DOCSLIB.ORG

N:\GSA\86180 Mar Bulletin\Azmy\Working Files

Total Page：16

File Type：pdf, Size：1020Kb

Download full-text PDF Read full-text
N:\GSA\86180 Mar Bulletin\Azmy\Working Files Silurian strontium isotope stratigraphy Karem Azmy* Ottawa-Carleton Geoscience Centre, University of Ottawa, Ottawa, Ontario K1N 6N5, Canada Jan Veizer Ottawa-Carleton Geoscience Centre, University of Ottawa, Ottawa, Ontario K1N 6N5, Canada, and Institut für Geologie, Ruhr Universität, 44780 Bochum, Germany Bernd Wenzel Institut für Geologie der Universität Erlangen-Nürnberg, 91054 Erlangen, Germany Michael G. Bassett Department of Geology, National Museum of Wales, Cardiff CF1 3NP, United Kingdom Paul Copper Department of Earth Sciences, Laurentian University, Sudbury, Ontario P3E 2C6, Canada ABSTRACT Burke et al., 1982; Veizer, 1989; McArthur, 1994), condition is that the temporal 87Sr/86Sr trends are to understand continental weathering processes characterized by steep slopes. This was the case A sample set of 164 calcitic brachiopod and mid-oceanic ridge hydrothermal circulation for several intervals of Phanerozoic time, and shells, covering the entire Silurian Period (~ 30 (cf. Hodell et al., 1990; Richter et al., 1992; Farrell particularly in Cenozoic time (e.g., Mead and m.y.) with a resolution of about 0.7 m.y., was et al., 1995), and to correlate and date marine sed- Hodell, 1995). collected from stratotype sections at Anticosti imentary rocks (e.g., Elderfield, 1986; Quinn et al., The main objectives of this study are to (1) re- Island (Canada), Wales (United Kingdom), 1991; McArthur, 1994). The dominant driving fine the Sr-isotope curve for the Silurian seawa- Gotland (Sweden), Podolia (Ukraine), Latvia, forces causing the changes in seawater isotopic ra- ter, (2) utilize such a refined curve for high-reso- and Lithuania. They show 87Sr/86Sr values tios are suggested to be (1) continental runoff and lution stratigraphic correlation, and (3) improve ranging from 0.707930 to 0.708792 that pro- ground-water runout, both of which supply radi- understanding of geochemical cycling for Sr dur- gressively increase with time. This may indicate ogenic strontium to the oceans, and (2) sea- ing Silurian time. an increasing riverine flux of radiogenic Sr into water–oceanic crust interaction, particularly hy- the ocean from weathering of continental sialic drothermal rift–related activities, supplying a GEOLOGICAL SETTING rocks due to progressive warming of the cli- less-radiogenic strontium (Palmer and Elderfield, mate. Exceptionally high increases in 87Sr/86Sr 1985). Other factors, such as diagenetic flux and The samples for this study were selected from values were observed in early Llandovery carbonate recycling, may account for a minor con- diverse depositional settings on different paleo- (Rhuddanian), late Llandovery (Telychian), tribution (Elderfield, 1986; Veizer, 1989). continents. Paleogeographic reconstructions (cf. and late Ludlow (Gorstian-Ludfordian bound- Low-Mg calcite brachiopod shells, particularly McKerrow et al., 1991) place all these basins ary) samples. Partial linear regressions, based if nonluminescent, have been documented to fre- within the tropical paleolatitudes and they in- on a stepwise climbing pattern, with local drops quently retain the primary Sr-isotope signals of clude Anticosti Island, Québec, Canada (Lauren- around the Llandovery-Wenlock boundary ambient seawater (Popp et al., 1986; Banner and tia), England, Sweden, Lithuania, Latvia, and and in latest Ludlow time, were used to esti- Kaufman, 1994; Diener et al., 1996). When bio- Podolia in the Ukraine (Baltica). The lithology mate relative ages with a resolution of about ±2 genic marine carbonate forms, the 87Sr/86Sr of of the studied sequences comprised mainly lime- biozones (~1.5–2 m.y.). The Sr-isotope curve ocean water is incorporated into its structure with- stones of shallow shelf environments, frequently shows distinct inflection points in earliest Wen- out fractionation. Oceanic uniformity of 87Sr/86Sr associated with reefs. The stratigraphic assign- lock and mid-PÍídolí time. These may be used at any given time is expected, because the resi- ment of these sections (Fig. 1) follows the global to correlate the Llandovery-Wenlock boundary dence time of Sr in the oceans (~ 106 yr) is much Silurian standard time scale. For further details in the United Kingdom, Gotland, and Lithua- longer than the time it takes for currents to mix the of geology and samples see Azmy (1996), Azmy nia, and the Kaugatuma-Ohesaare boundary oceans (Faure, 1986). However, for highly strati- et al. (1998), Wenzel and Joachimski (1996), and in the Baltic states and Podolia. fied oceans, the response may be different due to Wenzel (1997). possible mixing rates of bottom waters approach- INTRODUCTION ing the residence times for Sr in seawater METHODOLOGY (McArthur, 1994). Variations in seawater 87Sr/86Sr over geologic Variations in 87Sr/86Sr composition of past sea- The selected brachiopods were identified and time, particularly for Phanerozoic time, have been water, resolvable on a short-time scale of 107 to two identical slabs (~1.5 mm thick) were cut lon- used to reconstruct the evolutionary history of an- 106 yr, may be utilized for high-resolution strati- gitudinally through the umbo zone, using an cient seawater (e.g., Veizer and Compston, 1974; graphic correlations with an accuracy compara- ISOMET low-speed saw. The slabs were gently ble to, and perhaps higher than, that of biostratig- polished on a glass plate using Al2O3 powder *E-mail: [email protected]. raphy, the latter usually being 1 to 5 m.y. The (size 9.5 µm). A thin section of the sample, made Data Repository item 9933 contains additional material related to this article. GSA Bulletin; April 1999; v. 111; no. 4; p. 475–483; 7 figures; 3 tables. 475 AZMY ET AL. Graptolite Conodont Anticosti Is. Wales Gotland Podolia Kolka 54 Biozones Biozones CANADA BRITAIN SWEDEN UKRAINE LATVIA LITHUANIA 408.5 Ma 41 transgrediens ~ 40perneri detorta Dzwinogorod Ohesaare Jura 39bouceki 38lochkovensis ^ 37pridoliensis Rashkov Kaugatuma Minija PRIDOLI 36ultimus eosteinhornensis 411 Ma 35parultimus Sundre Prigorodok 34balticus/codatus Hamra 33kozlowski snajdri Isakovtsy 32inexpectatus 31auriculatus 30 cornutus Burgsvik siluricus Grinchuk 29bohemicus Ludfordian 415Ma 28 leintwardinensis Eke ploeckensis LUDLOW 27 hemiaversus Sokol 26invertus Hemse 25 scanicus 24 progenitor Konovka Gorstian crassa 424 Ma 23 nilssoni Much Wenlock Klinteberg G 22 ludensis Limestone 21 nassa stauros Halla Mulde Gèluva W 20 lundgreni Homerian Slite 19 ellesae 18 flexilis amsdeni Coalbrookdale 17 rigidus Tofta Riga SILURIAN 16 riccartonensis WENLOCK Hogklint 15 murchisoni ranuliformis 14 430.5 Ma Sheinwoodian centrifugus Buildwas U. Visby 13 crenulata amorphognathoides Chicotte L. Visby 12 griestoniensis 11 crispus celloni 10 turriculatus Jupiter Telychian 9 sedgwickii 8 convolutus staurognathoides 7 leptotheca 6 magnus Gun River 5 Aeronian triangulatus kentuckensis LLANDOVERY 4 cyphus Merrimack 3 acinaces 2 atavus nathani Becscie 1 acuminatus 439 Ma Rhuddanian ORDOVICIAN Ellis Bay Figure 1. Sampled Silurian sections and their stratigraphic assignments (modified from Basset et al., 1989; Siveter et al., 1989; Jin et al., 1990; Kaminskas and Musteikis, 1994; Long and Copper, 1994). from one of the slabs, was studied under a polar- at the University of Ottawa, to test for shell chem- on a tantalum filament. The strontium isotope ra- izing microscope to examine the preservation of ical preservation (Azmy, 1996). tio was measured using the Finnigan MAT 261 the calcite fibers. The thin section and the other For Sr-isotope analysis, about 1 mg of the multicollector thermal ionization mass spectro- polished slab were viewed under cathodolumi- powdered sample was dissolved for 30 min in 1.5 meter at Carleton University. The laboratory stan- nescence, with the operating conditions at ~10 to ml of 2.5N suprapure HCl at room temperature, dard used was NBS 987 (87Sr/86Sr = 0.710249) 11 kv, gun current of 350 to 400 mA, and vacuum and Sr was extracted via a clean 10 ml column with a (2σ) precision calculated from 30 mea- of ~ 0.03 Torr. filled with Dowex AG50-X8 cation resin. The surements of ± 0.000017. The blanks were 0.4 to Carbonate material from the nonluminescent eluent was dried at 125 °C for 2 hr. The dried 0.8 ng. The measured Sr isotope data are listed in parts of the secondary layer was microsampled sample was dissolved in 0.01N HCl for a few Table DR1, GSA Data Repository.1 For further from the slab under a binocular microscope by minutes and passed through a clean 10 ml sepa- details of geology, samples, and analytical and se- smashing the shell with a stainless steel dental ration column filled with Teflon resin to trap Ca lection procedures, see Azmy (1996) and Azmy pick. The fragments were cleaned in an ultra- that may not have been separated from Sr by first et al. (1998). sonic bath. column. The collected sample was evaporated at Another set of brachiopod samples, from Got- A fragment from each sample was studied un- 125 °C for 2 hr to be ready for running on the land, was prepared and measured independently at der a scanning electron microscope to examine mass spectrometer. Blank samples were fre- the laboratory of Ruhr Universität in Bochum fol- the preservation of the calcite crystals. The rest of quently run and spiked using 84Sr to measure any the sample was ground in an acid-washed agate contamination that might occur during the 1GSA Data Repository item 9933, Table DR1, is mortar and ~ 3 mg were used for trace element process of separation. available on request from Documents Secretary, GSA, P.O. Box 9140, Boulder, CO 80301. E-mail: analysis by a Thermo Jarrell Ash-AtomScan 25 The sample was dissolved in 0.4 ml of 1M [email protected]. Web: http://www.geosociety inductively coupled plasma source spectrometer, H3PO4 for 2 min and about half of it was loaded .org/pubs/ftpyrs.htm. 476 Geological Society of America Bulletin, April 1999 SILURIAN STRONTIUM ISOTOPE STRATIGRAPHY Graptolite 87 86 Biozones Sr/ Sr 0.7079 0.7081 0.7083 0.7085 0.7087 0.7089 0.7091 408.5 Ma 37 Í P ídolí 410.7Ma 31 Ludfordian Ludlow 25 Gorstian 424Ma Homerian 19 SILURIAN Wenlock 430.4 Ma Sheinwoodian 13 Telychian 7 This study Aeronian Bertram et al.
Load more

Recommended publications
  • Revised Correlation of Silurian Provincial Series of North America with Global and Regional Chronostratigraphic Units 13 and D Ccarb Chemostratigraphy
    Revised correlation of Silurian Provincial Series of North America with global and regional chronostratigraphic units 13 and d Ccarb chemostratigraphy BRADLEY D. CRAMER, CARLTON E. BRETT, MICHAEL J. MELCHIN, PEEP MA¨ NNIK, MARK A. KLEFF- NER, PATRICK I. MCLAUGHLIN, DAVID K. LOYDELL, AXEL MUNNECKE, LENNART JEPPSSON, CARLO CORRADINI, FRANK R. BRUNTON AND MATTHEW R. SALTZMAN Cramer, B.D., Brett, C.E., Melchin, M.J., Ma¨nnik, P., Kleffner, M.A., McLaughlin, P.I., Loydell, D.K., Munnecke, A., Jeppsson, L., Corradini, C., Brunton, F.R. & Saltzman, M.R. 2011: Revised correlation of Silurian Provincial Series of North America with global 13 and regional chronostratigraphic units and d Ccarb chemostratigraphy. Lethaia,Vol.44, pp. 185–202. Recent revisions to the biostratigraphic and chronostratigraphic assignment of strata from the type area of the Niagaran Provincial Series (a regional chronostratigraphic unit) have demonstrated the need to revise the chronostratigraphic correlation of the Silurian System of North America. Recently, the working group to restudy the base of the Wen- lock Series has developed an extremely high-resolution global chronostratigraphy for the Telychian and Sheinwoodian stages by integrating graptolite and conodont biostratigra- 13 phy with carbonate carbon isotope (d Ccarb) chemostratigraphy. This improved global chronostratigraphy has required such significant chronostratigraphic revisions to the North American succession that much of the Silurian System in North America is cur- rently in a state of flux and needs further refinement. This report serves as an update of the progress on recalibrating the global chronostratigraphic correlation of North Ameri- can Provincial Series and Stage boundaries in their type area.
    [Show full text]
  • University of Birmingham Carbon Isotope (13Ccarb) and Facies
    University of Birmingham Carbon isotope (13Ccarb) and facies variability at the Wenlock-Ludlow boundary (Silurian) of the Midland Platform, UK Blain, John Allan; Wheeley, James; Ray, David DOI: 10.1139/cjes-2015-0194 License: None: All rights reserved Document Version Peer reviewed version Citation for published version (Harvard): Blain, JA, Wheeley, J & Ray, D 2016, 'Carbon isotope (13Ccarb) and facies variability at the Wenlock-Ludlow boundary (Silurian) of the Midland Platform, UK', Canadian Journal of Earth Science. https://doi.org/10.1139/cjes-2015-0194 Link to publication on Research at Birmingham portal Publisher Rights Statement: Publisher Version of Record available at: http://dx.doi.org/10.1139/cjes-2015-0194 Validated Feb 2016 General rights Unless a licence is specified above, all rights (including copyright and moral rights) in this document are retained by the authors and/or the copyright holders. The express permission of the copyright holder must be obtained for any use of this material other than for purposes permitted by law. •Users may freely distribute the URL that is used to identify this publication. •Users may download and/or print one copy of the publication from the University of Birmingham research portal for the purpose of private study or non-commercial research. •User may use extracts from the document in line with the concept of ‘fair dealing’ under the Copyright, Designs and Patents Act 1988 (?) •Users may not further distribute the material nor use it for the purposes of commercial gain. Where a licence is displayed above, please note the terms and conditions of the licence govern your use of this document.
    [Show full text]
  • GEOLOGIC TIME SCALE V
    GSA GEOLOGIC TIME SCALE v. 4.0 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. (Ma) ANOM. CHRON. CHRO HOLOCENE 1 C1 QUATER- 0.01 30 C30 66.0 541 CALABRIAN NARY PLEISTOCENE* 1.8 31 C31 MAASTRICHTIAN 252 2 C2 GELASIAN 70 CHANGHSINGIAN EDIACARAN 2.6 Lopin- 254 32 C32 72.1 635 2A C2A PIACENZIAN WUCHIAPINGIAN PLIOCENE 3.6 gian 33 260 260 3 ZANCLEAN CAPITANIAN NEOPRO- 5 C3 CAMPANIAN Guada- 265 750 CRYOGENIAN 5.3 80 C33 WORDIAN TEROZOIC 3A MESSINIAN LATE lupian 269 C3A 83.6 ROADIAN 272 850 7.2 SANTONIAN 4 KUNGURIAN C4 86.3 279 TONIAN CONIACIAN 280 4A Cisura- C4A TORTONIAN 90 89.8 1000 1000 PERMIAN ARTINSKIAN 10 5 TURONIAN lian C5 93.9 290 SAKMARIAN STENIAN 11.6 CENOMANIAN 296 SERRAVALLIAN 34 C34 ASSELIAN 299 5A 100 100 300 GZHELIAN 1200 C5A 13.8 LATE 304 KASIMOVIAN 307 1250 MESOPRO- 15 LANGHIAN ECTASIAN 5B C5B ALBIAN MIDDLE MOSCOVIAN 16.0 TEROZOIC 5C C5C 110 VANIAN 315 PENNSYL- 1400 EARLY 5D C5D MIOCENE 113 320 BASHKIRIAN 323 5E C5E NEOGENE BURDIGALIAN SERPUKHOVIAN 1500 CALYMMIAN 6 C6 APTIAN LATE 20 120 331 6A C6A 20.4 EARLY 1600 M0r 126 6B C6B AQUITANIAN M1 340 MIDDLE VISEAN MISSIS- M3 BARREMIAN SIPPIAN STATHERIAN C6C 23.0 6C 130 M5 CRETACEOUS 131 347 1750 HAUTERIVIAN 7 C7 CARBONIFEROUS EARLY TOURNAISIAN 1800 M10 134 25 7A C7A 359 8 C8 CHATTIAN VALANGINIAN M12 360 140 M14 139 FAMENNIAN OROSIRIAN 9 C9 M16 28.1 M18 BERRIASIAN 2000 PROTEROZOIC 10 C10 LATE
    [Show full text]
  • The Early Ludfordian Leintwardinensis Graptolite Event and the Gorstian–Ludfordian Boundary in Bohemia (Silurian, Czech Republic)
    This is the peer reviewed version of the following article: Štorch, P., Manda, Š., Loydell, D. K. (2014), The early Ludfordian leintwardinensis graptolite Event and the Gorstian–Ludfordian boundary in Bohemia (Silurian, Czech Republic). Palaeontology, 57: 1003–1043. doi: 10.1111/pala.12099, which has been published in final form at 10.1111/pala.12099. This article may be used for non-commercial purposes in accordance with Wiley Terms and Conditions for Self-Archiving. The early Ludfordian leintwardinensis graptolite Event and the Gorstian– Ludfordian boundary in Bohemia (Silurian, Czech Republic) Petr Štorch, Štěpán Manda, David K. Loydell Abstract The late Gorstian to early Ludfordian hemipelagic succession of the south-eastern part of the Prague Synform preserves a rich fossil record dominated by 28 species of planktic graptoloids associated with pelagic myodocopid ostracods, pelagic and nektobenthic orthocerid cephalopods, epibyssate bivalves, nektonic phyllocarids, rare dendroid graptolites, brachiopods, crinoids, trilobites, sponges and macroalgae. Faunal dynamics have been studied with particular reference to graptolites. The early Ludfordian leintwardinensis graptolite extinction Event manifests itself as a stepwise turnover of a moderate diversity graptolite fauna rather than an abrupt destruction of a flourishing biota. The simultaneous extinction of the spinose saetograptids Saetograptus clavulus, Saetograptus leintwardinensis and the rare S. sp. B. at the top of the S. leintwardinensisZone was preceded by a short- term acme of S. clavulus. Cucullograptus cf. aversus and C. rostratusvanished from the fossil record in the lower part of the Bohemograptus tenuis Biozone. No mass proliferation of Bohemograptus has been observed in the postextinction interval. Limited indigenous speciation gave rise to Pseudomonoclimacis kosoviensis and Pseudomonoclimacis cf.dalejensis.
    [Show full text]
  • International Chronostratigraphic Chart
    INTERNATIONAL CHRONOSTRATIGRAPHIC CHART www.stratigraphy.org International Commission on Stratigraphy v 2014/02 numerical numerical numerical Eonothem numerical Series / Epoch Stage / Age Series / Epoch Stage / Age Series / Epoch Stage / Age Erathem / Era System / Period GSSP GSSP age (Ma) GSSP GSSA EonothemErathem / Eon System / Era / Period EonothemErathem / Eon System/ Era / Period age (Ma) EonothemErathem / Eon System/ Era / Period age (Ma) / Eon GSSP age (Ma) present ~ 145.0 358.9 ± 0.4 ~ 541.0 ±1.0 Holocene Ediacaran 0.0117 Tithonian Upper 152.1 ±0.9 Famennian ~ 635 0.126 Upper Kimmeridgian Neo- Cryogenian Middle 157.3 ±1.0 Upper proterozoic Pleistocene 0.781 372.2 ±1.6 850 Calabrian Oxfordian Tonian 1.80 163.5 ±1.0 Frasnian 1000 Callovian 166.1 ±1.2 Quaternary Gelasian 2.58 382.7 ±1.6 Stenian Bathonian 168.3 ±1.3 Piacenzian Middle Bajocian Givetian 1200 Pliocene 3.600 170.3 ±1.4 Middle 387.7 ±0.8 Meso- Zanclean Aalenian proterozoic Ectasian 5.333 174.1 ±1.0 Eifelian 1400 Messinian Jurassic 393.3 ±1.2 7.246 Toarcian Calymmian Tortonian 182.7 ±0.7 Emsian 1600 11.62 Pliensbachian Statherian Lower 407.6 ±2.6 Serravallian 13.82 190.8 ±1.0 Lower 1800 Miocene Pragian 410.8 ±2.8 Langhian Sinemurian Proterozoic Neogene 15.97 Orosirian 199.3 ±0.3 Lochkovian Paleo- Hettangian 2050 Burdigalian 201.3 ±0.2 419.2 ±3.2 proterozoic 20.44 Mesozoic Rhaetian Pridoli Rhyacian Aquitanian 423.0 ±2.3 23.03 ~ 208.5 Ludfordian 2300 Cenozoic Chattian Ludlow 425.6 ±0.9 Siderian 28.1 Gorstian Oligocene Upper Norian 427.4 ±0.5 2500 Rupelian Wenlock Homerian
    [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]
  • Late Silurian Trilobite Palaeobiology And
    LATE SILURIAN TRILOBITE PALAEOBIOLOGY AND BIODIVERSITY by ANDREW JAMES STOREY A thesis submitted to the University of Birmingham for the degree of DOCTOR OF PHILOSOPHY School of Geography, Earth and Environmental Sciences University of Birmingham February 2012 University of Birmingham Research Archive e-theses repository This unpublished thesis/dissertation is copyright of the author and/or third parties. The intellectual property rights of the author or third parties in respect of this work are as defined by The Copyright Designs and Patents Act 1988 or as modified by any successor legislation. Any use made of information contained in this thesis/dissertation must be in accordance with that legislation and must be properly acknowledged. Further distribution or reproduction in any format is prohibited without the permission of the copyright holder. ABSTRACT Trilobites from the Ludlow and Přídolí of England and Wales are described. A total of 15 families; 36 genera and 53 species are documented herein, including a new genus and seventeen new species; fourteen of which remain under open nomenclature. Most of the trilobites in the British late Silurian are restricted to the shelf, and predominantly occur in the Elton, Bringewood, Leintwardine, and Whitcliffe groups of Wales and the Welsh Borderland. The Elton to Whitcliffe groups represent a shallowing upwards sequence overall; each is characterised by a distinct lithofacies and fauna. The trilobites and brachiopods of the Coldwell Formation of the Lake District Basin are documented, and are comparable with faunas in the Swedish Colonus Shale and the Mottled Mudstones of North Wales. Ludlow trilobite associations, containing commonly co-occurring trilobite taxa, are defined for each palaeoenvironment.
    [Show full text]
  • Late Ludfordian and Early Pridoli Monograptids from the Polish Lowland
    LATE LUDFORDIAN AND EARLY PRIDOLI MONOGRAPTIDS FROM THE POLISH LOWLAND ADAM URBANEK Urbanek, A. 1997. Late Ludfordian and early Pfidoli monograptids from the Polish Low­ land. In: A. Urbanek and L. Teller (eds), Silur ian Graptolite Faunas in the East European Platform: Stratigraphy and Evolution. - Palaeontologia Polonica 56, 87-23 1. Graptolites etched from the Mielnik-I wellcore (EPoland) reveal the main features of the development of monograptid faunas within the late Ludfordian-early Pi'idoli interval. Fifteen species and subspecies are described and Monog raptus (Slovinog raptus) subgen. n. as well as Neocolonograptu s gen. n. are erected. Morphology of many species has been described adequately for the first time and their systematic position corrected. Four grap­ tolite zones of the late Ludfordian are distinguished. The late Ludfordian fauna, which appears after the kozlowskii Event, is composed mainly of immigrants dominated by hooded monograptids. They reappear as a result of the Lazarus effect. Some of them initiated the lobate-spinose phyletic line terminating with Mon ograptus (Uncinatograptus) spineus, a highly characteristic index species. The lobate and the lobate-spinose types are accompanied by bilobate forms (Pse udomonoclimac is latilobu s). The graptolite sequence indicates that the appeara nce of the early Pfidoli fauna was preceded by a biotic crisis, namely the spineus Event. Therefore this fauna is made up of a few holdovers and some new elements which developed from Pristiograptus dubiu s stem lineage (Neocolonograptus gen. n., Istrograpt us Tsegelnjuk). This early assemblage, com­ posed of bilobate forms, was later enriched by hooded monograptid s, reappearing after the spineus Event.
    [Show full text]
  • Phanerozoic Phanerozoic & Precambrian
    Geologic TimeScale Geologic Time Scale 2012 Foundation ISBN 978-0-44-459425-9 ISBN 978-0-44-459425-9 PHANEROZOIC PHANEROZOIC & PRECAMBRIAN y h 18 t d d d δ i c O SeaSea SeaSea AgeAge o PolarityPolarity o PolarityPolarity o i AgeAgeg AgeAgeg i AgeAgeg o ar LisiekiLisieki & ri a a AgeAge / Stage EpochEpoch AgeAge / Stage levellevel EpochEpoch AgeAge / Stage l levellevel EonEon EraEra PeriodPeriod ((Ma)Ma) p ra er er ChronChron Raymo,Raymo, 2005 CChronhron o (Ma)(Ma) -100- 0 100 200m200m (Ma)(Ma) -100 0 100 200m200m (Ma)(Ma) Era Er Period P Epoch E Era Er Period Pe Era E Period P 3453 4 5 Polarity P 0 00.0118.0118 HoloceneHolocene 2 0 Quat.Quat.PleistocenePleistocene see Quaternary detail C1C1 254.22 ChanghsingianChanggghsingian 2552255 Cenozoic Paleogene TTarantianarantian 4 Plioceneocene Piacenzian/P C2 LopingianLopingian 0.13 5.33 Zanclean 5 C3 259.8WuchiapingianW Cretaceous 6 7.257.25 MessinianMessinian 226060 100 CC44 10 e TortonianTortonian CaCapitanianpitanian Mesozoic Jurassic 11.6311.63 2262655 Guada-Guada- 265.1 200 8 13.8213.82 SerravallianSSllierravallian Triassic C5 lupianlupian 268268.8.8 WoWordianrdian 1010 15 15.9715.97 LanghianLLhianghig an Permian ocen 227070 eogene hes 272.272.33 Roadian 300 ian Carboniferous n BurdigalianBurdigalian Neogene N 1212 Miocene Mi 20.4420.44 u 20 227575 r C6 KKungurianungurian Devonian IonianIonian 23.0323.03 AquitanianAqquitanian rm 400 Paleozoic B 0.50.5 Brunhes 21,000 years Quaternary 2279.379.3 Silurian 1414 2525 228080 255 Ma M Permian P i ChattianChattian C7/9C7/9 Permian Pe Ordovician
    [Show full text]
  • INTERNATIONAL CHRONOSTRATIGRAPHIC CHART International Commission on Stratigraphy V 2020/03
    INTERNATIONAL CHRONOSTRATIGRAPHIC CHART www.stratigraphy.org International Commission on Stratigraphy v 2020/03 numerical numerical numerical numerical Series / Epoch Stage / Age Series / Epoch Stage / Age Series / Epoch Stage / Age GSSP GSSP GSSP GSSP EonothemErathem / Eon System / Era / Period age (Ma) EonothemErathem / Eon System/ Era / Period age (Ma) EonothemErathem / Eon System/ Era / Period age (Ma) Eonothem / EonErathem / Era System / Period GSSA age (Ma) present ~ 145.0 358.9 ±0.4 541.0 ±1.0 U/L Meghalayan 0.0042 Holocene M Northgrippian 0.0082 Tithonian Ediacaran L/E Greenlandian 0.0117 152.1 ±0.9 ~ 635 U/L Upper Famennian Neo- 0.129 Upper Kimmeridgian Cryogenian M Chibanian 157.3 ±1.0 Upper proterozoic ~ 720 0.774 372.2 ±1.6 Pleistocene Calabrian Oxfordian Tonian 1.80 163.5 ±1.0 Frasnian 1000 L/E Callovian Quaternary 166.1 ±1.2 Gelasian 2.58 382.7 ±1.6 Stenian Bathonian 168.3 ±1.3 Piacenzian Middle Bajocian Givetian 1200 Pliocene 3.600 170.3 ±1.4 387.7 ±0.8 Meso- Zanclean Aalenian Middle proterozoic Ectasian 5.333 174.1 ±1.0 Eifelian 1400 Messinian Jurassic 393.3 ±1.2 Calymmian 7.246 Toarcian Devonian Tortonian 182.7 ±0.7 Emsian 1600 11.63 Pliensbachian Statherian Lower 407.6 ±2.6 Serravallian 13.82 190.8 ±1.0 Lower 1800 Miocene Pragian 410.8 ±2.8 Proterozoic Neogene Sinemurian Langhian 15.97 Orosirian 199.3 ±0.3 Lochkovian Paleo- Burdigalian Hettangian proterozoic 2050 20.44 201.3 ±0.2 419.2 ±3.2 Rhyacian Aquitanian Rhaetian Pridoli 23.03 ~ 208.5 423.0 ±2.3 2300 Ludfordian 425.6 ±0.9 Siderian Mesozoic Cenozoic Chattian Ludlow
    [Show full text]
  • Type of the Paper (Article
    life Article Dynamics of Silurian Plants as Response to Climate Changes Josef Pšeniˇcka 1,* , Jiˇrí Bek 2, Jiˇrí Frýda 3,4, Viktor Žárský 2,5,6, Monika Uhlíˇrová 1,7 and Petr Štorch 2 1 Centre of Palaeobiodiversity, West Bohemian Museum in Pilsen, Kopeckého sady 2, 301 00 Plzeˇn,Czech Republic; [email protected] 2 Laboratory of Palaeobiology and Palaeoecology, Geological Institute of the Academy of Sciences of the Czech Republic, Rozvojová 269, 165 00 Prague 6, Czech Republic; [email protected] (J.B.); [email protected] (V.Ž.); [email protected] (P.Š.) 3 Faculty of Environmental Sciences, Czech University of Life Sciences Prague, Kamýcká 129, 165 21 Praha 6, Czech Republic; [email protected] 4 Czech Geological Survey, Klárov 3/131, 118 21 Prague 1, Czech Republic 5 Department of Experimental Plant Biology, Faculty of Science, Charles University, Viniˇcná 5, 128 43 Prague 2, Czech Republic 6 Institute of Experimental Botany of the Czech Academy of Sciences, v. v. i., Rozvojová 263, 165 00 Prague 6, Czech Republic 7 Institute of Geology and Palaeontology, Faculty of Science, Charles University, Albertov 6, 128 43 Prague 2, Czech Republic * Correspondence: [email protected]; Tel.: +420-733-133-042 Abstract: The most ancient macroscopic plants fossils are Early Silurian cooksonioid sporophytes from the volcanic islands of the peri-Gondwanan palaeoregion (the Barrandian area, Prague Basin, Czech Republic). However, available palynological, phylogenetic and geological evidence indicates that the history of plant terrestrialization is much longer and it is recently accepted that land floras, producing different types of spores, already were established in the Ordovician Period.
    [Show full text]