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1

Guettardiscyphia zitti sp. n. - a remarkable hexactinellid sponge from the Lower Turonian of the Bohemian Cretaceous Basin

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Vodrážka R.

Geological Quarterly

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2017

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tom Vol. 61, No. 3

632--640

EN

This paper describes a new hexactinosidan hexactinellid Guettardiscyphia zitti sp. n. on the basis of a detailed study of 279 specimens from 12 localities in the southern part of the Bohemian Cretaceous Basin. All the studied material comes from the basal Bílá Hora Formation (Lower Turonian). The geology and palaeontology of the sponge-bearing strata at studied locations exhibit identical palaeoenvironmental settings: 1 - transgressive character of sediments with low sedimentation rates, 2 - presence of submarine swells formed by crystalline basement, 3 - hemipelagic sedimentation below the storm-wave base, and 4 - the presence of proliferating diverse sponge faunas with subordinate accompanying macrofaunal remains.

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Upper Cretaceous of the Barranca (Navarra, northern Spain); integrated litho-, bio- and even stratigraphy. 1, Cenomanian through Santonian

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Kuchler T.

Acta Geologica Polonica

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1998

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tom Vol. 48, no. 2

157-236

EN

Fossiliferous Upper Cenomanian to Lower Maastrichtian strata in Navarra, northern Spain, particularly in the eastern Barranca, were investigated in terms of litostratigraphy, macrofossil biostratigraphy and event stratigraphy. Extensive bed-by bed-collections of ammonites, inoceramids, and echinoids allow the establishment of combined standard zonal schemes of inter-regional significance. Data on geochronological boundaries, macrofossil distribution, the succession of events and the inter-relations between bioevents, eustato-events and tectonic movements in northern Spain are presented. The Upper Cenomanian - Turonian successions of the Barranca sections (Arardi, Izurdiaga, Satrustegui) and of the Estella area (Ganuza, Ollogoyen), differ considerably in both lithofacies and thickness and periodically, in faunal composition, as a result of their palaeogeographical positions within an stable outer shelf and an unstable mit-shelf, respectively. The Ganuza/Ollogoyen standard section is revised. In the context of the established event stratigraphical scheme, discrepancies in previously applied ammonite zonation are pointed out and discussed in terms of their regional relevance. The expanded and relatively complete Turonian of the Estella area is subdivided into an unnamed interval devoid of ammonites (Upper Cenomanian Metoicoceras geslinianum Zone to the mid-Lower Turonian), six ammonite zones and an inoceramid/ammonite assemblage zone. The upper Lower Turonian Kamerunoceras ganuzai/Mammites nodosoides Zone is succeeded by the Middle Turonian zones of K. turoniense, Romaniceras kallesi, R. ornatissimum and R. deverianum; and the Upper Turonian Subprionocyclus neptuni and Cremnoceramus waltersdorfensis/ Prionocyclus germari zones. The Lower Turonian zonal scheme given by WIEDMANN (1979a) for the Estella area is shown to be impracticable, and neither Lower Turonian Choffaticeras quaasi Zone sensu SANTAMARIA (1992) nor a Watinoceras coloradoense Zone sensu LAMOLDA & al. (1989) can be recognized. On the other hand, the refined French Middle Turonian ammonite zonation of AMEDRO & al. (1982) is readily applicable, while the application of a Collignoniceras woolgari Zone is hardly possible. The base of the Middle Turonian has been placed at the FAD of K. turoniense, at a level stratigraphically lower (upper Lower Turonian) than the one recently accepted. C. woollgari is rare and appears no lower than the ornatissimum Zone. The base of the Upper Turonian is placed at the FAD of Subprionocyclus neptuni. Romaniceras deverianum appears considerably lower than the former, but has its main occurrence in the neptuni Zone, ranging up to overlap with Prionocyclus germari. The Barranca succession is condensed and includes hiati from the Upper Cenomanian Neocardioceras juddii Zone to the upper ganuzai/ nodosoides Zone; between the Middle Turonian kallesi and ornatissimum zones; and in the lower Upper Turonian neptuni Zone. Twelve bio-events that are significant for regional and inter-regional correlations are differentiated and dated: the Mytiloides kossmati, ganuzai, reveliereanus, turoniense/hercynicus, kallesi/ornatissimum, Scaphites geinitzii, Subprionocyclus I, Micraster ex gr. normanniaecortestudinarium, Subprionocyclus II events. Most of these events are time-equivalents of events already recognised by ERNST & al. (1983) in Germany. The biostratigraphic framework permits a dating and correlation of the major tectono-sedimentary and eustato-events, namely the Cenomanian-Turonian Boundary Event (CTBE), the Middle Turonian Event (MTE) and Lower Upper Turonian Event (LUTE). The calcareous Coniacian - Santonian succession of the eastern Barranca (Izurdiaga, Ecay and Zuazu sections), is divided into Lower Izurdiaga, Zuazu and Upper Izurdiaga formations, and into numerous component members. The succession is rich in echinoids, and is biostratigraphically important because of the cooccurrence of inoceramids and ammonites. The Coniacian ammonite assemblages show affinities to those of the French type region and to the largely endemic ones of the Spanish standard sections in Burgos. The data obtained permit a confident correlation of the biostratigraphic frameworks of these two areas for the first time. In contrast to the widespread basal Coniacian hiatus, the Barranca succession at this level is locally relatively complete. The lower Coniacian Cremnoceramus rotundatus, Forresteria petrocoriensis and Peroniceras subtricarinatum zones, the Middle Coniacian Gauthiericeras margae Zone and the lower Upper Coniacian Protexanites bourgeoisi Zone are recognized. In marginal sections, the bourgeoisi Zone is followed by an hiatus which comprises the late Upper Coniacian Magadiceramus subquadratus and the Lower Santonian Cladoceramus undulatoplicatus inoceramid zones recognized in the continuous section of the western Barranca. By means of ammonites, the Santonian at Olazagutia is divided into an unnamed interval devoid of ammonites; the middle Coniacian Texanites quiquenodosus and the Upper Santonian Jouaniceras hispanicum/Scalarites cingulatum Zone. This scheme has affinities with the zonation applied by KENNEDY & al. (1995) in the Corbieres, France. In addition to a sequence of regionally important events and marker-beds, some events, namely the Didymotis II, Micraster ex gr. cortestudinarium andCladoceramus undulatoplicatus events, are of inter-basinal importance.

3

Inoceramid bivalves at the Turonian/Coniacian boundary: biostratigraphy, events and diversity trend

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Walaszczyk I.

Acta Geologica Polonica

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2000

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tom Vol. 50, no. 4

421-430

EN

The Turonian/Coniacian boundary marks one of the main turnover levels in the Late Cretaceous history of the inoceramid bivalves. The change from the Mytiloides-dominated Late Turonian fauna to the Cremnoceramus-dominated Early Coniacian fauna was a dramatic experience for the group, with a series of successive assemblages interrupted by their almost total elimination, and with intervening short-term expansions of the bivalve Didymotis. The taxonomic diversity dropped to a few species per interval calculated and marks the lowest level in their Late Cretaceous history, comparable to the trough around the Cenomanian/Turonian boundary. The whole change must have taken no longer than a quarter of a milion years and its duration could have been as short as some tens of thousand years

4

Forresteria (Harleites) petrocoriensis (Coquand, 1859) from the Upper Turonian Mytiloides scupini Zone of Słupia Nadbrzeżna, Poland

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Kennedy W. J. , Walaszczyk I.

Acta Geologica Polonica

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2004

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tom Vol. 54, no. 1

55--59

EN

Forresteria (Harleites) petrocoriensis (Coquand, 1859) the classic ammonite marker for the base of the Coniacian stage in the Aquitaine Basin, France, is recorded from the Upper Turonian Mytiloides scupini Zone of Słupia Nadbrzeżna, Poland. The position of the upper and lower limits of the petrocoriensis Zone in terms of the standard inoceramid zonation across the Turonian-Coniacian boundary interval remains uncertain, and the proposed base of the Coniacian - the first occurrence of Cremnoceras deformis erectus (Meek, 1877) - lies in the lower part of the range of F. (H.) petrocoriensis. The inoceramid-defined base of the Coniacian cannot be recognised in the environs of Cognac, the type locality of the stage.

5

Uppermost Cenomanian ammonites from Eure, Haute-Normandie, northwest France

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Kennedy W. , Juignet P. , Girard J.

Acta Geologica Polonica

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2003

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tom Vol. 53, nr 1

1-18

EN

Temporary exposures of chalks spanning the Cenomanian-Turonian boundary to the east of Brionne, Eure, Haute-Normandie, France, yielded well-preserved ammonite faunas. The Metoicoceras geslinianum Zone assemblage is: Pseudocalycoceras angolaense (SPATH, 1931), Sumitomoceras cautisalbae (WRIGHT & KENNEDY, 1981), Calycoceras (Calycoceras) sp.juv., Eucalycoceras pentagonum (Jukes-Browne, 1896), Euomphaloceras septemseriatum (CRAGIN, 1893), Metoicoceras geslinianum (D'ORBIGNY, 1850), Hamites cimarronensis (KAUFFMAN & POWELL, 1977), Allocrioceras annulatum (SHUMARD, 1860), and Sciponoceras gracile (SHUMARD, 1860). The succeeding Neocardioceras juddii Zoneassemblage is: Thomelites serotinus (WRIGHT & KENNEDY, 1981), Neocardioceras juddii juddii (BARROIS & GUERNE, 1878), Neocardioceras juddii barroisi WRIGHT & KENNEDY, 1981, and Thomasites gongilensis (WOODS, 1911). Imprecisely localised are Pachydesmoceras sp., and Nigericeras aff. scotti COBAN, 1972. The majority of the species are new for northern France, and confirm the northwards extension of typicallyTethyan taxa (Thomasites, Nigericeras) into the Boreal region during the uppermost Cenomanian, and previously recognized in southern England, as well as the occurrence of cosmopolitan acanthoceratids well-known at this level in the United States (Pseudocalycoceras, Sumitomoceras).

6

Development of the Turonian Conulus Lagerstätte in the Wielkanoc quarry, Miechów Upland (South Poland)

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Olszewska-Nejbert D.

Annales Societatis Geologorum Poloniae

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2005

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tom Vol. 75, No 2

199-210

EN

Turonian sandy limestones and organodetrital limestones exposed in the Wielkanoc quarry, Miechów Upland, South Poland, lie on Oxfordian massive limestones, truncated with an abrasion surface. The bed situated ca. 2.5 m above the abrasion surface contains a parautochthonous and monotypic assemblage of the species Conulus subrotundus Mantell, 1822; thus the concentration can be referred to as the Conulus Lagerstätte. The microfacies analysis of the Conulus Lagerstätte indicates its development to have been determined by the existence of eco-events producing an increased population of Conulus subrotundus, and of sedimentological factors, that is waning of the loose sediment from the sea floor and erosion of the consolidated deposit rich in the earlier fossilised echinoids. The episodes of material accumulation, its consolidation and erosion in high-energy environment (action of bottom current) led to the increase of amount of echinoids as the intraclasts according to the model of lag sediment deposition.

PL

W kamieniołomie Wielkanoc (Wyżyna Miechowska), położonym na granicy Jury Polskiej i Niecki Miechowskiej (Fig. 1) odsłania się 10 m profil utworów oerodkowego i górnego turonu (Fig. 2), leżących na powierzchni abrazyjnej, oecinającej oksfordzkie wapienie skaliste. Utwory turońskie są wykształcone w dolnej części profilu w postaci wapieni piaszczysto-organodetrytycznych, organodetrytycznych lub piaszczystych, podczas gdy w górnej przeważają wapienie organodetrytyczne. Profil turonu kończy warstwa wapieni pelitowych z twardym dnem w stropie, nad którym leżą wapienie piaszczysto-glaukonitowe koniaku. Około 2,5 m nad powierzchnią abrazyjną znajduje się warstwa z wyraźnie większą frekwencją jeżowców (Fig. 3, 4), które stanowią paraautochtoniczny i monotypowy zespół gatunku Conulus subrotundus Mantell, 1822. Nagromadzenie jeżowców Conulus w jednej warstwie o znacznym rozprzestrzenieniu horyzontalnym pojawia się tylko raz w profilu turonu kamieniołomu Wielkanoc. Wykonane badania pokazały niejednorodną budowę warstwy z jeżowcami (Fig. 5–8). W obrębie tła skalnego występują intraklasty bez jeżowców, intraklasty, w których jeżowiec stanowi część intraklastu oraz jeżowce. Tło skalne jest packstonem inoceramowym (Fig. 5h, 7F), podobnie jak utwory leżące powyżej warstwy z jeżowcami (Fig. 5i, 8). Intraklasty nie zawierające jeżowców są zbudowane z wakstonu otwornicowo-kalcisferowego z dużą domieszką kwarcu oraz podrzędnie glaukonitu (Fig. 5c, 7B). Litologicznie odpowiadają osadom podoecielającym warstwę z jeżowcami (Fig. 5b, 7A). Intraklasty z jeżowcami charakteryzują się nieco bardziej złożoną budową. Skała otaczająca pancerz wykształcona jest jako wakston otwornicowo-kalcisferowy z dużą domieszką kwarcu oraz podrzędną glaukonitu (Fig. 5d, f; 7D, E). Ten sam rodzaj osadu wypełnia większość pancerzy jeżowców (Fig. 5e, 7E). Znacznie rzadziej spotykane są okazy, gdzie skała wypełniająca pancerz jeżowca w całości jest wakstonem otwornicowo- kalcisferowym bez domieszek kwarcowo-glaukonitowych (Fig. 5g, 7C), lub też wypełnienie pancerza ma charakter mieszany, tzn. część okazu wypełniona jest wakstonem otwornicowokalcisferowym z dodatkiem dużej ilości kwarcu i niewielkiej glaukonitu, zaś pozostała część, tej domieszki jest pozbawiona. Jeżowce nie będące częścią intraklastu wypełnione są wakstonem otwornicowo-kalcisferowym z dużą domieszką kwarcu i niewielk ą glaukonitu. Nieliczne okazy są wypełnione wakstonem otwornicowo-kalcisferowym, który nie zawiera domieszek kwarcowo- glaukonitowych. Obserwacje terenowe i analiza mikrofacjalna pozwoliły stwierdzić, iż do nagromadzenia jeżowców w analizowanej warstwie przyczyniły się czynniki ekologiczne i złożone czynniki sedymentologiczne. Do tych pierwszych należą zdarzenia ekologiczne, kiedy w środowisku stosunkowo niskoenergetycznym powstały optymalne warunki rozwoju Conulus subrotundus Mantell. Na czynniki sedymentologiczne złożyło się zarówno wymywanie świeżo złożonego luźnego osadu jak i erozja już skonsolidowanego osadu, bogatego w sfosylizowane wcześniej jeżowce (Fig. 9). Proces ten polegał na epizodach akumulacji materiału, jego konsolidacji i erozji w środowisku wysokoenergetycznym, co doprowadziło do powstania bruku rezydualnego (ang. lag deposit) składającego się ze sfosylizowanych wczeoeniej jeżowców. Opisane procesy zachodziły na podmorskim progu krakowskim, który funkcjonował jako jednostka paleogeograficzna od turonu po santon. Próg krakowski rozdzielał dwa głębsze baseny, położony na NE basen bruzdy duńsko-polskiej od basenu opolskiego na SW. W generalnie transgresywnych utworach późnej kredy, na progu krakowskim osadzały się utwory płytkowodne. Osadzanie tych utworów było przerywane częstymi epizodami erozji, gdyż próg krakowski, zanim został ostatecznie pogrążony w późnym santonie, podlegał okresowo silnej działalności falowania i prądów dennych.

7

Lithistid spicules in the sediments of the Turonian Variegated Shale in the Silesian Nappe, Polish Outer Carpathians

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Okoński S. , Górny Z. , Bąk M. , Bąk K.

Geology, Geophysics and Environment

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2014

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tom Vol. 40, no. 1

33--48

EN

Turbiditic silty and sandy intercalations in the Turonian Variegated Shale from the Silesian Nappe (Polish Outer Carpathians) contain numerous sponge spicules among siliciclastic fine-grained particles. The highest amount of spicule admixture is nearly 50%. In such layers, they create spiculitic sublitharenite microfacies. These sponge spicules contain forms belonging mostly to the Lithistida group (97% of morphotypes), with a small admixture of spicules from the Hexactinellidae group. Tetraclones with a high content of different types of triaenes dominate among desmas, what indicates the dominance of sponges from subfamily Tetracladina. The preservation state of spicules is generally poor. The Variegated Shale deposits that contain the sponge spicules were accumulated in a deep sea basin, below the calcium compensation depth. Most probably, the spicules were derived from loose material accumulated earlier in various parts of the basin slopes, from which they were exhumed and again redeposited by turbidity currents during the Turonian times.

8

Foraminifers and stable isotope record of the Dubivtsi chalk (upper Turonian, Western Ukraine): palaeoenvironmental implications

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Dubicka Z. , Peryt D.

Geological Quarterly

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2012

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tom Vol. 56, No 1

199-214

EN

A combined micropalaeontological and stable isotope study of the Dubivtsi chalk in the Western Ukraine indicates its middle late Turonian age. One long-term and clearly distinguishable positive excursion of the isotope curve (d1318

9

Barnasiówka Radiolarian Shale Formation - a new lithostratigraphic unit in the Upper Cenomanian-lowermost Turonian of the Polish Outer Carpathians (Silesian Series)

75%

Bąk K. , Bąk M. , Paul Z.

Annales Societatis Geologorum Poloniae

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2001

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tom Vol. 71, No 2

75-103

EN

A new lithostratigraphic unit - the Barnasiówka Radiolarian Shale Formation - is herein defined. It belongs to the Silesian Series of the Outer Carpathians. The formation consists of biosiliceous deposits rich in organic matter, laid down around the Cenomanian-Turonian boundary. The formation includes, from bottom to top: (1) a series of green to black, calcareous and siliceous shales, alternating with layers of chert, siliceous siltstone and sandstone (up to 10 m thick); (2) a series of green to black, argillaceous to siliceous shales, intercalated with tuffites, bentonites, and a ferromanganese layer (up to 9 cm thick) in its middle part (up to 3.2 m thick); (3) a series of green and red, siliceous siltstones and cherts with intercalations of non-calcareous green shales and benthonites (up to 2 m thick). The total thickness of the formation ranges from 0.5 m in the eastern part (reduced tectonically?) up to about 14-15 m in the middle and the western parts of the Silesian Nappe, due to the increase in the number and thickness of turbidite intercalations. The formation represents the Holocryptocanium barbui - Holocryptocanium tuberculatum through the Alie-vium superbum radiolarian zones and the Uvigerinammina praejankoi-Uvigerinammina jankoi foraminiferal zones, which correspond to the Upper Cenomanian through the lowermost Turonian. Microfacies and geochemical characteristics of the distinguished lithological types are presented in this paper, based on recent studies and published data. The described formation has been compared and correlated with deposits of similar age from other tectonic- facies units of the Outer Carpathians in Poland and Ukraine.

10

On some Late Turonian and Early Coniacian (Upper Cretaceous) heteromorph ammonites from Germany

75%

Wiese F.

Acta Geologica Polonica

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2000

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tom Vol. 50, no. 4

407-419

EN

Five heteromorph ammonite taxa belonging to the Nostoceratidae and the Diplomoceratidae are described from the Upper Turonian and Lower Coniacian of northern Germany and Saxony. The investigation serves the presentation of additional material of Hyphantoceras flexuosum, Neocrioceras paderbornense and Scalarites turoniense that are rarely documented in northern Germany and Saxony. Furthermore, one new species, Hyphantoceras ernsti sp. n., is introduced. One taxon is described in open nomenclature as nostoceratid gen. et sp. indet

11

Pueblo, Colorado, USA, candidate Global Boundary Stratotype Section and Point for the base of the Turonian Stage of the Cretaceous and for the base of the Middle Turonian Substage, with a revision of the Inoceramidae (Bivalvia)

75%

Kennedy W. , Walaszczyk I. , Cobban W.

Acta Geologica Polonica

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2000

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tom Vol. 50, no. 3

295-334

EN

An updated account of the candidate Global Boundary Stratotype Section and Point for the base of the Turonian Stage and the base of the Middle Turonian Substage in the Bridge Creek Member of the Greenhorn Limestone exposed in the Rock Creek Anticline west of Pueblo, Colorado is provided. Key ammonite distributions are revised and marker species illustrated. A taxonomic revision of the uppermost Cenomanian to lower Middle Turonian bivalve family Inoceramidae provides, for the first time, an adequately documented detailed zonation for the interval in the form of five successive partial range zones based on species of the genus Mytiloides. These are successive zones of M. hattini ELDER (uppermost Cenomanian), M. puebloensis n. sp., M. kossmati (HEINZ), M. mytiloides (MANTELL)(all Lower Turonian) and M. subhercynicus (SEITZ) (lower Middle Turonian). The base of the Turonian, defined by the first appearance of the ammonite Watinoceras devonense (WRIGHT & KENNEDY) at the base of bed 86 of the Bridge Creek Member corresponds to the first occurrence of Mytiloides puebloensis, and the base of the puebloensis Zone. The base of the Middle Turonian, defined bythe first occurrence of the ammonite Collignoniceras woollgari (MANTELL) in bed 120 of the Bridge Creek Members is just bellow the first occurrence of M. subhercynicus in bed 121, and the base of the sybhercynicus Zone.

12

Inoceramid/foraminiferal succession of the Turonian and Coniacian (Upper Cretaceous) of the Briansk region (Central European Russia)

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Walaszczyk I. , Kopaevich L. F. , Olferiev A. G.

Acta Geologica Polonica

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2004

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tom Vol. 54, no. 4

597-609

EN

An integrated inoceramid-foraminiferal zonation for the topmost Turonian and Lower Coniacian near Briansk, SW of Moscow is presented. The inoceramid fauna enables the application of the refined zonal scheme currently applied in central and western Europe. Three zones based on benthic foraminifera, the Gavelinella moniliformis, Ataxophragmium nautiloides and Stensioeina granulata granulata zones; and three zones based on planktonic foraminifera, the Whiteinella archaeocretacea, Marginotruncana pseudolinneiana and Marginotruncana renzi zones, are distinguished. The Turonian/ Coniacian boundary, defined by the first appearance of the inoceramid Cremnoceramus deformis erectus (MEEK, 1877), falls within the basal part of the Stensioeina granulata granulata Zone and the basal part of Marginotruncana renzi Zone.In foraminiferal terms the Turonian/Coniacian boundary interval is marked additionally by a sudden, short-lived increase in the plankton/benthos ratio, caused primarily by more abundant shallow-water morphotypes.

13

Coilopoceras inflatum Cobban and Hook, 1980, a United States Western Interior ammonite from the Upper Turonian of the southern Corbières, Aude, France

63%

Melchior P. , Bilotte M. , Kennedy W. J.

Acta Geologica Polonica

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2017

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tom Vol. 67, no. 1

121--134

EN

A newly discovered ammonite faunule from the Padern region of the southern Corbières in southern France includes representatives of typical northwest European Upper Turonian species Subprionocyclus cf. neptuni (Geinitz, 1850) and Lewesiceras cf. woodi Wright 1979, tethyan/ northwestern Pacific species Phyllopachyceras cf. ezoense (Yokoyama, 1890), Anagaudryceras involvulum (Stoliczka, 1865) and, Desmoceras (Pseudouhligella) sp., together with Coilopoceras inflatum Cobban and Hook, 1980, a species previously known only from New Mexico in the United States, where it is regarded as Middle Turonian. The faunule occurs above one with Romaniceras (R.) mexicanum Jones, 1938 and Coilopoceras springeri Hyatt, 1903, also originally described from New Mexico and northern Mexico, and recently described from the Uchaux massif in Vaucluse in southern France. The records suggest that the base of the Upper Turonian may be drawn at different, higher level in the United States Western Interior than in Europe. The coming together of these mixed faunal elements may be a result of high sea levels, and changing oceanic circulation patterns.

14

Turonian ammonite faunas from the southern Corbières, Aude, France

63%

Kennedy W. J. , Bilotte M. , Melchior P.

Acta Geologica Polonica

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2015

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tom Vol. 65, no. 4

437--494

EN

The Turonian successions of the southern Corbières comprise three transgressive-regressive cycles in which ammonites occur in three intervals. The lowest comes from the glauconitic basal transgressive unit of the first cycle, and comprises 21 species, including Kamerunoceras douvillei (Pervinquière, 1907), Kamerunoceras turoniense (d’Orbigny, 1850), Spathites (Jeanrogericeras) revelerianus (Courtiller, 1860), Spathites (Jeanrogericeras) combesi (d’Orbigny, 1856), Mammites nodosoides (Schlüter, 1871), Mammites powelli Kennedy, Wright and Hancock, 1987, Fagesia tevestensis (Péron, 1896), Neoptychites cephalotus (Coutiller, 1860), Thomasites rollandi (Thomas and Péron, 1889), Wrightoceras wallsi Reyment, 1954, and Choffaticeras (Choffaticeras) quaasi (Péron, 1904). This is a Lower Turonian assemblage referred to the Mammites nodosoides Zone, although the possibility that elements from the preceding Fagesia catinus Zone are also present cannot be excluded. The fauna from the transgressive glauconitic interval of the succeeding cycle comprises nine species, including Romaniceras (Romaniceras) mexicanum Jones, 1938, Romaniceras (Yubariceras) ornatissimum (Stoliczka, 1864), Pseudotissotia galliennei (d’Orbigny, 1850), Collignoniceras woollgari (Mantell, 1822) sensu lato, Coilopoceras springeri Hyatt, 1903, and Eubostrychoceras (Eubostrychoceras) saxonicum (Schlüter, 1872). They indicate the Middle Turonian Romaniceras (R.) mexicanum and R. (Y.) ornatissimum zones. The highest fauna, from the Marnes supérieurs de Saint-Louis of the Saint-Louis syncline, is: Subprionocyclus sp. juv., Prionocyclus sp. and Worthoceras cf. rochatianum (d’Orbigny, 1850). The Subprionocyclus are minute individuals that resemble S. bravaisianus (d’Orbigny, 1841), and suggest the presence of the lower Upper Turonian bravaisianus Zone.

15

Facies and integrated stratigraphy of the Upper Turonian (Upper Cretaceous) Grossberg Formation south of Regensburg (Bavaria, southern Germany)

63%

Niebuhr B. , Richardt N. , Wilmsen M.

Acta Geologica Polonica

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2012

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tom Vol. 62, no. 4

595-615

EN

The Upper Turonian Grossberg Formation of the Regensburg area (Danubian Cretaceous Group, Bavaria, southern Germany) has a mean thickness of 20-25 m and consists of sandy bioclastic calcarenites and calcareous sandstones which are rich in bryozoans, serpulids and bivalves (oysters, rudists, inoceramids). Eight facies types have been recognized that characterize deposition on a southward dipping homoclinal ramp: the inner ramp sub-environment was characterized by high-energy sandwave deposits (sandy bioclastic rud- and grainstones, bioclastic sandstones) with sheltered inter-shoal areas. In mid-ramp settings, bioturbated, glauconitic, calcareous sand- and siltstones as well as bioturbated, bioclastic wacke- and packstones predominate. The carbonate grain association of the Grossberg Formation describes a temperate bryomol facies with indicators of warm-water influences. An inferred surplus of land-derived nutrients resulted in eutrophic conditions and favoured the heterozoan communities of the Grossberg Ramp. Carbon stable isotope geochemistry cannot significantly contribute to the stratigraphic calibration of the Grossberg Formation due to the depleted and trendless bulk-rock [delta^13]C values, probably resulting from a shallow-water aquafacies with depleted [delta^13]C DIC values and low [delta^13]C values of syndepositional and early diagenetic carbonate phases. However, strongly enriched skeletal calcite [delta^13]C values support a correlation of the Grossberg Formation with the mid-Late Turonian positive Hitch Wood isotope event (Hyphantoceras Event of northern Germany). This interpretation is supported by biostratigraphic data and a range from the Mytiloides striatoconcentricus Zone into the lower My. scupini Zone is indicated by inoceramid bivalves. Both the base and top of the Grossberg Formation are characterized by unconformities. Sequence boundary SB Tu 4 at the base is a major regional erosion surface (erosional truncation of the underlying Kagerhoh Formation in the Regensburg area, fluvial incision at the base of the Seugast Member of the Roding Formation in the Bodenwohr area towards the north and northeast). It is suggested that this unconformity corresponds to a major sea-level drop recognized in many other Cretaceous basins below the Hitch Wood or Hyphantoceras Event. The transgression and highstand of the Grossberg Formation is concomitant to the deposition of the fluvial Seugast Member and the onlap of the marginal-marine. Veldensteiner Sandstein. onto the Frankische Alb. The unconformity at the top of the Grossberg Formation (late Late Turonian SB Tu 5) is indicated by a ferruginous firm-/ hardground and an underlying zone of strongly depleted [delta^13]C values. The abrupt superposition by deeper marine marls of the lower Hellkofen Formation (uppermost Turonian.Lower Coniacian) may be connected with inversion tectonics at the southwestern margin of the Bohemian Massif.

16

Turonian (Upper Cretaceous) inoceramid bivalves of the genus Mytiloides from the Sredna Gora Mountains, north-western Bulgaria

63%

Dochev D.

Acta Geologica Polonica

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2015

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tom Vol. 65, no. 1

101--119

EN

The inoceramid bivalves of the genus Mytiloides, from the Turonian (Upper Cretaceous) of the Sredna Gora Mts (north-western Bulgaria), are studied. The material comes from three sections: Izvor, Filipovtsi, and Vrabchov dol. Eight species are described taxonomically, with one left in open nomenclature: M. cf. mytiloides (Mantell, 1822), M. mytiloidiformis (Tröger, 1967), M. incertus (Jimbo, 1894), M. scupini (Heinz, 1930), M. herbichi (Atabekian, 1969), M. striatoconcentricus (Gümbel, 1868), M. labiatoidiformis (Tröger, 1967) and M. carpathicus (Simionescu, 1899). Mytiloides incertus and Mytiloides scupini are index species for the eponymous Upper Turonian inoceramid biozones

17

On some Turonian and Coniacian ammonites from central Colombia

63%

Kennedy W. J.

Acta Geologica Polonica

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2021

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tom Vol. 71, no. 3

259--285

EN

The rich collections of Turonian and Coniacian ammonites from Colombia, housed in the University of California Museum of Paleontology, Berkeley, are described, with 20 species recognized, referred to the genera Reymenticoceras Kennedy, 2018, Vascoceras Choffat, 1898, Fagesia Pervinquière, 1907, Wrightoceras Reyment, 1954a, Subprionocyclus Shimizu, 1932, Subprionotropis Basse, 1951, Prionocycloceras Spath, 1926, Barroisiceras de Grossouvre, 1894, Forresteria Reeside, 1932, Niceforoceras Basse, 1948, Peroniceras de Grossouvre, 1894, Gauthiericeras de Grossouvre, 1894, Protexanites Matsumoto, 1955, and Metaptychoceras Spath, 1926. One species, Reymenticoceras ornatum, is new. Most of the species described can be assigned to the substages and ammonite zones recognized in Western Europe.

18

The oldest African eucryptodiran turtle from the Cretaceous of Angola

63%

Mateus O. , Jacobs L. , Polcyn M. , Schulp A. S. , Vineyard D. , Buta Neto A. , Antunes M. T.

Acta Palaeontologica Polonica

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2009

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tom 54

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nr 4

EN

A new Late Cretaceous turtle, Angolachelys mbaxi gen. et sp. nov., from the Turonian (90 Mya) of Angola, represents the oldest eucryptodire from Africa. Phylogenetic analysis recovers Angolachelys mbaxi as the sister taxon of Sandownia harrisi from the Aptian of Isle of Wight, England. An unnamed turtle from the Albian Glen Rose Formation of Texas (USA) and the Kimmeridgian turtle Solnhofia parsonsi (Germany), are successively more distant sister taxa. Bootstrap analysis suggests those four taxa together form a previously unrecognized monophyletic clade of marine turtles, herein named Angolachelonia clade nov., supported by the following synapomorphies: mandibular articulation of quadrate aligned with or posterior to the occiput, and basisphenoid not visible or visibility greatly reduced in ventral view. Basal eucryptodires and angolachelonians originated in the northern hemisphere, thus Angolachelys represents one of the first marine amniote lineages to have invaded the South Atlantic after separation of Africa and South America.

19

Late Turonian ammonites from Haute-Normandie, France

63%

Kennedy W. J. , Gale A. S.

Acta Geologica Polonica

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2015

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tom Vol. 65, no. 4

507--524

EN

Upper Turonian chalks of Haute-Normandie yield a distinctive ammonite fauna within the Subprionocyclus neptuni ammonite Zone and the Plesiocorys (Sternotaxis) plana echinoid Zone. Well-localised material all comes from the phosphatic fauna of the Senneville 2 Hardground that marks the boundary between the Formation de Senneville and the Életot Member of the succeeding Formation de Saint-Pierre-en-Port. The association is dominated by Lewesiceras mantelli Wright and Wright, 1951, accompanied by Mesopuzosia mobergi (de Grossouvre, 1894), Lewesiceras woodiWright, 1979, Subprionocyclus hitchinensis (Billinghurst, 1927), Subprionocyclus branneri (Anderson, 1902), Subprionocyclus normalis (Anderson, 1958), Allocrioceras nodiger (F. Roemer, 1870), Allocrioceras billinghursti Klinger, 1976, Hyphantoceras reussianum (d’Orbigny, 1850), Sciponoceras bohemicum bohemicum (Fritsch, 1872), and Scaphites geinitzii d’Orbigny, 1850. The fauna represents the Hyphantoceras reussianum Event of authors, elements of which have been recognised on the north side of Tethys from Northern Ireland to the Mangyschlak Mountains of western Kazakstan, a distance of more than 3,500 kilometres.

20

Foraminifera and Late Cenomanian-Turonian biostratigraphy of the northern palaeobiogeographic district of Western Siberia

63%

Podobina V.

Geologos

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2013

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tom Vol. 19, No. 3

201--227

EN

The study of 114 core samples from seven borehole sections of the Van-Eganskaya area in the central part of Western Siberia yielded sufficient data to investigate the Late Cenomanian-Turonian foraminifers, palaeoenvironments, and the Late Cenomanian-Turonian biostratigraphy of this poorly studied area. Two Late Cenomanian foraminifer zones were established, viz. a (lower) Saccammina micra - Ammomarginulina sibirica Zone and an (upper) Trochammina wetteri tumida - Verneuilinoides kansasensis Zone. They reflect changes in the species composition of the foraminifer assemblages and lithology of the host rocks of the Uvatskian Horizon. In the lower part of the upper zone, beds with Gaudryinopsis nanushukensis elongatus are present. The changes in the species composition and lithology of the upper Cenomanian resulted from water-depth variations during the Boreal transgression. Two distinct assemblages and two homonymous zones, viz. the (lower) Gaudryinopsis angustus and the (upper) Pseudoclavulina hastata zones occur in the Turonian clayey cap-rocks of the superimposed Kuznetsovskian Horizon. Comparison of the Late Cenomanian-Turonian assemblages from the West-Siberian and Canadian provinces of the same Arctic palaeobiogeographical realm shows that the West-Siberian species are the same as, and closely related to, Canadian taxa, along with geographical subspecies. This comparison allows a detailed correlation, which results in a precise dating of the foraminifer zones.