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The Turonian Stage and Substage Boundaries by Peter BENGTSON (Compiler) with Contributions by William A

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BULLETIN DE L'INSTITUT ROYAL DES SCIENCES NATURELLES DE BELGIQUE SCIENCES DE LA TERRE, 66-SUPP.: 69-79, 1996 BULLETIN VAN HET KONINKLIJK BELGISCH INSTITUUT VOOR NATUURWETENSCHAPPEN AARDWETENSCHAPPEN, 66-SUPP.: 69-79. 1996 The Turonian stage and substage boundaries by Peter BENGTSON (compiler) with contributions by William A. Cobban, Paul Dodsworth, Andrew S. Gale, William James Kennedy, Marcos A. Lamolda, Tatsuro Matsumoto, Richard A. Reyment, Ekbert Seibertz and Karl-Armin Tröger. «golden spike») abb CeHOMaHO-TypoHCKOÏi rpaHHLtbl flonxeH Abstract öbiTb onpeflenëH b pa3pe3e Rock Canyon Anticline, Ha 3anane Pueblo, Konopaflo, CLUA, b ocHOBaHUM Gnoa 86, Formai définitions of the Cenomanian-Turonian and lower-middle coBnaflaioiuero c nepBbiM noHB/ieHHeM aMMOHHTa Turonian are boundaries proposed, following discussions at the Second watinoceras devonense (wright & kennedy, 1981). B International Symposium on Cretaceous Stage Boundaries, held in KanecTBe gssp ahh HUXHe-cpeAHeü TypoHcxoft rpaHHLtbl Brussels, 8-16 September 1995. The Global boundary Stratotype Sec¬ 6bi.no npeanoxteHO nepBoe noHBneHHe aMMOHHTa tion and Point (GSSP, "golden spike") for the Cenomanian-Turonian Collignonoceras woollgari (mantell, 1822) Toro xce boundary should be placed at the base of Bed 86 in a section at Rock pa3pe3a(CnoPi 120). Hto KacaeTca cpeAHe-Bepxnero Canyon Anticline, west of Pueblo, Colorado, USA, coincident with the TypoHa, to Ha AaHHbiü MOMeHT npeftnoxmb KaKoü-nn6o gssp first occurrence of the ammonite Watinoceras devonense Wright & He npeACTaBnseTCB B03M0)KHbiM. Kennedy, 1981. A GSSP for the lower-middle Turonian boundary is proposed at the level of first occurrence of the ammonite Collignoni- KnioHeBbie cnosa: TypoHCKwü npyc, BepxHMû Men, ceras woollgari (Mantell, 1822) in the same section (Bed 120). For xpoHOCTpaTHrpachHB, 6nocTpaTnrpacJ)HB, unioiocTpaTurpacbun, the middle-upper Turonian boundary no GSSP can be proposed at present. KapÔOHHHeCKHe M3OT0nbl, aMMOHMTbl, HHOUepaMbl, ChopaMHHHChepbl, HaHOCt>OCCMnHM, CTpaTOTHflbl, gssp. Key-words: Turonian, Upper Cretaceous, chronostratigraphy, biostra- tigraphy, cyclostratigraphy, carbon isotopes, ammonites, inoceramids, foraminifers, nannofossils, stratotypes, GSSP. Introduction Résumé The Turonian Working Group of the Subcommission on Cretaceous Stratigraphy has in recent years been Des définitions formelles sont proposées pour la limite Cénomanien- primarily concerned with the définition of the bases Turonien et pour la limite Turonien inférieur-moyen, suite aux dis¬ of the Turonian cussions lors du "Second International Symposium on Cretaceous substages. According to informai but Stage Boundaries" (Bruxelles 8-16 septembre 1995). Le "Global well-established usage the Turonian Stage is best subdi- boundary Stratotype Section and Point" (GSSP, "golden spike") pour vided into three substages. Work has focused on agree- la limite Cénomanien-Turonien devrait être placé dans une section à Rock Canyon Anticline, à l'ouest de Pueblo, Colorado, USA, à la base ing about suitable chronostratigraphical levels for the du Banc 86 qui coïncide avec la première apparition de l'ammonite bases of the lower, middle and upper Turonian substa¬ Watinoceras devonense Wright & Kennedy, 1981. Comme GSSP ges, respectively, and on finding suitable boundary stra¬ pour la limite Turonien inférieur-moyen la première apparition de l'ammonite Collignoniceras woollgari (Mantell, 1822) dans la même totypes in which these levels can be appropriately fixed section (Banc 120) a été proposée. Pour la limite Turonien moyen- through GSSPs (Global boundary Stratotype Sections supérieur aucun GSSP ne peut être proposé pour le moment. and Points or, colloquially, golden spikes). The Cenoma¬ nian-Turonian Mots-clefs: Turonien. Crétacé supérieur, chronostratigraphie, biostra¬ boundary (i.e., the base of the [lower] tigraphie, cyclostratigraphie, isotopes du carbone, ammonites, inocé- Turonian) has become one of the least controversial ramidés, foraminifères, nannofossiles, stratotypes, GSSP. among the Cretaceous stage boundaries. The reason for 1 TypoHCKMfi apyc m rpaHtmbi noflwipyca: npetyioxeHMSt Stage (and substage) boundaries are chronostratigraphical datum PaöoHeü Tpynnbi TypoHCKoro npyca noflKOMUccun MenoBoft planes and by définition globally isochronous. As biostratigraphical CTpaTurpacJtMM. markers, such as first occurrences (FOs) of taxa or bases of biozones, are bound to be diachronous (no matter how insignificantly, geologi- Pe3ioMe. cally speaking) they cannot be used to define stage boundaries. The ctopMajibHoe onpefleneHHe CeHOMaHO-TypoHCKOM h HMXHe- International Commission on Stratigraphy (Remane 1995) recom- cpeAHeïi TypoHCKoPi rpaHHU 6t>ino npeAJioxeHo nocne mends that stage boundaries should be defined by Global boundary o6cy>«AeHnPt, npoujeauinx b TeneHwe BToporo Stratotype Sections and Points (GSSPs). Biostratigraphical or other MexflyHapoflHoro CnMno3uyMa (Bpioccejib, 8-16 ceHTHÖpn markers in the rock record inferred to be nearly isochronous are then 1995), nocBHLttëHHoro TpaHHuaM MenoBbix flpycoB. «Global important instruments for the Worldwide récognition of boundaries defined boundary Stratotype Section and Point» (GSSP, by GSSPs. 70 Peter BENGTSON this is partly to be sought in the considérable international Turonian boundary, whereas the concept of the middle- attention given to the Cenomanian-Turonian boundary upper Turonian boundary remains more elusive. The in recent years, as a resull of the discovery of a World¬ Turonian stage and substage boundaries are discussed wide oceanic anoxie event and a possible mass extinction here and proposals made for GSSPs for the Cenoma¬ event near or at the boundary. In 1991, at Grenoble, nian-Turonian and lower-middle Turonian boundaries, France, an entire international symposium was devoted respectively. These proposals are the main outcome of to the Cenomanian-Turonian boundary (cf. Robaszynski discussions at the Second International Symposium on & Gale, 1993). The biostratigraphical "définition" 1 of Cretaceous Stage Boundaries, held in Brussels, 8-16 the boundary has remained relatively stable during the September 1995, and subséquent postal voting among past decade or so; this is also true of the lower-middle the members of the Turonian Working Group. PUEBLO bioevents geochemistry eustacy ammonite assembl. zones equivalent zones TURONIAN Mammites nodosoides M.n. 6 l t: FS i Vascoceras sensu a s13c birchbyi Kennedy 1 s 1984 i 'o § sensu '6 Pseudaspidoceras Cobban ^, flexuosum k 1984 Watinoc. l! 5 Colorado. Ag Pseuda- Assembl. Watinoceras spidoc. Zone devonense flexuosum là Zone TR 4 m. '■g Nigericeras 'Si scotti '•S I 3 q> Neocardioceras I'S juddii 'I 3 a/./I 'à Burroceras clydense CENOMANIAN Europe Metoico. Sciponoceras i Euomph. i Plenus TS 2 - gracile gesl. iseptems-t Zone ^ SMW 1 M.g.^ SB Metoicoceras mosbyense HS Calycoceras _ Calycoceras canitaurinum naviculare Text-fig. 1 — Cenomanian-Turonian boundary stratigraphy, illustrated by the section at Rock Canyon Anticline, near Pueblo, Colorado, USA, showing six of the alternative levels for defining the boundary. 1. Base of the Sciponoceras gracile-Metoicoceras geslinianum-Euomphaloceras septemseriatum-Actinocamax plenus Assemblage Zone, with FO of M. geslinianum (d'Orbigny, 1850) and LOs of the genera Dunveganoceras and Cunningtoniceras. Commencement of 5BC excursion. Sequence boundary. 2. LO of Calycoceras naviculare (Mantell, 1822), approximately coincident with LO of the genus Rotalipora, notably Rotalipora cushmani (Morrow, 1934), at the transgressive surface, coincident with the first 813C max¬ imum. 3. FOs of Neocardioceras juddii (Barrois & de Guerne, 1878) and the genera Pseudaspidoceras, Watinoceras, Fagesia, etc. LOs of M. geslinianum and F. septemseriatum (Cragin, 1893), approximately coincident with the second ô13C maximum. 4. FO of Watinoceras devonense Wright & Kennedy, 1981, approximately coincident with the FOs of the genus Mytiloides and Quadrum gartneri Prins & Perch-Nielsen, 1977. ö'3C starts to fall. 5. FOs of Pseudaspidoceras flexuosum Powell, 1963, and the genera Mammites, Wrightoceras and then Neopty- chites. 6. FOs of Mammites nodosoides (Schlüter, 1871) and the genus Morrowites. Flooding surface. (Modified after Robaszynski & Gale, 1993, table 1.) The Turonian boundary proposals 71 The Cenomanian-Turonian boundary (= base of the index has a restricted geographical distribution). Impor¬ [lower] Turonian) tant support for that boundary définition is the widespread appearance of early représentatives of the inoceramid Historical review genus Mytiloides. Birkelund et al. (1984) argued that a suitable bound¬ A large number of biostratigraphical datums have been ary stratotype for alternative b should lie in Texas or used historically and in more recent times as markers for Mexico, where both the Pseudaspidoceras flexuosum the Cenomanian-Turonian boundary. In order to preserve Zone and the underlying Neocardioceras juddii Zone continuity it is important that the boundary level to be are rich in ammonites. The section chosen should also chosen agree with the historical view as expressed by contain Mytiloides and other groups such as planktonic d'Orbigny (1850, 1852; see review by Wright & Ken¬ foraminifers. nedy 1981, p. 126). In terms of the traditional "standard" In the plenary session of the 1991 Grenoble meeting ammonite zonation this means that the boundary should the boundary alternatives were discussed further and be chosen so as to fall within the interval between the illustrated
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    Boletín de Geología ISSN: 0120-0283 [email protected] Universidad Industrial de Santander Colombia Patarroyo, Pedro SUCESIÓN DE AMONITAS DEL CRETÁCICO SUPERIOR (CENOMANIANO – CONIACIANO) DE LA PARTE MÁS ALTA DE LA FORMACIÓN HONDITA Y DE LA FORMACIÓN LOMA GORDA EN LA QUEBRADA BAMBUCÁ, AIPE - HUILA (COLOMBIA, S. A.) Boletín de Geología, vol. 33, núm. 1, enero-junio, 2011, pp. 69-92 Universidad Industrial de Santander Bucaramanga, Colombia Disponible en: http://www.redalyc.org/articulo.oa?id=349632022005 Cómo citar el artículo Número completo Sistema de Información Científica Más información del artículo Red de Revistas Científicas de América Latina, el Caribe, España y Portugal Página de la revista en redalyc.org Proyecto académico sin fines de lucro, desarrollado bajo la iniciativa de acceso abierto Boletín de Geología Vol. 33, N° 1, enero-junio de 2011 SUCESIÓN DE AMONITAS DEL CRETÁCICO SUPERIOR (CENOMANIANO – CONIACIANO) DE LA PARTE MÁS ALTA DE LA FORMACIÓN HONDITA Y DE LA FORMACIÓN LOMA GORDA EN LA QUEBRADA BAMBUCÁ, AIPE - HUILA (COLOMBIA, S. A.) Pedro Patarroyo1 RESUMEN La sección de la quebrada Bambucá (Aipe - Huila) posee una buena exposición de los depósitos del Cretácico del Valle Superior del Magdalena. De la parte alta de la Formación Hondita se recolectaron Acanthoceras sp. y Rhynchostreon sp. del Cenomaniano superior. Dentro del segmento inferior de la Formación Loma Gorda se hallaron Choffaticeras (C.) cf. segne, Fagesia cf. catinus, Neoptychites cf. andinus, Mitonia gracilis, Morrowites sp., Nannovascoceras ? sp., Quitmaniceras ? sp., Benueites ? sp. junto con Mytiloides kossmati, M. goppelnensis y Anomia sp. del Turoniano inferior. Estratigráficamente arriba aparecen Paramammites ? sp., Hoplitoides sp.
  • Redalyc. SUCESIÓN DE AMONITAS DEL CRETÁCICO SUPERIOR (CENOMANIANO – CONIACIANO) DE LA PARTE MÁS ALTA DE LA FORMACIÓN HONDI

    Redalyc. SUCESIÓN DE AMONITAS DEL CRETÁCICO SUPERIOR (CENOMANIANO – CONIACIANO) DE LA PARTE MÁS ALTA DE LA FORMACIÓN HONDI

    Boletín de Geología ISSN: 0120-0283 [email protected] Universidad Industrial de Santander Colombia Patarroyo, Pedro SUCESIÓN DE AMONITAS DEL CRETÁCICO SUPERIOR (CENOMANIANO – CONIACIANO) DE LA PARTE MÁS ALTA DE LA FORMACIÓN HONDITA Y DE LA FORMACIÓN LOMA GORDA EN LA QUEBRADA BAMBUCÁ, AIPE - HUILA (COLOMBIA, S. A.) Boletín de Geología, vol. 33, núm. 1, enero-junio, 2011, pp. 69-92 Universidad Industrial de Santander Bucaramanga, Colombia Available in: http://www.redalyc.org/articulo.oa?id=349632022005 Abstract The Bambucá creek section (Aipe - Huila) shows a very good exposition of the Upper Magdalena Valley Cretaceous deposits. To the upper part of the Hondita Formation were recollected Acanthoceras sp. and Rhynchostreon sp. of the upper Cenomanian. Related to the lower segment of the Loma Gorda Formation were found Choffaticeras ( C .) cf. segne , Fagesia cf. catinus , Neoptychites cf. andinus , Mitonia gracilis , Morrowites sp., Nannovascoceras ? sp., Quitmaniceras ? sp., Benueites ? sp., Paramammites ? sp. togheter with Mytiloides kossmati , M . goppelnensis and Anomia sp. of the lower Turonian. Following by Hoplitoides sp. H . ingens , H . cf. lagiraldae , Codazziceras ospinae , Allocrioceras sp. that can be representing between the lower and middle Turonian. To the upper part of this segment were collected Prionocycloceras sp. P . guayabanum , Reesidites subtuberculatum , Subprionotropis colombianus , Mytiloides scupini , Dydimotis sp., Gauthiericeras sp., Anagaudryceras ? sp., Eulophoceras jacobi , Paralenticeras sieversi , Hauericeras
  • Upper Cenomanian–Lower Turonian Ammonoids from the Saxonian Cretaceous (Lower Elbtal Group, Saxony, Germany)

    Upper Cenomanian–Lower Turonian Ammonoids from the Saxonian Cretaceous (Lower Elbtal Group, Saxony, Germany)

    Upper CenomanianLower Turonian ammonoids from the Saxonian Cretaceous (lower Elbtal Group, Saxony, Germany) MARKUS WILMSEN & EMAD NAGM The Upper Cenomanian to Lower Turonian ammonoid fauna of the Saxonian Cretaceous (Elbtal Group, Saxony, Ger- many) has been revised based on the study of 270 specimens hosted in the Museum für Mineralogie und Geologie (MMG) of the Senckenberg Naturhistorische Sammlungen Dresden. In total, 12 species have been identified and, based on this revision, a number of ammonoids are now reported and/or illustrated for the first time from the Elbtal Group of Saxony: Euomphaloceras septemseriatum, Neocardioceras juddii barroisi, Watinoceras coloradoense, Spathites (Jeanrogericeras) reveliereanus, Sciponoceras gracile and Scaphites equalis. The study demonstrated the presence of all Upper Cenomanian and Lower Turonian standard ammonite biozones in the lithostratigraphic succession of the lower Elbtal Group: the lower Upper Cenomanian Calycoceras naviculare Zone (represented by the Oberhäslich For- mation), the mid- and upper Upper Cenomanian Metoicoceras geslinianum and Neocardioceras juddii zones (repre- sented by the Dölzschen Formation), and the Lower Turonian Watinoceras coloradoense and Mammites nodosoides zones (represented by the Brießnitz Formation). The ammonoid fauna from the Saxonian Cretaceous is dominated by strongly ornamented and widely distributed Acanthoceratidae. • Key words: Upper Cretaceous, Saxo-Bohemian Creta- ceous Basin, ammonites, taxonomic revision, biostratigraphy. WILMSEN,M.&NAGM, E. 2013. Upper Cenomanian–Lower Turonian ammonoids from the Saxonian Cretaceous (lower Elbtal Group, Saxony, Germany). Bulletin of Geosciences 88(3), 647–674 (18 figures). Czech Geological Sur- vey, Prague. ISSN 1214-1119. Manuscript received September 26, 2012; accepted in revised form January 25, 2013; published online July 3, 2013; issued July 3, 2013.
  • Stratigraphy and Biostratigraphy of an Upper Cretaceous Outlier Near Roy, Harding County, New Mexico

    Stratigraphy and Biostratigraphy of an Upper Cretaceous Outlier Near Roy, Harding County, New Mexico

    New Mexico Geological Society Guidebook, 52nd Field Conference, Geology ofthe Llano Estacado, 2001 251 STRATIGRAPHY AND BIOSTRATIGRAPHY OF AN UPPER CRETACEOUS OUTLIER NEAR ROY, HARDING COUNTY, NEW MEXICO SPENCER G. LUCASI AND ANDREW B. HECKERT2 INew Mexico Museum of Natural History, 1801 Mountain Rd NW, Albuquerque, 87104; 2Department of Earth and Planetary Sciences, University of New Mexico, Albuquerque, NM 87131-1116 Abstract.-Upper Cretaceous strata exposed as outliers near Roy in Harding County, New Mexico, are assigned to the Graneros Shale and the overlying Greenhorn Formation. The Greenhorn Formation locally consists of three members (in ascending order): Lincoln, Hartland, and Bridge Creek. The Lincoln Member is 8.3 m thick and dominated by yellowish gray and very pale orange calcareous shale and characteristic persistent beds of calcarenite. The Hartland Member is 11.0 m thick and consists mostly of medium and brownish gray bentonitic shale. The Bridge Creek Member here is erosionally truncated by the Neogene Ogallala Formation 4.1 m above its base and consists of interbeds ofledge­ forming limestone and calcareous shale. Fossils from the Lincoln Member include numerous specimens of the bivalve Ostrea beloiti Logan and of the selachian Ptychodus anonymus Williston. The Hartland Member lacks biostratigraphic ally significant fossils. The Bridge Creek Member produces the ammonites Euomphaloceras sp. and Sciponoceras gracile (Shumard) near its base and Watinoceras coloradoense (Henderson) and Vascoceras birchbyi Cobban and Scott near its top. These fossils can be assigned to the upper Cenomanian Sciponoceras gracile ammonite zone and the lower Turonian Vascoceras birchbyi ammonite zone. Younger ammonite zones normally present in the Bridge Creek Member are not present at Roy, having been stripped offby Neogene erosion.