninsula and south-eastern France but their importance relies on the integration of magnetostratigraphy also with the Tethyan ammonite zonation. Correlation of Boreal and Tethyan regions still remains a major problem. Just two sections with reliable correlation to the global polarity time scale are documented outside Tethys: a shallow marine to non-marine Tithonian–Berriasian–Valanginian sequence in southern England (Portland–Purbeck beds) and the marine clastic Upper Tithonian–Middle Berriasian (= Middle Volgian–lowermost Ryazanian) sequence at Nordvik Peninsula (Siberia). The Volgian/Ryazanian boundary at Nordvik seems to be located in the lower part of magnetochron M18n, while the most commonly accepted definitions of the Tethyan Jurassic/Cretaceous boundary are situated either within magnetochron M19n (A/B calpionellid zonal boundary, Durangites/Jacobi ammonite zonal boundary), or at the boundary of M19n/M18r (Jacobi/Grandis ammonite subzonal boundary).

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Further observations on the bio- and magnetostratigraphy of the J/K boundary interval in southern Ukraine

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Wimbledon W. A. P. , Svobodova A. , Bakhmutov V. , Poliachenko I. , Hlavatskyi D.

Geological Quarterly

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2022

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tom Vol. 66, No. 1

art. no. 11

EN

This is an account of finds of stratigraphically useful calcareous nannofossils and the magnetostratigraphy of the Jurassic-Cretaceous boundary interval of the eastern Crimean peninsula (southern Ukraine). We compare these new complementary results with those presented by our team in earlier publications. A missing interval in the Crimean sequence is filled, and the position of the Tithonian-Berriasian (J/K) boundary is confirmed.

3

Post-evaporitic carbonates of the Saudi Arabian Late Jurassic

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Hughes G. , Naji N. , Al-Khaled M. , Harland T. , Bacchus D.

Volumina Jurassica

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2006

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tom Vol. 4, no. 1

91-91

EN

The Hith Formation forms the latest lithostratigraphic unit of the Jurassic Shaqra Group, and was deposited during the Tithonian. The Formation outcrops in central Saudi Arabia, but has been studied in detail in subsurface eastern Saudi Arabia where the upper carbonate member hosts an important hydrocarbon reservoir called the Manifa reservoir. Chronostratigraphic control is absent, and the Tithonian age is based on stratigraphic position between the underlying Kimmeridgian Arab Formation, and the overlying Sulaiy Formation, of Berriasian age. The lower anhydrite-dominated member is un-named, and considered to represent subaqueous deposition representing the transgressive systems tract of the Manifa sequence. A transitional unit, consisting of interbedded anhydrites and carbonates, approximates with the maximum flooding zone, and the overlying carbonates are considered to represent the results of a prograding shallow marine succession related to the highstand systems tract. The carbonates of the Manifa reservoir consist of five parasequences, each of which represents a shoaling-upwards cycle that commences with a stromatolitic, microfaunally-barren unit that is followed by fine-grained grainstones with a monospecific but abundant ostracod biofacies. A succession of coarse pelloidal grainstones with rare Foraminifera, including Redmondoides lugeoni, Trocholina alpina and miliolids, then follows, that passes vertically into coarse ooid grainstones that form the uppermost part of each parasequence. The Hith Formation represents the culmination of a succession of hypersaline and euryhaline cycles that characterise the Late Jurassic of Saudi Arabia, and provides an insight to the palaeoenvironmental conditions that existed across the Arabian Plate at the end of the Jurassic.

4

Corals from the Tithonian carbonate complex in the Dąbrowa Tarnowska–Szczucin area (Polish Carpathian Foreland)

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Morycowa E.

Annales Societatis Geologorum Poloniae

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2012

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tom Vol. 82, No. 1

1–-38

EN

The studied corals have been collected from cores of boreholes located in the central part of the Polish Carpathian Foreland in the Dąbrowa Tarnowska–Szczucin area. The Jurassic complex in this area presents a continuous stratigraphic section from the Upper Callovian to Tithonian, locally passing to the Lower Cretaceous (Berriasian). Its thickness exceeds 1,100 m in this area. This complex is composed of marine, mainly shallow-water deposits. The corals occur within the upper part of the Upper Jurassic (Tithonian) deposits, almost entirely within the Swarzów Limestone Formation (= coral-algal limestone formation). This occurrence marks the northernmost extent of Tithonian shallow-water corals in Poland and one of the northernmost in Europe. 42 coral species (among them 14 in open nomenclature) were identified in deposits of this formation. They include two new species: Complexastrea magna and Complexastrea dabroviensis. All taxa, except one, belong to the order Scleractinia. The described assemblage displays a Late Jurassic character. The broader stratigraphic span is assigned to some species, which are quoted from the Middle Jurassic and some species lasted until the Early Cretaceous, Berriasian and/or Valanginian.

5

The base of the Tithonian Stage – historical review and state of the art

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Schweigert G. , Atropos F.

Volumina Jurassica

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2006

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tom Vol. 4, no. 1

213-214

EN

When introducing the Tithonian Stage in a preliminary way, Oppel in 1865 listed several localities, which, according to him, yielded typical faunas of this age. The original list of Oppel comprises 117 taxa, mostly ammonites. The main localities which proliferated these taxa are: Rogoenik, Radzichov (Polish Carpathians), Ignaziberg, Koniakow, Willamowice, TeĘin (Silesia), Stramberk (Moravia), Trento, Rovereto (Southern Alps), Ruhpolding (Eastern Alps), Solnhofen, Eichstatt, Neuburg a. d. Donau (Bavaria), Nusplingen (Swabia), Grenoble, Val d'Ormonds (Switzerland), Chambery (Savoie), Boulogne-sur-Mer (Normandy), and Portland (Dorset). However, no type locality was ever selected. One of the localities in Oppel's list, Nusplingen, is not a time equivalent of the Solnhofen Limestones in Franconia, as suggested by Oppel in disregard of the completely different ammonite faunas. In the original definition of the Tithonian no zonal subdivision was presented. The first ammonite zone of the Tithonian, the Hybonotum Zone, was informally proposed by Benecke (1866, "Schichten des Ammonites hybonotus and lithographicus"), who focussed on the correlation between the Tithonian in the Tethyan Late Jurassic - mainly the Ammonitico Rosso Superiore of the Southern Alps - and its supposed coeval deposits in SW Germany. This Hybonotum Zone was an assemblage range zone, which included the taxa from the Diphyakalk of the Southern Alps, intercalated between the beds containing Aspidoceras acanthicum and the Early Cretaceaous Biancone, thus being approximately synonymous with the Tithonian Stage of Oppel. Neumayr introduced the Beckeri Zone in 1873 by subdividing the Acanthicum Zone. An increase of provincialism in the Late Jurassic forced the establishment of several independent zonal schemes and stages. Today, the Tithonian Stage starting with the Hybonotum Zone is regarded as standard for chronostratigraphy in the Jurassic. More recently several attempts for a definition of the Kimmeridgian/Tithonian boundary, the base of the Hybonotum Zone, were made. Sections in SW Germany were studied in detail but it was not possible to find suitable sites for the proposal of a GSSP. The only published suggestion is from Contrada Fornazzo near Castellammare in W Sicily, but the flatter section is rather poor in respect of its ammonite faunas and hence of little correlation value, especially in contrast to sections in SE France (Canjuers, Mt. Crussol). The latter provide rich, well-preserved faunas with a succession of chronospecies of Hybonoticeras (in ascending order): Hybonoticeras kamicense (Schopen) - H. n. sp. - H. pseudohybonotum Vigh - H. n. sp. (=autharis sensu Berckhemer & Holder) - H. hybonotum (Oppel) - H. n. sp. They are accompanied by numerous perisphinctids, oppeliids and aspidoceratids. The final decision of a GSSP for the base of the Tithonian Stage is a formal convention, in which these valuable data should be taken into account, and we warn of a premature decision

6

Recent discoveries of Tithonian ammonites in the Štramberk Limestone (Kotouč Quarry, Outer Western Carpathians)

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Vašíček Z. , Skupien P.

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2014

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tom Vol. 84, No. 2

131--141

EN

Recent discoveries of ammonites in the Štramberk Limestone in the type area of their occurrence near the town of Štramberk supplement existing data on the Tithonian age of the limestones. Franconites cf. fascipartitus occurs in the lower part of the Lower Tithonian (Neochetoceras mucronatum Zone). Lemencia ciliata has a zonal character in the upper part of the Lower Tithonian. Richterella richteri is a subzonal species of the upper part of the Lower Tithonian in the Mediterranean and Submediterranean areas (Semiformiceras fallauxi Zone). All of the new discoveries are referable to the faunal associations of the Submediterranean bioprovince, and are in agreement with existing knowledge of it. Sexual dimorphism was seen in the genus Richterella, with the recognition of both macroconchs and microconchs in the type species of Richterella, i.e. R. richteri. The stratigraphic position of these recent ammonite discoveries in the Štramberk Limestone at the Kotouč Quarry does not support the stratigraphy of the limestones based on the distribution of calpionellids, as previously assumed by other authors. The recent collection of ammonites confirms that the Štramberk Limestone belongs to the lower Tithonian and lower Berriasian and also represents the lower Tithonian as a shallow-water facies.

7

The problem of establishing the Tithonian Stage in Western Siberia

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Podobina V. , Gabysheva E. , Tatyanin G.

Volumina Jurassica

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2006

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tom Vol. 4, no. 1

205-206

EN

In 1996 the Volgian Stage was withdrawn from the General Stratigraphic Scale and replaced with the Tithonian Stage by the Resolution of the Interdepartmental Stratigraphical Committee of Russia. However, this did not solve the problem of correlation between the Volgian and Tithonian stages. The problem of identifying and mapping the Tithonian Stage within the Boreal deposits becomes unresolved. On this basis the Volgian Stage was retained in the West Siberian Stratigraphical Scale as the terminal Jurassic Stage, owing to the impossibility of the application of the new standard directly to the Boreal sections. The difficulties in comparison between the Regional Scale and the Standard one arise not only for the ammonite zones, but also in correlating the West Siberian foraminiferal zones. Numerous boreholes penetrating Western Siberia and combined studies on core samples enable tracing the continuous sequence of the Volgian foraminiferal zones and beds. The foraminiferal sequence traced through the Nyarginskian type section in the southeast of Western Siberia may serve as an example. There, in the Upper Kimmeridgian – Lower Volgian deposits, the f-beds with the Pseudolamarkina sp. Assemblage were established. The Middle Volgian Spiroplectammina vicinalis-Dorothia tortuosa F-zone was divided into two subzones: the lower Spiroplectammina vicinalis-Saracenaria pravoslavlevi subzone and the upper Dorothia tortuosa subzone The Upper Volgian deposits enclose the Ammodiscus veteranus-Evolutinella volossatovi F-zone. At the Jurassic/Cretaceous boundary, the taxonomy of benthic Foraminifera is essentially different. The phylogenetic succession of numerous foraminiferal genera during the Volgian Age indicates the integrity of the Volgian Stage. A number of genera are characteristic only for the Volgian. Benthic Foraminifera forming the basis for establishing the Upper Jurassic assemblages, and the Volgian ones in particular, showed a wide distribution in the Late Jurassic marine basins of the Boreal belt: Northern Europe (Russia and Poland), Northeast Asia, Northern America (Northern and Northwest Canada, Northern Alaska), islands of the Arctic Region and shelves of northern seas. This wide distribution of the Volgian Foraminifera resulted from the Late Jurassic transgression. The Boreal and Tethyan foraminiferal assemblages differ essentially each other in their taxonomy, which result in significant difficulties in correlation between the Volgian and Tithonian deposits of Boreal and Tethyan belts, respectively. Besides, the distinctive feature of all provinces of the Boreal belt is the absence of planktonic foraminifers or their insignificant development. The direct correlation of the Volgian assemblages is possible only within the Boreal belt, basing on the taxonomical analysis of foraminiferal assemblages and the presence of the species of correlation value. The correlation of the Volgian-Tithonian deposits of the Boreal and Tethyan belts is feasible only at the level of Lower-Middle Volgian substages and the Tithonian. We suppose that at present it is impossible to find direct counterparts of the Upper Volgian Substage.

8

Sedimentological and micropalaeontological evidence to elucidate post-evaporitic carbonate palaeoenvironments of the Saudi Arabian latest Jurassic

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Hughes G. , Naji N.

Volumina Jurassica

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2008

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tom Vol. 6, no. 1

61-73

EN

The Hith Formation forms the youngest lithostratigraphic unit of the Jurassic Shaqra Group. It represents the culmination of a succession of hypersaline and euryhaline cycles that characterise the Late Jurassic of Saudi Arabia. The Formation is poorly exposed in central Saudi Arabia, but it has been studied in detail in subsurface eastern Saudi Arabia where the upper carbonate member hosts an important hydrocarbon reservoir called the Manifa Reservoir. Chronostratigraphic control is absent from the formation itself, and the Tithonian age is suggested for the Hith Formation based on its stratigraphic position between the underlying Arab Formation of Late Kimmeridgian age, and the overlying Sulaiy Formation, of Late Tithonian to Berriasian age. The Hith Formation needs redefining in the light of new lithological evidence, and a tripartite member scheme is suggested. This includes the lower anhydrite-dominated member here termed the “anhydrite” member, and considered to represent hypersaline subaqueous deposition within a restricted deep lagoon during the lowstand systems tract of the Manifa sequence. A “transitional“ member consists of interbedded anhydrites and carbonates and approximates with the transgressive zone. The overlying “carbonate” member represents the results of a prograding shallow, normal salinity marine succession related to the highstand systems tract. Interbedded carbonates within the evaporites are interpreted to represent superimposition of a higher frequency, possibly 4th order eustatic cyclicity. The “carbonate“ member hosts the Manifa Reservoir, and here proposed as the Manifa Member, consist of five parasequences, each of which represents a shoaling-upwards cycle with a succession of up to five repeated lithofacies and biofacies that commences with a stromatolitic, microfaunally-barren unit followed by fine-grained grainstones with a monospecific but abundant ostracod biofacies. A succession of coarse pelloidal grainstones with rare foraminifera, including Redmondoides lugeoni, Trocholina alpina with a variety of unidifferentiated valvulinids and miliolids then follows, that passes vertically into coarse ooid grainstones, with rare Redmondoides lugeoni, forming the uppermost part of each parasequence.

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Geotectonic evolution of the northern Tethyan margins in the Tithonian - sedimentological and biostratigraphical implications (Silesian Basin, Western Outer Carpathians)

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Neścieruk P. , Szydło A.

Volumina Jurassica

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2006

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tom Vol. 4, no. 1

62-62

EN

During the Late Jurassic the geotectonic reorganization of the extensive shelves on the southern margins of the Eastern European Platform was influenced by rifting in the Carpathian Basin which resulted in formation of the marginal Tethyan seas. The origin of the Silesian Basin was correlated with the first stage of the rifting (Golonka et al. 2000). The process of opening and deepening of the basin was completed at the end of the Jurassic when Neocimmerian movements were intensified and a regression on the Tethyan shelf had reached its peak. At that time, in the Western Outer Carpathians, breccias and olistostromes including mainly carbonate boulders, olistoliths and klippen were formed. In the Silesian Basin the supply of these redeposited materials culminated in Late Tithonian. The marly layers with olistolithes are known from the Cieszyn Silesian. The deposits occur at the top of nonflysch marly deposits, which belong to the oldest units of the Cieszyn Beds of the Polish and the Czech Outer Carpathians. In the Czech Carpathians these deposits correspond to the Ropice horizon (Eliáš & Eliášova 1984), which apart from the Štramberk reef and allodapic Cieszyn Limestones contains also calcareous sandstones and claystones including boulders of metamorphic and magmatic rocks (Eliáš & Eliášova 1984). These deposits yielded foraminifers which were also subject to removal and transportation. These include numerous calcareous (involutinids, placentulininds) and single agglutinated (lituolids) foraminifers which have been reported in rocks containing the olistolithes, but mainly in the overlying marls. Late Tithonian microfossils include also fragments of crinoids, bryozoans, and corals. These layers including calcareous material coming from destruction of the reef complex and carbonate platform can be assigned to a lithohorizon, deposited during geotectonic rebuilding of the northern Tethyan margins.

10

The Tithonian Chitinoidellidae and other microfossils from Owadów–Brzezinki quarry (central Poland)

75%

Pszczółkowski A.

Volumina Jurassica

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2016

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tom Vol. 14, no. 1

133--144

EN

Tithonian (= “Middle Volgian”) carbonate rocks are exposed in Owadów-Brzezinki quarry 19 km southeast of Tomaszów Ma-zowiecki, central Poland. In the upper part of the Sławno Limestone Member, chitinoidellids have been identified in thin sections from three samples, only. Therefore, the documented part of the Chitinoidella Zone in Owadów-Brzezinki quarry is about 0.3 m thick. The identified chitinoidellid taxa suggest that this assemblage represents the Upper Tithonian Boneti Subzone. The Chitinoidella Zone occurs at the top of Unit I and correlates with the uppermost interval of the Zarajskensis Horizon (Matyja, Wierzbowski, 2016). Other microfossils identified in the Chitinoidella Zone consist of Saccocoma sp. and benthic foraminifera of the genus Planularia. Calcareous dinoflagellate cysts (Cadosina semiradiata semiradiata Wanner and C. cf. semiradiata semiradiata Wanner) occur above the chitinoidellid assemblage, in the strata corresponding to the Gerassimovi Subzone of the Virgatus Zone (Matyja, Wierzbowski, 2016). Calcareous nannofossils are extremely rare in the thin sections studied; only one small specimen was seen, identified as Rhombolithion minutum (Rood et al., 1971) Young et Bown 2014. In contrast, microbial filaments are frequently observed in the studied thin sections. Their shape and pattern are reminiscent of some recent Cyanobacteria of the order Nostocales, however the Tithonian microbial filaments are much thinner.

11

Late Jurassic facies succession of the Kleszczów Graben area (southern border of the Łódź Depression, peri-Tethyan shelf, central Poland)

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Olchowy P. , Krajewski M. , Felisiak I.

Geological Quarterly

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2019

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tom Vol. 63, No. 4

657--682

EN

Numerous fully cored boreholes completed in the last years in central Poland (Kleszczów Graben area, southern border of the Łódź Depression) enabled the researchers to obtain new sedimentological data on the Oxfordian-Tithonian continuous sedimentary record in the Polish part of the northern Tethys shelf. Twenty-two facies were distinguished in the sedimentological succession. The facies represent the outer-, mid- and inner-ramp environments, including evaporitic episodes and palaeosols. The facies document that the Oxfordian-Lower Kimmeridgian (up to Hypselocyclum) carbonate ramp has evolved to the Upper Kimmeridgian-Tithonian carbonate-siliciclastic ramp. Among the Kimmeridgian deposits, numerous hardgrounds, tidal channel deposits and gravity flow sediments were identified. The Kleszczów Graben sedimentary succession is discussed along with the lithostratigraphical units known from the adjacent regions of southern and central Poland.

12

The Tithonian-earliest Berriasian Nannoconus zones in selected sections of the Pieniny Klippen Belt and the Western Tatra Mountains (southern Poland)

63%

Pszczółkowski A.

Studia Geologica Polonica

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2009

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tom Vol. 132

7-38

EN

In comparison with the Spanish sections, first appearance (FAD) of the Tithonian Nannoconus species is recorded earlier in the Pieniny Klippen Belt and the Western Tatra Mountains (Western Carpathians). The Early Tithonian Nannoconus compressus Zone correlates with the uppermost part of the "Pulla-Tithonica" Zone and the lower part of the Malmica Zone. The N. infans Zone corresponds to the upper part of the Malmica Zone and the lower part of the Chitinoidella Zone (Dobeni Subzone) including the lowermost interval of the Boneti Subzone. The N. wintereri Zone is equivalent to the uppermost part of the Chitinoidella Zone, entire Crassicollaria Zone, and the basal interval of the Berriasian Alpina Subzone. In the Kryta Valley section (Tatra Mts), the Infans/ Wintereri zonal boundary is located within the Boneti Subzone and is correlated with the lower part of the CM20n magnetozone. Specimens referred to Nannoconus sp. A occur in the studied sections; these specimens differ from the published descriptions of all previously established Tithonian species. In the Lower Tithonian limestones nannoconids are scarce being more numerous in the lower interval of the N. wintereri Zone. Increase in abundance of the genus Nannoconus correlates with the Mid- to Late Tithonian Nannofossil Calcification Event (NCE) reported from the Central Atlantic Ocean.

13

Magnetic susceptibility and gamma ray spectrometry in the Tré Maroua section (Tithonian/Berriasian, SE France) - terrigenous input and comparison with Tethyan record

63%

Grabowski J. , Frau C. , Schnabl P. , Svobodová A.

Volumina Jurassica

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2022

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tom Vol. 20

47--58

EN

Field magnetic susceptibility (MS) and gamma ray spectrometry (GRS) measurements were performed in the Jurassic/Cretaceous boundary interval in the Tré Maroua section (SE France). The 24 m thick section covers the interval from the upper Tithonian magnetozone M20n (Chitinoidella Zone) to the lower Berriasian M17r magnetozone (Calpionella elliptica Subzone). The micritic limestones reveal a very low content of terrigenous impurities (0.0-0.2% K and 0.2-2.0 ppm Th) and low MS values (-5 to 15 × 10-6 SI). Despite low intensity of both MS and GRS signal, a consistent trend of terrigenous input is observed: decreasing values in the upper Tithonian and increasing tendency in the upper part of the lower Berriasian. The long-term trends are quite similar to those documented in some Western Tethyan sections and the Polish Basin, indicating that variations of terrigenous input might be controlled by large-scale palaeoclimatic variations and relative sea-level changes. Decrease of Conusphaera and increase of Nannoconus frequencies fall in the lower part of M19n2n in the uppermost Tithonian. These events correlate with large decrease of terrigenous input and widespread oligotrophication in the Western Tethyan domain.

14

Górnojurajsko–?dolnokredowy kompleks węglanowy w rejonie Dąbrowy Tarnowskiej–Szczucina (Przedgórze Karpat)

63%

Morycowa E. , Moryc W.

Biuletyn Państwowego Instytutu Geologicznego

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2011

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tom nr 447

25--47

PL

Górnojurajskie utwory formacji wapieni koralowcowo-glonowych ze Swarzowa, występujące w środkowej części przedgórza Karpat, w rejonie Dąbrowy Tarnowskiej–Szczucina, zawierają liczne makroskamieniałości (m.in. skleraktinie, mszywioły, ramienionogi, algi) oraz niezbyt liczne mikroskamieniałości. Niektóre mikroskamieniałości są interesującymi wskaźnikami biostratygraficznymi. Występujące sporadycznie w wyższej części tej formacji kalpionellidy (Calpionella alpina, C. aff. alpina, Crassicolaria cf. brevis, Tintinopsella cf. carpatica) wskazują na późnotytoński wiek tych osadów (zona Crassicollaria). Być może, do tytonu należy prawie cała formacja ze Swarzowa i najniższa część leżącej wyżej formacji wapienno-dolomitycznej, muszlowcowej ze Smęgorzowa. Wyższa część formacji ze Smęgorzowa może należeć już do kredy dolnej, do beriasu.

EN

The Upper Jurassic coral-algal Swarzów Formation in the Dąbrowa Tarnowska–Szczucin area, occuring in the middle part of the Carpathian Foreland Poland contains rich macrofossils (i.e. scleractinian corals, bryozoans, brachiopods, algae) and generally sparse assemblages of microfossils. Some of the latter are interesting as a biostratigraphical tool. Thus, the presence of rare calpionellids (Calpionella alpina, C. aff. alpina, Crassicolaria cf. brevis, Tintinopsella cf. carpatica) argues for Late Tithonian age (standard Crassicollaria zone) of the upper part of this formation. It is suggested that the Swarzów Limestone Formation almost entirely represents the Tithonian, which probably reaches the lowest part of the lithostratigraphic unit of the Smęgorzów Limestone-Dolomitic Coquina Formation. The upper part of this unit may belong to the Lower Cretaceous, to Berriasian.

15

Macroconch ammonites from the Štramberk Limestone deposited in the collections of the Czech Geological Survey (Tithonian, Outer Western Carpathians, Czech Republic)

63%

Vašíček Z. , Malek O.

Volumina Jurassica

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2019

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tom Vol. 17, no. 1

81--94

EN

11 specimens of large sized ammonites from the Štramberk Limestone deposited in the collections in Prague represent 6species. Two species belong to the superfamily Lytoceratoidea, the remaining ones to the superfamily Perisphinctoidea. The perisphinctid specimens belong to the Lower and the Upper Tithonian, and the lytoceratids probably correspond to the same stratigraphic level. Two species, namely Ernstbrunnia blaschkei and Djurjuriceras mediterraneum were not known from the Štramberk Limestone earlier.

16

Functional anatomy and mode of life of the latest Jurassic crinoid Saccocoma

63%

Brodacki M.

Acta Palaeontologica Polonica

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2006

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tom 51

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nr 2

EN

Loose elements of the roveacrinid Saccocoma from the Tithonian red Rogoża Coquina, Rogoźnik, Pieniny Klippen Belt, Poland, are used to test the contradictory opinions on the mode of life of Saccocoma. The investigated elements belong to three morphological groups, which represent at least two separate species: S. tenella, S. vernioryi, and a third form, whose brachials resemble those of S. vernioryi but are equipped with wings of different shape. The geometry of brachials’ articular surfaces reveals that the arms of Saccocoma were relatively inflexible in their proximal part and left the cup at an angle of no more than 45, then spread gradually to the sides. There is no evidence that the wings were permanently oriented in either horizontal or vertical position, as proposed by two different benthic life−style hypotheses. The first secundibrachial was probably more similar to the first primibrachial than to the third secundibrachial, in contrast to the traditional assumption. The winged parts of the arms were too close to the cup and presumably too stiff to propel the animal in the water efficiently. Swimming was probably achieved by movements of the distal, finely branched parts of the arms. The nonhorizontal attitude of the winged parts of the arms is also not entirely consistent with the assumption that they functioned as a parachute. Moreover, the wings added some weight and thus increased the energy costs associated with swimming. The hydrodynamic benefits balancing these extra costs are not entirely clear, but it seems probable that the wings reduced the sinking rate of the animal not by increasing the pressure drag, as suggested by the parachute−analogy, but by increasing the surface drag (friction drag), which also harmonize with the presence of spines, reticulate sculpture and conspicuous vacuolar ornamentation in some species of Saccocoma.

17

Górny tyton i berias w płaszczowinie reglowej dolnej Tatr Zachodnich w świetle danych lito-, bio- i magnetostratygraficznych

51%

Grabowski J. , Pszczółkowski A.

Przegląd Geologiczny

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2006

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tom Vol. 54, nr 10

870-877

EN

Detailed magnetostratigraphic investigations of the Tithonian–Berriasian strata, integrated with litho- and biostratigraphic observations were carried out within the Bobrowiec Unit of the Lower Sub-Tatric (Krina) Nappe in theWestern Tatra Mts. Amodification of the existing lithostratigraphic scheme is proposed, splitting the Pieniny Limestone Formation (sensu Lefeld et al. 1985) into two formations, accordingly with lithostratigraphic subdivisions of the coeval deposits in some other parts of the Krina Nappe in Slovakia: the Jasenina Formation (includes Pośrednie Member sensu Pszczółkowski 1996, in its uppermost part) and the Osnica Formation (Osnica Member sensu Pszczółkowski 1996). The Jurassic/Cretaceous boundary, as defined by calpionellids, falls within the lowermost part of the Osnica Fm. Magnetozones from CM20r (Lower/Upper Tithonian boundary) up to CM16n (Upper Berriasian) were identified. Jurassic/Cretaceous boundary is situated within the CM19n magnetozone, below the short reversed Brodno subzone. Magnetostratigraphic correlation of four sections revealed existence of some “gaps” which are interpreted as tectonic reductions, which have to be considered while calculating the sedimentation rate which, however, might be roughly estimated. Sedimentation was relatively slow within the Jasenina Formation (5–7 m/My), but accelerated within the Osnica Fm (mean value: 10–15 m/My) and in the investigated lower part of the Kościeliska Marl Fm (20–30 m/My). Presence of hematite correlates with low sedimentation rate.

18

New finds of well-preserved Tithonian (Late Jurassic) fossils from Owadów–Brzezinki Quarry, Central Poland: a review and perspectives

51%

Błażejowski B. , Gieszcz P. , Tyborowski D.

Volumina Jurassica

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2016

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tom Vol. 14, no. 1

123--132

EN

Here we briefly report the discovery of new, exceptionally well-preserved Late Jurassic (Tithonian) fossils from Owadow- Brzezinki quarry - one of the most important palaeontological sites in Poland. These finds which comprise organisms living originally in different environments indicate that the Owadow-Brzezinki site represents a link - most probably in a form of open marine passages - betweeen distinct palaeobiogeographical provinces. This creates an unprecedented opportunity for better recognition of the regional palaeobiogeography of adjacent European areas during the Late Jurassic.

19

Diversity of chondrostean fish Coccolepis from the Late Jurassic Solnhofen Archipelago, Southern Germany

51%

Lopez-Arbarello A. , Ebert M.

Acta Palaeontologica Polonica

|

2021

|

tom 66

|

nr 4

20

Additional Tithonian and Berriasian ammonites from the Vaca Muerta Formation in Pampa Tril, Neuquén Basin, Argentina

51%

Parent H. , Schweigert G. , Scherzinger A. , Garrido A. C.

Volumina Jurassica

|

2017

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tom Vol. 15, no 1

139--154

EN

The ammonite fauna of the Tithonian–Berriasian of the Vaca Muerta Formation in Pampa Tril has been recently described in detail. New important specimens and additional information are presented in this paper. The phyletic evolution of Choicensisphinctes, passing from C. platyconus to C. erinoides is confirmed, as well as the sexual dimorphic correspondence of this latter with C. mendozanus. A microconch of the genus Krantziceras is described for the first time. New specimens of Substeueroceras koeneni identical to the paralec¬totype, along with material already described from the koeneni Hz. (Koeneni Zone), point to the fixation of this horizon as the type horizon of the species. New specimens of Subthurmannia boissieri from the Damesi Zone match clearly the range of variation of this species in Spain, thus providing an element for time-correlation with the Tethyan standard scale. Additional material from the internispinosum alpha Hz. confirms the origin of W. internispinosum from C. proximus by the inception of an evolutionary innovation in the juvenile ontogeny.