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1

Integrated biostratigraphy and palaeoenvironments of the Upper Cretaceous in the Petrich section (Central Srednogorie Zone, Bulgaria)

Pavlishina Polina, Dochev Docho, Wagreich Michael, Koukal Veronika

Acta Geologica Polonica

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2023

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Vol. 73, no. 1

33--62

EN

The Upper Cretaceous succession (Coniacian to lowermost Maastrichtian, with focus on the Campanian) at Petrich, Central Srednogorie Zone in Bulgaria, is described and calibrated stratigraphically based on nannofossils, dinoflagellate cysts and inoceramids. The following standard nannofossil zones and subzones are identified: UC10-UC11ab (middle to upper Coniacian), UC11c-UC12-UC13 (uppermost Coniacian to Santonian), UC14a (lowermost Campanian), UC14bTP-UC15cTP (lower Campanian to ‘middle’ Campanian), UC15dTP-UC15eTP (upper Campanian), UC16aTP (of Thibault et al. 2016; upper part of the upper Campanian), and UC16b (Campanian-Maastrichtian boundary). The base of the Campanian is defined by the FO of Broinsonia parca parca (Stradner) Bukry, 1969 and Calculites obscurus (Deflandre) Prins and Sissingh in Sissingh, 1977 (a morphotype with a wide central longitudinal suture). The Areoligera coronata dinoflagellate cyst Zone (upper lower Campanian to upper upper Campanian) is identified, corresponding to the UC14bTP-UC16aTP nannofossil subzones. The inoceramid assemblage indicates the ‘Inoceramus’ azerbaydjanensis-‘Inoceramus’ vorhelmensis Zone, correlated within the interval of nannofossil subzones UC15dTP-UC15eTP. The composition of the dinoflagellate cyst assemblages and palynofacies pattern suggest normal marine, oxic conditions and low nutrient availability within a distal shelf to open marine depositional environment during the Campanian.

2

Turonian-Coniacian (Upper Cretaceous) of the Babadag Basin (North Dobrogea, Romania) : integrated biostratigraphy and microfacies succession

Lodowski Damian Gerard, Walaszczyk Ireneusz Piotr, Grădinaru Eugen

Geological Quarterly

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2019

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Vol. 63, No. 1

39--64

EN

The Upper Turonian to Middle Coniacian (Upper Cretaceous) succession of the Babadag Basin (North Dobrogea, Romania) constitutes an apparently continuous fossiliferous carbonate succession. The presence of moderately rich inoceramid, ammonite and foraminiferal assemblages allows for the application of a precise biostratigraphic subdivision. The palaeoenvironmental conditions and evolution of the Babadag Basin during the Late Turonian-Middle Coniacian are inferred using microfacies analysis and foraminiferal spectra. Together, these suggest the Turonian-Coniacian Badabag Basin reflects relatively shallow-water conditions in a near-shore environment, punctuated by two regression events in the Late Turonian and in the Middle Coniacian.

3

Inoceramids and associated ammonite faunas from the uppermost Turonian-lower Coniacian (Upper Cretaceous) of the Anaipadi-Saradamangalam region of the Cauvery Basin, south-east India

Walaszczyk I., Kennedy W. J., Paranjape A. R.

Acta Geologica Polonica

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2018

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Vol. 68, no. 4

663--687

EN

The lower (but not lowermost) part of the Upper Cretaceous Anaipadi Formation of the Trichinopoly Group in the area between Kulatur, Saradamangalam and Anaipadi, in the south-western part of the Cauvery Basin in southeast India yielded rich inoceramid and ammonite faunas. The ammonites: Mesopuzosia gaudama (Forbes, 1846), Damesites sugata (Forbes, 1846), Onitschoceras sp., Kossmaticeras (Kossmaticeras) theobald ianum (Stoliczka, 1865), Lewesiceras jimboi (Kossmat, 1898), Placenticeras kaffrarium Etheridge, 1904, and Pseudoxybeloceras (Schlueterella) sp., are characteristic of the Kossmaticeras theobaldianum Zone. The absence of Peroniceras (P.) dravidicum (Kossmat, 1895) indicates the presence of only lower part of this zone, referred to the nominative Kossmaticeras theobaldianum Subzone at the localities studied. The inoceramids present are Tethyoceramus madagascariensis (Heinz, 1933) and Cremnoceramus deformis erectus (Meek, 1877), recorded for the first time from the region. The latter dates the studied interval as early early Coniacian, and allows, for the first time, direct chronostratigraphic dating of the Tethyoceramus madagascariensis Zone, and consequently also of the Kossmaticeras theobaldianum Subzone. As inoceramids occur in the middle part of the ammonite-rich interval, the Kossmaticeras theobaldianum Subzone may be as old as latest Turonian and not younger than early early Coniacian. The base of the Coniacian lies in the lower, but not lowermost part of the Anaipadi Formation. Both inoceramids and ammonites represent taxa known from Madagascar and South Africa.

4

Klasyczne stanowiska paleontologiczne górnej kredy zachodniej Ukrainy: historia badań oraz biostratygrafia

Machalski M., Malchyk O.

Przegląd Geologiczny

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2016

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Vol. 64, nr 8

570--576

EN

For a long time, outcrops at Potelych, Nahoryany and Lviv in western Ukraine have been of special interestfor Campanian andMaastrichtian (Upper Cretaceous) palaeontology and biostratigraphy. An overview of studies devoted to these classic sites is presented, including an early account of the locality of Nahoryany in a Polish newspaper, dated 1843. The biostratigraphic position ofthese successions is reviewed, based on recent progress in studies of inoceramid bivalves and ammonites. The succession at Potelych, from where a unique land flora was described at the beginning of the 20th century, represents the upper Campanian “Ino- ceramus” costaecus Zone. The Nahoryany opoka, the source of rich fossil collections that were sent to many European museums in the 19th century, belongs to the lower Maastrichtian Endo- costea typica and Trochoceramus radiosus zones. The so-called Lviv marls correspond to the lower upper Maastrichtian Spyridocera- mus tegulatus Zone. The giant scaphitid ammonites Hoploscaphites quadrispinosus and Acanthoscaphites tridens s. str from Potelych and Nahoryany corroborate the inoceramid-based dating of these successions.

5

Encrustation of inarticulate brachiopods on scaphitid ammonites and inoceramid bivalves from the Upper Cretaceous U. S. Western Interior

Landman N. H., Slattery J. S., Harries P. J.

Acta Geologica Polonica

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2016

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Vol. 66, no. 4

645--662

EN

The inarticulate brachiopod Discinisca is a rare faunal element in the Upper Cretaceous of the U.S. Western Interior. We report two occurrences of encrustation of Discinisca on a scaphitid ammonite (scaphite) and several inoceramids from the lower Maastrichtian Baculites baculus/Endocostea typica Biozones of the Pierre Shale at two localities. Six specimens of Discinisca are present on a single specimen of Hoploscaphites crassus from eastcentral Montana. They occur along the furrow at the mature apertural margin. Because the brachiopods are restricted to the margin and do not occur on the rest of the shell, it is likely that they encrusted the ammonite during its lifetime. If so, this implies that the soft body of the scaphite did not cover the outside surface of the aperture, leaving this area vulnerable to epizoan attachment. A total of 13 specimens of Discinisca are also present on four specimens of Cataceramus? barabini from east-central Wyoming. The brachiopods occur in crevices on the outside of the shells and may have encrusted the inoceramids after their death as the shells began to break down and delaminate, resulting from the decomposition of the organic matrix holding them together. Based on the faunal assemblages at both localities, the presence of Discinisca may indicate environments with either low oxygen levels and/or few predators or competitors.

6

Palaeontology of the Middle Turonian limestones of the Nysa Kłodzka Graben (Sudetes, SW Poland): biostratigraphical and palaeogeographical implications

Chrząstek Alina

Geologos

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2012

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Vol. 18, No. 2

83--109

EN

The ammonites Lewesiceras peramplum Mantell and ?Lewesiceras sp. are reported from the Upper Cretaceous in the Nysa Kłodzka Graben; they date from the Middle Turonian and ?Coniacian, respectively. The Middle Turonian limestones of the Stara Bystrzyca quarry contain an abundant assemblage of inoceramids (Inoceramus cuvieri Sowerby and I. lamarcki Parkinson) and other bivalves, including oysters, as well as brachiopods and trace fossils. Micropalaeontological data show the presence of foraminifers and siliceous sponge spiculae, bryozoans, ostracods and fragments of bivalves and gastropods. The Middle Turonian calcareous deposits belongs to the upper part of the Inoceramus lamarcki Zone (late Middle Turonian) and were deposited on a shallow, subtidal offshore shelf. They overlie the Middle Turonian Bystrzyca and Długopole Sandstones, which represent foreshore-shoreface delta deposits. The fossil assemblage suggests a moderate- to low-energy, normal-salinity environment with occasionally an oxygen deficit.

7

Testing the congruence of the macrofossil versus microfossil record in the Turonian-Coniacian boundary succession of the Wagon Mound-Springer composite section (NE New Mexico, USA)

Walaszczyk I., Lees J., Peryt D., Cobban W., Wood C.

Acta Geologica Polonica

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2012

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Vol. 62, no. 4

581-594

EN

The Turonian-Coniacian boundary succession from the Wagon Mound-Springer composite section in the US Western Interior shows a virtually identical macrofaunal record to that revealed in the proposed candidate Coniacian GSSP in the Salzgitter-Salder-Slupia Nadbrzezna composite section in central Europe, with easy identification in both regions of the base of the Coniacian Stage, as defined by the first appearance of the inoceramid bivalve species, Cremnoceramus deformis erectus (Meek). The macrofaunal boundary definition is additionally confirmed by the foraminiferal and nannofossil data, demonstrating the high potential of the inoceramid marker for the base of the Coniacian. The former claims about distinct diachroneity between macrofossil and microfossil dates in the trans-Atlantic correlations, resulted from methodological deficiencies, and have no factual basis.

8

A new Lower Coniacian fauna from the Jerzmanice Zdrój region of the North Sudetic Basin, SW Poland

Chrząstek A.

Geologia Sudetica

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2008

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Vol. 40

33-50

EN

This paper describes and interprets a newly discovered Lower Coniacian (lower Upper Cretaceous) macro- and micro- fossil fauna (vertebrate and invertebrate remains) from sedimentary rocks of the Jerzmanice Zdrój region of the North Sudetic Basin of SW Poland. Several inoceramid bivalve taxa that previously were only known from other parts of the North Sudetic Basin were recovered from light grey, marly sandstones of Early Coniacian age. A fragment of ammonite was also discovered, as was a shark's tooth from the family Cretoxyrhinidae: this may be Cretoxyrhina mantelli Agassiz, 1843, a species not hitherto known from the Lower Coniacian (Emscherian sensu Scupin (1912-13)) of the North Sudetic Basin. Abundant foraminifers were observed in thin sections. The newly discovered inoceramid bivalves - Cremnoceramus deformis erectus Meek, 1877, Cremnoceramus waltersdorfensis waltersdorfensis Andert, 1911 and Inoceramus lusatiae Andert, 1911 - fit into the current biostratigraphic scheme for the region. The inoceramids can all be assigned to the Cremnoceramus deformis erectus Zone, which correlates with the Gavelinella moniliformis foraminiferal Zone and thereby confirms an Early Coniacian age. The Turonian-Coniacian boundary in the North Sudetic Basin can now be placed between the respective inoceramid zones of Inoceramus costellatus Woods, 1912 (actually Mytiloides costellatus Woods, 1912) and Inoceramus schloenbachi Böhm, 1911 (actually Cremnoceramus crassus crassus Petrascheck, 1903). The macrofossils found in the Jerzmanice section suggest that the host sediments were laid down in a Late Cretaceous epicontinental basin, under the North Sudetic Sea, that had deepened during the Early Coniacian. This interpretation agrees with the global bathymetric curve for the Late Cretaceous in Europe.

9

Palaeontology and biostratigraphy of the Middle-Upper Coniacian and Santonian inoceramids of the US Western Interior

Walaszczyk I., Cobban W.

Acta Geologica Polonica

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2006

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Vol. 56, no. 3

241-348

EN

The taxonomy of the Middle-Late Coniacian and Santonian inoceramids of the US Western Interior, including some specimens from the Canadian Western Interior, is revised, based mainly on the extensive collections of the US Geological Survey. The classic Meek and Hayden material is discussed. Forty-four species are described of which 5 are new: Inoceramus americanus, Inoceramus sokolovi, Inoceramus robertsoni, Inoceramus glacierensis, and Sphenoceramus gilli. The Middle Coniacian to Santonian inoceramids of the Western Interior represent a uniform Euramerican fauna. This allows the application of a uniform biostratigraphical zonation throughout the whole biogeographical region. Starting in the Late Coniacian, inoceramid faunas are characterised by relatively strong north.south biogeographic differentiation. The inoceramid zonation applied is discussed, diagnosed, and compared to previously used schemes, and to the ammonite zonation commonly used in the US Western Interior.

10

New observations on the inoceramid biostratigraphy of the higher part of the Upper Turonian and the Turonian - Coniacian boundary transition in Poland, Germany and the UK

Wood C., Walaszczyk I., Mortimore R., Woods M.

Acta Geologica Polonica

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2004

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Vol. 54, no. 4

541-550

EN

New studies of sections in southern England (Bridgewick Pit, Downley, Shoreham Cement Works Quarry), eastern England (Kiplingcotes Station Quarry, Arras Road Pit), Germany (Salzgitter-Salder Quarry, a potential candidate GSSP for the Coniacian Stage) and central Poland (Słupia Nadbrzeżna, another potential candidate GSSP) have enabled a re-evaluation and refinement of the inoceramid biostratigraphy of the higher part of the Upper Turonian and the Turonian-Coniacian boundary transition. The inoceramid record at Słupia Nadbrzeżna below the terminal Turonian entry of Cremnoceramus is shown to be more complete than at the standard Salzgitter-Salder Quarry section. A new inoceramid event (Inoceramus lusatiae Event) identified at Słupia Nadbrzeżna is inferred to be present at the Sonnenberg Quarry, Waltersdorf, the type locality of Inoceramus lusatiae, as well as of I. glatziae and Cremnoceramus waltersdorfensis,and it is possibly represented in the condensed Navigation Hardgrounds in southern England. The absence of this event at Salzgitter-Salder suggests a significant hiatus. An inoceramid assemblage characterised by a taxon of uncertain affinities that immediately precedes the flood occurrence of Cremnoceramus (waltersdorfensis I Event) at Salzgitter-Salder has been identified at a comparable biostratigraphic position in eastern England (Yorkshire) and, tentatively, also in southern England. Inoceramids from this assemblage in the UK had previously been incorrectly assigned to Cremnoceramus waltersdorfensis and the basal Coniacian marker taxon, C. deformis erectus. The position of the base of the Coniacian has accordingly been revised upwards in both the southern and eastern England successions.

11

Linking southern Poland and northern Germany: Campanian cephalopods, inoceramid bivalves and echinoids

Jagt J.

Acta Geologica Polonica

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2004

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Vol. 54, no. 4

573-586

EN

The Campanian strata in the Wolbrom-Miechów area at Wierzchowisko, Jeżówka and Rzeżuśnia (i.e., the southwestern part of the Miechów Trough, southern Poland) have been studied in some detail. Collections of macrofossils available to date include generally well-preserved and diverse cephalopods (ammonoids, coleoids), inoceramid bivalves and irregular echinoids of considerable stratigraphic and correlative value. For the present paper, taxa which allow a preliminary correlation with northern Germany (Lagerdorf, Lehrte West Syncline and Munsterland Basin) are singled out for brief discussion. Stratigraphically useful taxa include the ammonites Pachydiscus (P.) haldemsis (SCHLUTER), Lewyites elegans (MOBERG), Scaphites (S.) hippocrepis III sensu COBBAN, S. (S.) gibbus SCHLUTER and Trachyscaphites spiniger spiniger (SCHLUTER), the coleoids Belemnitella ex gr. mucronata (VON SCHLOTHEIM) and Gonioteuthis quadrata (DE BLAINVILLE),the inoceramids Cataceramus dariensis (DOBROV & PAVLOVA), "Inoceramus" azerbaydjanensis ALIEV and "I." agdjakendsis ALIEV, and the echinoids Offaster pilula (LAMARCK), Galeola papillosa (LESKE), Echinocorys ex gr. subglobosa/turrita, E. ex gr. conica, Micraster (Gibbaster) ex gr. fastigatus/stolleyi and M. (M.) ex gr. schroederi/glyphus. The ammonite fauna, which is dominated by pachydiscids and diplomoceratids, is closely comparable to that from the Busko Zdrój area (i.e., the southeastern part of the Miechów Trough), but hoplitoplacenticeratids are still unknown from the Wolbrom-Miechów area which, taken together with inoceramid data, may point to a gap in the upper Lower Campanian (equivalent of conica/mucronata Zone).

12

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

Walaszczyk I., Kopaevich L., Olferiev A.

Acta Geologica Polonica

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2004

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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

Cenomanian through Lower Coniacian events in the Upper Cretaceous of Saxony, Germany

Troger K.

Acta Geologica Polonica

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2004

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Vol. 54, no. 4

629-638

EN

The event sequence recognised in the Cenomanian through basal Coniacian (Late Cretaceous) of the Elbe Valley is compared with the event stratigraphic scheme worked out in NW Germany. The following events, recognised originally in Lower Saxony, and subsequently in other Cretaceous areas of north-western Europe, were found in Saxony: Schloenbachia / virgatus eustatoevent (Lower Cenomanian); Chondrites ecoevent, Puzosia eustatoevent and plenus eustatoevent (Upper Cenomanian); hattini ecoevent, Mytiloides ecoevents, hercynicus ecoevent, Hyphantoceras ecoevent, Didymotis ecoevents and waltersdorfensis ecoevent (Turonian); erectus ecoevent, hannovrensis ecoevent, and incostans ecoevent (Lower Coniacian). Both the oxic/anoxic Cenomanian/Turonian boundary event and the facies change at the base of the Metoicoceras geslinianum Zone are recognisable. With the exception of the Mytiloides ecoevents, recorded in all facies types, all the events are well developed only in the marly-silty facies.Local events, specific to the Cretaceous of Saxony are: the Late Cenomanian Pennrich event, known from the Sudetic area, and the Middle Turonian rhynchonellid events, occurring in sandy and transitional facies between Pirna and Bad Schandau.

14

Upper Cretaceous of the Barranca (Navarra, northern Spain); integrated litho-, bio- and event stratigraphy.Part 2, Campanian and Maastrichtian

Kuchler T.

Acta Geologica Polonica

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2000

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Vol. 50, no. 4

441-499

EN

Campanian to Lower Maastrichtian strata of the eastern Barranca (Navarra, northern Spain), based on 11 exposures near Irurzun, were investigated in detail and correlated with coeval strata of the western Barranca and the Oroz-Betelu Massif (Navarra). The Sarasate Formation exposed in the Barranca in divided into ten members. Deposition was influenced by uplift of the Anoz-Ollo salt structure during the latest Santonian and Early Campanian. The Campanian-Maastrichtian of Navarra is characterised by thick and relatively complete successions containing biostratigraphically significant fossil groups (ammonites, inoceramids, echinoids). Detailed bed-by-bed collecting has enabled the establishment of an integrated zonal scheme with potential for interbasinal correlation. In addition to local peak, partial range and assemblage zones, based on echinoids and ammonite-echinoid assemblages, an ammonite zonation, based on an unnamed interval and the following 10 partial range (PRZ) and assemblage zones (AZ) of Scaphites hippocrepis III, S. hippocrepis III/Menabites spp., Hoplitoplacenticeras marroti, Trachyscaphites spiniger, Pseudoxybeloceras phaleratum, Nostoceras (Bostrychoceras) polyplocum, Trachyscaphites pulcherrimus, N. (didymoceras) archiacianum, N. (Nostoceras) hyatti and Pachydiscus neubergicus/Pachydiscus epiplectus, is presented. The ammonite zonation markedly refines both the existing regional and the so-called European standard zonal schemes. Correlation with other Spanish areas (Cantabria, Burgos and Guipuzcoa), the Aquitaine (France), Westphalia and Lower Saxony (Germany) and the Vistula valley (Poland) is discussed. Twelve of the recognised bio-events, characterised by mass-occurrences of irregular echinoids and of monospecific, or taxonomically more variable, mostly heteromorph ammonite assemblages, are significant for regional correlation. Three Offaster maxima are of interbasinal importance as they can be correlated to Germany, Great Britain and Northern Ireland. The origin of these bio-events is closely related to the transgressive and regressive pulses recognised in Navarra, of which the pomeli Transgression I and the hippocrepis, subglobosa and polyplocum regressions are the most pronounced. The tectonic phase at the Santonian/Campanian boundary is related to the Wernigerode Phase. The onset of the second phase is placed in the lower Upper Campanian marotti Zone, the onset of a third phase (UCTE) in theUpper Campanian polyplocum Zone.

15

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)

Kennedy W., Walaszczyk I., Cobban W.

Acta Geologica Polonica

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2000

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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.

16

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

Walaszczyk I.

Acta Geologica Polonica

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2000

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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

17

Inoceramids and buchiids in the Tithonian deposits of western Cuba: a possible faunistic link with South-Eastern Pacific

Myczyński R.

Studia Geologica Polonica

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1999

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Vol. 114

77-92

EN

Occurrence of the “Boreal type” bivalves: inoceramids (represented by the genera: Inoceramus Parkinson, 1819; Retroceramus Koshelkina, 1963 and Anopaea Eichwald, 1861) and buchiids (Buchia Rouillier, 1845) in the Tithonian sections of the Sierra de los Organos and Sierra del Rosario belts, western Cuba, is described. Anopaea and other “Boreal” bivalves probably migrated to the Cuban Jurassic basin over the South American shelf and probably throught Southern Mexico. Their occurrence might reflect cooler temperature in the proto-Caribbean basin caused by oceanic currents and/or upwelling, rather than tectonic transport from Southern Boreal province.

18

The Upper Cretaceous succession (Cenomanian - Santonian) of the Staffhorst Shaft, Lower Saxony, northern Germany: integrated biostratigraphic, lithostratigraphic and downhole geophysical log data

Niebuhr B.

Acta Geologica Polonica

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1999

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Vol. 49, no. 3

175-213

EN

The Cenomanian to Santonian succession of the Staffhorst shaft, ca. 50 km south of Bremen, because of its structural position in the northern German Upper Cretaceous basin, is intermediate in character and fossil content between the pelagic sediments characterizing the Pompeckj Block in the north and the proximal sediments of the Lower Saxony Block in the south. The biostratigraphic subdivision of the shaft is based on inoceramids, echinoids, belemnites and foraminifera. The various biozonations and zonal boundaries used in the Boreal Realm are compared and applied to the zonation of the shaft succession, and the biostratigraphy of the individual fossil groups is described. A new inoceramid zone, that of Inoceramus gibbosus, is proposed for the topmost Lower Coniacian; and an echinoid assemblage zonation is introduced. The existing benthic foraminiferal zonation of the Middle Turonian to Santonian has been modified, with changed age assignments based on the macrofossil zonation. The proposed basal stage boundary criteria of the "Second International Symposium on Cretaceous Stage Boundaries" (Brussels, 1995) could be applied only in some cases. The proximity of the Staffhorst shaft to the trial borehole, situated only 39 m away, has permitted the Self Potential (SP) and Resistivity (R) logs to be uniquely directly calibrated against the lithostraligraphical and biostratigraphic succession of the shaft. The previous identification of some stage and substage boundaries on the logs of northern German boreholes based on foraminiferal zonation will need to be shifted by several tens of metres as a result of thid calibration.

19

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

Kuchler T.

Acta Geologica Polonica

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1998

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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.

20

The Turonian - Coniacian boundary in the United States Western Interior

Walaszczyk I., Cobban W.

Acta Geologica Polonica

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1998

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Vol. 48, no. 4

495-507

EN

The Turonian/Coniacian boundary succession in the United States Western Interior is characterized by the same inoceramid faunas as recognized in Europe, allowing the application of the same zonal scheme in both regions; Mytiloides scupini and Cremnoceramus waltersdorfensis zones in the tompost Turonian and Cremnoceramus deformis erectus Zone in the lowermost Coniacian. The correlation with Europe is enhanced, moreover, by a set of boundary events recognized originally in Europe and well represented in the Western Interior: Didymotis I Event and waltersdorfensis Event in the tompost Turonian, and erectus I, II and ?III events in the Lower Coniacian. First "Coniacian" ammonite, Forresteria peruana, appears in the indisputable Turonian, in the zone of M. scupini, and the reference to Forresteria in the boundary definition should be rejected. None of the North American sections, proposed during the Brussels Symposium as the potential boundary stratotypes, i.e. Wagon Mound and Pueblo sections, appears better than the voted section of the Salzgitter-Salder. The Pueblo section is relatively complete but markedly condensed in comparison with the German one, but it may be used as a very convenient reference section for the Turonian/Coniacian boundary in the Western Interior. The Wagon Mound section was mis-interpreted in respect of its biostratigraphical position and is entirely of Late Turonian age.