DOCSLIB.ORG

Early Eocene) in the Northern Part of the Caspian Depression (Russia)

Total Page：16

File Type：pdf, Size：1020Kb

Download full-text PDF Read full-text
Early Eocene) in the Northern Part of the Caspian Depression (Russia) J. Nannoplankton Res. 37 (1), 2017, pp.67–76 © 2017 International Nannoplankton Association 67 ISSN 1210-8049 Printed by The Sheridan Press, USA A new species of the genus Chiphragmalithus from the Ypresian stage (early Eocene) in the northern part of the Caspian Depression (Russia) Vladimir A. Musatov The Lower Volga Scientific Research Institute for Geology and Geophysics Russia, 410600 Saratov, 70 Moskovskaya st.; [email protected] Manuscript received 19th November, 2015; revised manuscript accepted 25th March, 2017 Abstract The formal description is provided for a new taxon, Chiphragmalithus muzylevii sp. nov., from the early Eocene beds penetrated by the Novouzensk №1 key borehole in the northern part of the Caspian Depression. This species is confined to a narrow stratigraphic range and, therefore, possesses good potential for high resolution biostratigraphy and for accurate dating of the Ypresian sedimentary masses in the Northern hemisphere. Keywords nannofossils, new taxon, Lower Eocene, Ypresian stage, Caspian Depression, Russia, Chiphragmolithus 1. Introduction in the northern part of the Caspian Depression within the Deposits of Ypresian age occur over wide areas of Crimea, 568–405m interval (Figures 1, 2). The lower part of the North Caucasia, in the south of the Russian Platform, in section (568–475m interval) is represented by a member the Caspian Depression and the Turan Plate (Figure 1). of interbedded clays (greenish-gray, non-calacreous) and Their age is most accurately determined from foraminifer sandstones (glauconite-quartzose, clayey, noncalcareous). assemblages, calcareous nannofossils and dinoflagellates. No calcareous nannofossils have been detected in this The most complete data on calcareous nannoplankton lower interval. The age has been determined from Vasilye- complexes is presented in papers by Muzylev (1980, va’s dinoflagellate assemblages (2008, 2010). Zones from 1994), Musatov (1996), Vasil’eva & Musatov (2008, D5a to the lowermost of the D7c on the Luterbacher scale 2010, 2012), Shcherbinina et al. (2014), Bugrova et al. have been identified there. (2002) and King et al. (2013). The associations are gen- The upper part of the section in the 475–414m interval erally characterized by good preservation and a large is represented by a member of interbedding clays (green- number of species. Over the major part of the territory, the ish light gray, calcareous) with interlayers of sandstones deposits are represented by marine facies – clays of vari- and siltstones (glauconite quartzose, calcareous, clayey). able carbonate content, marls and limestones. According Interlayers of brown clays occur in the 436–428m inter- to Zachos et al. (2001), this interval corresponds to the val, with substantial contents of brown organic matter in Early Eocene Climatic Optimum (EECO), which provides the form of small amorphous “drops”. A certain amount good paleontologic grounding for age determination and of pollen has been encountered, as well as small roundish position in the general stratigraphic scale. grains (unicellular algae?), dinoflagellate fragments, and Though the genus Chiphragmalithus Bramlette & amorphous clots. Muzylev (1994) believes that accumula- Sullivan (1961) has been known for nearly 60 years, only tion of sediments with high organic matter content may be six species have been described up to the present time: associated with anoxic environments in the near-bottom Chiphragmalithus acanthodes Bramlette & Sullivan zone and may correspond to the “Ypresian sapropelite” 1961, Chiphragmalithus calathus Bramlette & Sullivan level described by Muzylev (1980, 1994) from the sec- 1961, Chiphragmalithus barbatus Perch-Nielsen 1984, tions in the North Caucasia, and by Steurbaut (2011) and Chiphragmalithus altinlii Varol 1989, Chiphragmalithus King et al. (2013) from the sections in the Aktulagay armatus Perch-Nielsen 1971, Chiphragmalithus van- Plateau (West Kazakhstan). denberghei Steurbaut 2011, and four of these - Ch. acan- In the 420–411m interval, the carbonate content in the thodes, Ch. calathus, Ch. barbatus and Ch. altinli – are section increases and the section is represented by highly probably synonymous. carbonate clays and marls (See Figure 2). Zones NP12 and Discovery of a new species, Chiphragmalithus muzylevii NP13 of the standard Martini zonation (1971) or CP10 and sp. nov., within a short stratigraphic interval will allow more CP11 of the Okada & Bukry zonation (1980) have been accurate correlations of remote Ypresian sections. recognized with a reasonable level of confidence in that part of the section. According to dinoflagellates, the inter- 2. Materials val corresponds to the uppermost of the D7 zone and to The studied materials consist of samples selected from the D8 zone. the Ypresian and lowest Lutetian beds penetrated by the A member of noncarbonated sandy clay and clayey Novouzensk №1 key borehole (50.4583°N, 48.0200°E) siltstones occurs higher in the 411–405m interval; no 68 Musatov nannofossils have been found. The lowermost part of the the ready “smears” were 40–50х25mm if the sediment D9 zone has been determined from dinoflagellates. The was of low nannofossil abundance, and 20–30х25mm in total thickness of the Ypresian beds is about 160m. cases of marls and soft coccolith chalk. After the fairly In the 405–400m interval, greenish light gray marls quick volatilization of alcohol, some immersion liquid, occur, highly sandy in the lower part of the interval, with Immersol 518N, was added and the slide was placed on large amounts of glauconite and rare phosphorite gravel the specimen stage of the light microscope, a Zeiss Axio grains. This part of the section corresponds to the upper- Lab.A1. No coverslips were used. Examination was made most of the NP14 zone or to the CP12b subzone. Those with a х100 Plan-NEOFLUAR objective lens, and х10–15 are overlain with low siltstone greenish marls grading into occular lenses. Nannofossils were examined and photo- white marls (soft coccolith chalk) higher in the section. graphed in transmitted normal and polarized light with a This part of the section corresponds to the base of the Canon-1000D digital camera. The images were processed NP15 zone and to the base of the CP13a subzone. with AxioVision Rel.4.8 software product. The Electronic Practically all the described species of the Chiphrag- Calcareous Nannofossils: BugCam-NannoWare [Version malithus genus have been encountered in the upper part of 2002.12.1] (2002) electronic database was used for spe- the Ypresian clay unit (420–411m interval). In addition, a cies determinations, as well as the accessible electronic further, very distinctive morphotype has been found and is database of nannoplankton images, inclusive of index spe- described herein as Chiphragmalithus muzyleuvii sp. nov. cies and holotypes, of the Nannotax3 website (2014). The The species was first encountered at the depth of 416m biostratigraphic division of the section was based on the and was traced up to 411m. standard Paleogene NP calcareous nannofossil zonation of Martini (1971) and on the CP zonal scale of Okada & 3. Methods Bukry (1980) The core samples analyzed for nannofossils were selected Taxonomy was adopted from Perch-Nielsen (1985) by the author at a sampling frequency of 1.0–0.2m. In and Nannotax3. Only taxonomic references not included the upper, fossiliferous part of the section, samples were in these resources are provided herein. The author of the selected at 0.2–0.05m intervals. For nannofossil exam- present paper keeps the examined samples and original inations, temporary whole mounts were prepared by the photos. method described by Bown & Young (1998), with certain modifications: small amounts of rock powder were scraped 4. Systematic palaeontology with a needle off a clean sample surface to the object To provide a better understanding for recognizing the new plate; two or three drops of ethyl alcohol were added, the taxon, Chiphragmolithus muzylevii sp. nov., we briefly alcohol suspension was accurately distributed over the discuss the most characteristic features of species within object plate surface with a wooden needle. The sizes of the genera Chiphragmalithus Bramlette & Sullivan, 1961, A N B Russia Sweden Novouzensk Norway Finland Russia Novouzensk №1 Baltic Sea Estonia Latvia North Sea Moscow United Denmark Lithuania Kingdom Poland Belarus Netherland B . Kazachstan Germany Belgium olga Riv Czechia V Novouzensk №1 Slovakia Ukrain Kazachstan Moldova Austria Hungary France Romania Croatia Serbia Italy Black Sea Georgia Bulgaria Sea Caspian Uzbekistan Azerbaijan Spain Greece Turkey Turkmenistan Syria Mediterranean Sea Tunisia Lebanon Afganistan Iraq Iran Figure 1: A) Regional and B) local site maps of Novouzensk №1 borehole A new species of the genus Chiphragmolithus… 69 Novouzensk key borehole Nannoplankton Bioevents Dinocyst Bioevents ghei Vasilyeva O., This study Musatov V. , 1980 2012, emend. 400 N. fulgens Martini, 1971 Okada & C. bucina Samples et al., 2012 CP Bukry Formation Dinocyst zones k2 Vandenberghe NP C. bucina Stage Lithology D. parcilimbatum Depth, m 1a D.parcilimbatum 1 1a B. inflatus 15a 13a d W. eocaenica 400 405 14b 12b b-c 405 W. eocaenica D. sublodoensis D9 A. diktyoplokum 1b Barren a 405 1c N. cristata W. coronata 2 Lutetian 414 16 Barren Kopterek 410 13 11 Ch. columna 19 D8 O. romanum 420 5 20 A. diktyoplokum 1d D. cruciformis Chiphragmalithus vandenber 6 438 414 Ch. muzylevii D. politum W. coronata 2a 12 10 460 16 H.lophota . 475 Ch. columna 3 D7c 78 S.acervus T.crass. D. varielongitudum 420 4 D. lodoensis sp. nov presian 486 Ch. aff.clathrata T. orthostylus Y 425 H. seminulum 486 Neococcolithes minutus Bostandyk D. oebisfeldensis 428 b 500 430 D. oebisfeldensis omanum 4b Barren A. augustum D5 523 O. r D. oebisfeldensis a 435 A. augustum M. mirabilis Barren 560 A. parvum 5438 A. quinquelatum 440 W. pechoricum 572 Chiphragmalithus muzylevii c Ch. coleothrypta 445 621 A. homomorphum D4 635 A. hyperacanthum 664 450 Thanetian 672 b Novouzensk 455 A. margarita 6 5 H. kleinpelli * * D.politum 721 I.? viborgense 747 Ch. bidens 460 772 5 4 F. tympaniformis S. densispinatum L. janii L. ulii 465 Selandian U.
Load more

Recommended publications
  • A Window Into Paleocene to Early Eocene Depositional History in Egypt Basedoncoccolithstratigraphy
    The Dababiya Core: A window into Paleocene to Early Eocene depositional history in Egypt basedoncoccolithstratigraphy Marie-Pierre Aubry1 and Rehab Salem1,2 1Department of Earth and Planetary Sciences, Rutgers University, 610 Taylor Road, NJ 08854-8066, USA email: [email protected] 2Geology Department, Faculty of Science, Tanta University, 31527, Tanta, Egypt [email protected] ABSTRACT: The composite Paleocene-lower Eocene Dababiya section recovered in the Dababiya Quarry core and accessible in out- crop in the Dababiya Quarry exhibits an unexpected contrast in thickness between the Lower Eocene succession (~Esna Shales) and the Paleocene one (~Dakhla Shales and Tarawan Chalk). We investigate the significance of this contrast by reviewing calcareous nannofossil stratigraphic studies performed on sections throughout Egypt. We show that a regional pattern occurs, and distinguish six areas—Nile Valley, Eastern Desert and western Sinai, Central and eastern Sinai, northern Egypt and Western Desert. Based on patterns related to thicknesses of selected lithobiostratigraphic intervals and distribution of main stratigraphic gaps, we propose that the differences in the stratigraphic architecture between these regions result from differential latest Paleocene and Early Eocene subsidence following intense Middle to Late Paleocene tectonic activity in the Syrian Arc folds as a result of the closure of the Neo-Tethys. INTRODUCTION view of coccolithophore studies in Egypt since their inception During the Late Cretaceous and Early Paleogene Egypt was (1968). Coccolith-bearing sedimentary rocks as old as part of a vast epicontinental shelf at the edge of the southern Cenomanian outcrop in central Sinai (Thamed area; Bauer et al. Tethys (text-fig. 1). Bounded by the Arabian-Nubian craton to 2001; Faris and Abu Shama 2003).
    [Show full text]
  • Climatic Shifts Drove Major Contractions in Avian Latitudinal Distributions Throughout the Cenozoic
    Climatic shifts drove major contractions in avian latitudinal distributions throughout the Cenozoic Erin E. Saupea,1,2, Alexander Farnsworthb, Daniel J. Luntb, Navjit Sagooc, Karen V. Phamd, and Daniel J. Fielde,1,2 aDepartment of Earth Sciences, University of Oxford, OX1 3AN Oxford, United Kingdom; bSchool of Geographical Sciences, University of Bristol, Clifton, BS8 1SS Bristol, United Kingdom; cDepartment of Meteorology, Stockholm University, 106 91 Stockholm, Sweden; dDivision of Geological and Planetary Sciences, Caltech, Pasadena, CA 91125; and eDepartment of Earth Sciences, University of Cambridge, CB2 3EQ Cambridge, United Kingdom Edited by Nils Chr. Stenseth, University of Oslo, Oslo, Norway, and approved May 7, 2019 (received for review March 8, 2019) Many higher level avian clades are restricted to Earth’s lower lati- order avian historical biogeography invariably recover strong evi- tudes, leading to historical biogeographic reconstructions favoring a dence for an origin of most modern diversity on southern land- Gondwanan origin of crown birds and numerous deep subclades. masses (2, 6, 11). However, several such “tropical-restricted” clades (TRCs) are repre- The crown bird fossil record has unique potential to reveal sented by stem-lineage fossils well outside the ranges of their clos- where different groups of birds were formerly distributed in deep est living relatives, often on northern continents. To assess the time. Fossil evidence, for example, has long indicated that total- drivers of these geographic disjunctions, we combined ecological group representatives of clades restricted to relatively narrow niche modeling, paleoclimate models, and the early Cenozoic fossil geographic regions today were formerly found in different parts of record to examine the influence of climatic change on avian geo- – graphic distributions over the last ∼56 million years.
    [Show full text]
  • Late Cretaceous–Eocene Geological Evolution of the Pontides Based on New Stratigraphic and Palaeontologic Data Between the Black Sea Coast and Bursa (NW Turkey)
    Turkish Journal of Earth Sciences (Turkish J. Earth Sci.), Vol.Z. ÖZCAN 21, 2012, ET pp. AL. 933–960. Copyright ©TÜBİTAK doi:10.3906/yer-1102-8 First published online 25 April 2011 Late Cretaceous–Eocene Geological Evolution of the Pontides Based on New Stratigraphic and Palaeontologic Data Between the Black Sea Coast and Bursa (NW Turkey) ZAHİDE ÖZCAN1, ARAL I. OKAY1,2, ERCAN ÖZCAN2, AYNUR HAKYEMEZ3 & SEVİNÇ ÖZKAN-ALTINER4 1 İstanbul Technical University (İTÜ), Eurasia Institute of Earth Sciences, Maslak, TR−34469 İstanbul, Turkey (E-mail: [email protected]) 2 İstanbul Technical University (İTÜ), Faculty of Mines, Department of Geology, Maslak, TR−34469 İstanbul, Turkey 3 General Directorate of Mineral Research and Exploration (MTA Genel Müdürlüğü), Geological Research Department, TR−06520 Ankara, Turkey 4 Middle East Technical University (METU), Department of Geological Engineering, Ünversiteler Mahallesi, Dumlupınar Bulvarı No. 1, TR−06800 Ankara, Turkey Received 17 February 2011; revised typescript receipt 04 April 2011; accepted 25 April 2011 Abstract: Th e Late Cretaceous–Eocene geological evolution of northwest Turkey between the Black Sea and Bursa was studied through detailed biostratigraphic characterization of eleven stratigraphic sections. Th e Upper Cretaceous sequence in the region starts with a major marine transgression and lies unconformably on a basement of Palaeozoic and Triassic rocks in the north (İstanbul-type basement) and on metamorphic rocks and Jurassic sedimentary rocks in the south (Sakarya-type basement). Four megasequences have been diff erentiated in the Late Cretaceous–Eocene interval. Th e fi rst one, of Turonian to Late Campanian age, is represented by volcanic and volcanoclastic rocks in the north along the Black Sea coast, and by siliciclastic turbidites and intercalated calcarenites in the south, corresponding to magmatic arc basin and fore-arc basin, respectively.
    [Show full text]
  • Redalyc.Palynology of Lower Palaeogene (Thanetian-Ypresian
    Geologica Acta: an international earth science journal ISSN: 1695-6133 [email protected] Universitat de Barcelona España TRIPATHI, S.K.M.; KUMAR, M.; SRIVASTAVA, D. Palynology of Lower Palaeogene (Thanetian-Ypresian) coastal deposits from the Barmer Basin (Akli Formation, Western Rajasthan, India): Palaeoenvironmental and palaeoclimatic implications Geologica Acta: an international earth science journal, vol. 7, núm. 1-2, marzo-junio, 2009, pp. 147- 160 Universitat de Barcelona Barcelona, España Available in: http://www.redalyc.org/articulo.oa?id=50513109009 How to cite Complete issue Scientific Information System More information about this article Network of Scientific Journals from Latin America, the Caribbean, Spain and Portugal Journal's homepage in redalyc.org Non-profit academic project, developed under the open access initiative Geologica Acta, Vol.7, Nos 1-2, March-June 2009, 147-160 DOI: 10.1344/105.000000275 Available online at www.geologica-acta.com Palynology of Lower Palaeogene (Thanetian-Ypresian) coastal deposits from the Barmer Basin (Akli Formation, Western Rajasthan, India): Palaeoenvironmental and palaeoclimatic implications S.K.M. TRIPATHI M. KUMAR and D. SRIVASTAVA Birbal Sahni Institute of Palaeobotany 53, University Road, Lucknow, 226007, India. Tripathi E-mail: [email protected] Kumar E-mail: [email protected] Srivastava E-mail: [email protected] ABSTRACT The 32-m thick sedimentary succession of the Paleocene-Eocene Akli Formation (Barmer basin, Rajasthan, India), which is exposed in an open-cast lignite mine, interbed several lignite seams that alternate with fossilif- erous carbonaceous clays, green clays and widespread siderite bands and chert nodules. The palynofloral assemblages consist of spore, pollen and marine dinoflagellate cysts that indicate a Thanetian to Ypresian age.
    [Show full text]
  • Early Eocene Sediments of the Western Crimean Basin, Ukraine 100 ©Geol
    ZOBODAT - www.zobodat.at Zoologisch-Botanische Datenbank/Zoological-Botanical Database Digitale Literatur/Digital Literature Zeitschrift/Journal: Berichte der Geologischen Bundesanstalt Jahr/Year: 2011 Band/Volume: 85 Autor(en)/Author(s): Khoroshilova Margarita A., Shcherbinina E. A. Artikel/Article: Sea-level changes and lithological architecture of the Paleocene - early Eocene sediments of the western Crimean basin, Ukraine 100 ©Geol. Bundesanstalt, Wien; download unter www.geologie.ac.at Berichte Geol. B.-A., 85 (ISSN 1017-8880) – CBEP 2011, Salzburg, June 5th – 8th Sea-level changes and lithological architecture of the Paleocene- early Eocene sediments of the western Crimean basin, Ukraine Margarita A. Khoroshilova1, E.A. Shcherbinina2 1 Geological Department of the Moscow State University ([email protected]) 2 Geological Institute of the Russian Academy of Sciences, Moscow, Russia During the Paleogene time, sedimentary basin of the western Crimea, Ukraine was bordered by land of coarse topography, which occupied the territory of modern first range of the Crimean Mountains, on the south and by Simferopol uplift on the north and displays a wide spectrum of shallow water marine facies. Paleocene to early Eocene marine deposits are well preserved and can be studied in a number of exposures. Correlated by standard nannofossil scale, five exposures present a ~17 Ma record of sea- level fluctuations. Danian, Selandian-Thanetian and Ypresian transgressive-regressive cycles are recognized in the sections studied. Major sea-level falls corresponding to hiatuses at the Danian/Selandian and Thanetian/Ypresian boundaries appear as hard-ground surfaces. Stratigraphic range of the first hiatus is poorly understood because Danian shallow carbonates are lack in nannofossils while accumulation of Selandian marl begins at the NP6.
    [Show full text]
  • Mesozoic and Cenozoic Sequence Stratigraphy of European Basins
    Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3789969/9781565760936_frontmatter.pdf by guest on 26 September 2021 Downloaded from http://pubs.geoscienceworld.org/books/book/chapter-pdf/3789969/9781565760936_frontmatter.pdf by guest on 26 September 2021 MESOZOIC AND CENOZOIC SEQUENCE STRATIGRAPHY OF EUROPEAN BASINS PREFACE Concepts of seismic and sequence stratigraphy as outlined in To further stress the importance of well-calibrated chronos- publications since 1977 made a substantial impact on sedimen- tratigraphic frameworks for the stratigraphic positioning of geo- tary geology. The notion that changes in relative sea level shape logic events such as depositional sequence boundaries in a va- sediment in predictable packages across the planet was intui- riety of depositional settings in a large number of basins, the tively attractive to many sedimentologists and stratigraphers. project sponsored a biostratigraphic calibration effort directed The initial stratigraphic record of Mesozoic and Cenozoic dep- at all biostratigraphic disciplines willing to participate. The re- ositional sequences, laid down in response to changes in relative sults of this biostratigraphic calibration effort are summarized sea level, published in Science in 1987 was greeted with great, on eight charts included in this volume. albeit mixed, interest. The concept of sequence stratigraphy re- This volume also addresses the question of cyclicity as a ceived much acclaim whereas the chronostratigraphic record of function of the interaction between tectonics, eustasy, sediment Mesozoic and Cenozoic sequences suffered from a perceived supply and depositional setting. An attempt was made to estab- absence of biostratigraphic and outcrop documentation. The lish a hierarchy of higher order eustatic cycles superimposed Mesozoic and Cenozoic Sequence Stratigraphy of European on lower-order tectono-eustatic cycles.
    [Show full text]
  • Pickford 2018 Namahyrax Corvus from Black Crow, Sperrgebiet
    Additional material of Namahyrax corvus from the Ypresian/Lutetian of Black Crow, Namibia Martin PICKFORD Sorbonne Universités (CR2P, MNHN, CNRS, UPMC - Paris VI) 8, rue Buffon, 75005, Paris, France ([email protected]) Abstract : Three teeth of a small hyracoid were found during the 2017 campaign of acid digestion of blocks of limestone from Black Crow, Namibia. The specimens, a left D1/, half an upper premolar and a right p/1 can be attributed with confidence to Namahyrax corvus , up to now the only hyracoid known from the site. The D1/ is more complete than the broken P1/ in the holotype and yields additional information about the crown morphology of the anterior cheek teeth. The p/1 was not previously known for the species. The three teeth underscore the primitive brachyodont morphology of the teeth. The teeth are somewhat more primitive than the corresponding teeth in Dimaitherium patnaiki from the Fayum, Egypt. Direct comparisons cannot be made with Seggeurius amourensis and Bunohyrax matsumotoi because these tooth positions are unknown in these species, but the shape of the p/1 of Namahyrax corresponds with what would be expected from the p/2 morphology in them. Comparisons with Microhyrax lavocati are difficult to make because not even the p/2 is known in that species, but the simplicity of its p/3 (lack of crescentic cusps) suggests a ground plan for the p/1 that could correspond to that observed in the Black Crow specimen. The new specimens of Namahyrax resolve the uncertainty concerning its familial status, indicating that it belongs to the family Geniohyidae.
    [Show full text]
  • Offshore Marine Actinopterygian Assemblages from the Maastrichtian–Paleogene of the Pindos Unit in Eurytania, Greece
    Offshore marine actinopterygian assemblages from the Maastrichtian–Paleogene of the Pindos Unit in Eurytania, Greece Thodoris Argyriou1 and Donald Davesne2,3 1 UMR 7207 (MNHN—Sorbonne Université—CNRS) Centre de Recherche en Paléontologie, Museum National d’Histoire naturelle, Paris, France 2 Department of Earth Sciences, University of Oxford, Oxford, UK 3 UMR 7205 (MNHN—Sorbonne Université—CNRS—EPHE), Institut de Systématique, Évolution, Biodiversité, Museum National d’Histoire naturelle, Paris, France ABSTRACT The fossil record of marine ray-finned fishes (Actinopterygii) from the time interval surrounding the Cretaceous–Paleogene (K–Pg) extinction is scarce at a global scale, hampering our understanding of the impact, patterns and processes of extinction and recovery in the marine realm, and its role in the evolution of modern marine ichthyofaunas. Recent fieldwork in the K–Pg interval of the Pindos Unit in Eurytania, continental Greece, shed new light on forgotten fossil assemblages and allowed for the collection of a diverse, but fragmentary sample of actinopterygians from both late Maastrichtian and Paleocene rocks. Late Maastrichtian assemblages are dominated by Aulopiformes (†Ichthyotringidae, †Enchodontidae), while †Dercetidae (also Aulopiformes), elopomorphs and additional, unidentified teleosts form minor components. Paleocene fossils include a clupeid, a stomiiform and some unidentified teleost remains. This study expands the poor record of body fossils from this critical time interval, especially for smaller sized taxa, while providing a rare, paleogeographically constrained, qualitative glimpse of open-water Tethyan ecosystems from both before and after the extinction event. Faunal similarities Submitted 21 September 2020 Accepted 9 December 2020 between the Maastrichtian of Eurytania and older Late Cretaceous faunas reveal a Published 20 January 2021 higher taxonomic continuum in offshore actinopterygian faunas and ecosystems Corresponding author spanning the entire Late Cretaceous of the Tethys.
    [Show full text]
  • Paleogeographic Maps Earth History
    History of the Earth Age AGE Eon Era Period Period Epoch Stage Paleogeographic Maps Earth History (Ma) Era (Ma) Holocene Neogene Quaternary* Pleistocene Calabrian/Gelasian Piacenzian 2.6 Cenozoic Pliocene Zanclean Paleogene Messinian 5.3 L Tortonian 100 Cretaceous Serravallian Miocene M Langhian E Burdigalian Jurassic Neogene Aquitanian 200 23 L Chattian Triassic Oligocene E Rupelian Permian 34 Early Neogene 300 L Priabonian Bartonian Carboniferous Cenozoic M Eocene Lutetian 400 Phanerozoic Devonian E Ypresian Silurian Paleogene L Thanetian 56 PaleozoicOrdovician Mesozoic Paleocene M Selandian 500 E Danian Cambrian 66 Maastrichtian Ediacaran 600 Campanian Late Santonian 700 Coniacian Turonian Cenomanian Late Cretaceous 100 800 Cryogenian Albian 900 Neoproterozoic Tonian Cretaceous Aptian Early 1000 Barremian Hauterivian Valanginian 1100 Stenian Berriasian 146 Tithonian Early Cretaceous 1200 Late Kimmeridgian Oxfordian 161 Callovian Mesozoic 1300 Ectasian Bathonian Middle Bajocian Aalenian 176 1400 Toarcian Jurassic Mesoproterozoic Early Pliensbachian 1500 Sinemurian Hettangian Calymmian 200 Rhaetian 1600 Proterozoic Norian Late 1700 Statherian Carnian 228 1800 Ladinian Late Triassic Triassic Middle Anisian 1900 245 Olenekian Orosirian Early Induan Changhsingian 251 2000 Lopingian Wuchiapingian 260 Capitanian Guadalupian Wordian/Roadian 2100 271 Kungurian Paleoproterozoic Rhyacian Artinskian 2200 Permian Cisuralian Sakmarian Middle Permian 2300 Asselian 299 Late Gzhelian Kasimovian 2400 Siderian Middle Moscovian Penn- sylvanian Early Bashkirian
    [Show full text]
  • 2009 Geologic Time Scale Cenozoic Mesozoic Paleozoic Precambrian Magnetic Magnetic Bdy
    2009 GEOLOGIC TIME SCALE CENOZOIC MESOZOIC PALEOZOIC PRECAMBRIAN MAGNETIC MAGNETIC BDY. AGE POLARITY PICKS AGE POLARITY PICKS AGE PICKS AGE . N PERIOD EPOCH AGE PERIOD EPOCH AGE PERIOD EPOCH AGE EON ERA PERIOD AGES (Ma) (Ma) (Ma) (Ma) (Ma) (Ma) (Ma) HIST. HIST. ANOM. ANOM. (Ma) CHRON. CHRO HOLOCENE 65.5 1 C1 QUATER- 0.01 30 C30 542 CALABRIAN MAASTRICHTIAN NARY PLEISTOCENE 1.8 31 C31 251 2 C2 GELASIAN 70 CHANGHSINGIAN EDIACARAN 2.6 70.6 254 2A PIACENZIAN 32 C32 L 630 C2A 3.6 WUCHIAPINGIAN PLIOCENE 260 260 3 ZANCLEAN 33 CAMPANIAN CAPITANIAN 5 C3 5.3 266 750 NEOPRO- CRYOGENIAN 80 C33 M WORDIAN MESSINIAN LATE 268 TEROZOIC 3A C3A 83.5 ROADIAN 7.2 SANTONIAN 271 85.8 KUNGURIAN 850 4 276 C4 CONIACIAN 280 4A 89.3 ARTINSKIAN TONIAN C4A L TORTONIAN 90 284 TURONIAN PERMIAN 10 5 93.5 E 1000 1000 C5 SAKMARIAN 11.6 CENOMANIAN 297 99.6 ASSELIAN STENIAN SERRAVALLIAN 34 C34 299.0 5A 100 300 GZELIAN C5A 13.8 M KASIMOVIAN 304 1200 PENNSYL- 306 1250 15 5B LANGHIAN ALBIAN MOSCOVIAN MESOPRO- C5B VANIAN 312 ECTASIAN 5C 16.0 110 BASHKIRIAN TEROZOIC C5C 112 5D C5D MIOCENE 320 318 1400 5E C5E NEOGENE BURDIGALIAN SERPUKHOVIAN 326 6 C6 APTIAN 20 120 1500 CALYMMIAN E 20.4 6A C6A EARLY MISSIS- M0r 125 VISEAN 1600 6B C6B AQUITANIAN M1 340 SIPPIAN M3 BARREMIAN C6C 23.0 345 6C CRETACEOUS 130 M5 130 STATHERIAN CARBONIFEROUS TOURNAISIAN 7 C7 HAUTERIVIAN 1750 25 7A M10 C7A 136 359 8 C8 L CHATTIAN M12 VALANGINIAN 360 L 1800 140 M14 140 9 C9 M16 FAMENNIAN BERRIASIAN M18 PROTEROZOIC OROSIRIAN 10 C10 28.4 145.5 M20 2000 30 11 C11 TITHONIAN 374 PALEOPRO- 150 M22 2050 12 E RUPELIAN
    [Show full text]
  • Astronomical Calibration of the Ypresian Timescale: Implications for Seafloor Spreading Rates and the Chaotic Behavior of the Solar System?
    Clim. Past, 13, 1129–1152, 2017 https://doi.org/10.5194/cp-13-1129-2017 © Author(s) 2017. This work is distributed under the Creative Commons Attribution 3.0 License. Astronomical calibration of the Ypresian timescale: implications for seafloor spreading rates and the chaotic behavior of the solar system? Thomas Westerhold1, Ursula Röhl1, Thomas Frederichs2, Claudia Agnini3, Isabella Raffi4, James C. Zachos5, and Roy H. Wilkens6 1MARUM – Center for Marine Environmental Sciences, University of Bremen, Leobener Straße, 28359 Bremen, Germany 2Faculty 5 Geosciences, University of Bremen, 28359 Bremen, Germany 3Dipartimento di Geoscienze, Università degli Studi di Padova, via G. Gradenigo 6, 35131 Padua, Italy 4Dipartimento di Ingegneria e Geologia (InGeo) – CeRSGeo, Universitaà degli Studi “G. d’Annunzio” Chieti-Pescara, via dei Vestini 31, 66013 Chieti-Pescara, Italy 5Department of Earth and Planetary Sciences, University of California Santa Cruz, 1156 High Street, Santa Cruz, CA 95064, USA 6Institute of Geophysics and Planetology, University of Hawai’i, Honolulu, HI 96822, USA Correspondence to: Thomas Westerhold ([email protected]) Received: 8 February 2017 – Discussion started: 10 February 2017 Revised: 24 July 2017 – Accepted: 7 August 2017 – Published: 11 September 2017 Abstract. To fully understand the global climate dynamics solution for eccentricity, which was used as a target curve of the warm early Eocene with its reoccurring hyperthermal for compiling the Ypresian astronomical timescale (YATS). events, an accurate high-fidelity age model is required. The The consistent positions of the very long eccentricity minima Ypresian stage (56–47.8 Ma) covers a key interval within the in the geological data and the La2010b solution suggest that Eocene as it ranges from the warmest marine temperatures in the macroscopic feature displaying the chaotic diffusion of the early Eocene to the long-term cooling trends in the mid- the planetary orbits, the transition from libration to circula- dle Eocene.
    [Show full text]
  • Alphabetical List
    LIST E - GEOLOGIC AGE (STRATIGRAPHIC) TERMS - ALPHABETICAL LIST Age Unit Broader Term Age Unit Broader Term Aalenian Middle Jurassic Brunhes Chron upper Quaternary Acadian Cambrian Bull Lake Glaciation upper Quaternary Acheulian Paleolithic Bunter Lower Triassic Adelaidean Proterozoic Burdigalian lower Miocene Aeronian Llandovery Calabrian lower Pleistocene Aftonian lower Pleistocene Callovian Middle Jurassic Akchagylian upper Pliocene Calymmian Mesoproterozoic Albian Lower Cretaceous Cambrian Paleozoic Aldanian Lower Cambrian Campanian Upper Cretaceous Alexandrian Lower Silurian Capitanian Guadalupian Algonkian Proterozoic Caradocian Upper Ordovician Allerod upper Weichselian Carboniferous Paleozoic Altonian lower Miocene Carixian Lower Jurassic Ancylus Lake lower Holocene Carnian Upper Triassic Anglian Quaternary Carpentarian Paleoproterozoic Anisian Middle Triassic Castlecliffian Pleistocene Aphebian Paleoproterozoic Cayugan Upper Silurian Aptian Lower Cretaceous Cenomanian Upper Cretaceous Aquitanian lower Miocene *Cenozoic Aragonian Miocene Central Polish Glaciation Pleistocene Archean Precambrian Chadronian upper Eocene Arenigian Lower Ordovician Chalcolithic Cenozoic Argovian Upper Jurassic Champlainian Middle Ordovician Arikareean Tertiary Changhsingian Lopingian Ariyalur Stage Upper Cretaceous Chattian upper Oligocene Artinskian Cisuralian Chazyan Middle Ordovician Asbian Lower Carboniferous Chesterian Upper Mississippian Ashgillian Upper Ordovician Cimmerian Pliocene Asselian Cisuralian Cincinnatian Upper Ordovician Astian upper
    [Show full text]