DOCSLIB.ORG

Triviale Spath

Total Page：16

File Type：pdf, Size：1020Kb

Download full-text PDF Read full-text

Load more

Acta Palaeontologica Polonica Vol. 29, No. 3-4 pp. 161-194; pi s. 17-26 VVarszavva, 1984 TERESA ORLOVVSKA-ZVVOLINSKA PALYNOSTRATIGRAPHY OF THE BUNTSANDSTEIN IN SECTIONS OF WESTERN POLAND ORLOWSKA-ZWOLINSKA, T. : Palynostratigraphy of the Buntsandstein in sec­ tions of western Poland. Ac ta P alaeont. Polonic a , 29, 3-4, 161-194, 1985 (1984) . The .palynological assemblages zones and subzones provide biostratigraphic frame­ work for the Investi gated sections. The Ludbtadispora obs oleta - Protohaplory­ pinus pantlt zone established for the Lower Buntsandstein strata In three sec­ tions of western Poland Is correlated with the Protohaploryplnus association, concurrent with Otoceras In rock of the Griesbachlan stage of East Green­ land. Selected m iospore species are ·descrlbed, Including two new ones: Bacula­ tisporttes verus sp, n. and Elttpsovetatisporltes rugulatus sp, n. , as well as one ne w combination: Protohaploryplnus pantlt Jansonius comb. n, Key w 0 r d s: Lower Triassic, Buntsandstein, palynostratigraphy, palynological assemblage zones, miospores, Poland. Teresa Or!owska-Zwol!71ska, Instytut Geologlczny, Rakowlecka 4, 02-517 Warszawa, Poland. Received: November 1983. INTRODUCTION Results of the author's earlier palynological investigations of the Buntsandstein (Orlowska-Zwolinska 1977) are compared with data from borehole sections Dach6w M-24, Otyn IG-1, Florentyna IG-2 and Czap­ linek IG-2 (fig. 1). A microfloral assemblage, hitherto unknown from the Buntsandstein of Poland, is distinguished, which served to define a new palynological assemblage zone, named after two species abundant in it the Lundbladis­ pora obsoleta - Protohaploxypinus pantii zone . The species composition of this assemblage closely resembles the composition of the Protohaploxy­ pinus association distinguished in East Greenland (Balme 1979) in deposits with Otoceras boreale Spath and Glyptophiceras (Hypophiceras) triviale Spath. .The miospore assemblages of the consecutive assemblage zones are concurrent with index fauna of Early Triassic in the western Poland sec­ tions. The assemblage zone Densoisporites nejburgii occurs in the Middle 162 T ERESA ORLOWSKA-ZWOLINSKA o KOSZALIN Czootine« I G~ Polczyn /G-l POZNAN II a _ . PI . Sroda 16-2 oWARSZAWA /' c:chow M-2t. ~ \ .. ~/, ~·ROty n 16 -1 PI, .F~~rentYna 16 -2 1, 1/ P 1/ /I 1 PI :!l""\. P WROCl.AW P ...."" 9<.• ........,.""~ L,) ">-. '-...... Pa lynolagicalas~ .<'~ ........ J zcnesr sotaooe: .... ~ '\., .~:..,; V. heteromorpha ~ 0 nej burg ii PI o 50 ~P L.obsoleta - P pantii Fig. 1. Localization of borehole. Buntsandstein strata. Its extent partly covers the extent of Gervillia murchisoni Geinitz, as e.g. in .the section Otyn 10-1 (Iig. .3). Quantitative and qualitative variations of the species composition within this zone per­ mitted its subdivision into 3 subzones. The Voltziaceaesporites hetero­ morpha assemblage zone was distinguished in the Upper Buntsandstein strata. It-has been described under the same name in an earlierpaper by the author (Ortowska-Zwolinska 1977). The zone's assemblage concurs with Costatoria costata (Zenker) in the sections: OOTz6w Wielkopolski 10-1, Dach6w M-24 (Senkowiczowa 1965 and unpublished data), Sroda 10-2, and Otyn 10-1 (Oajewska 1982, and unpublished data). The miospore assemblages of the aforementioned section Otyn 10-1 could be compared with megaspore assemblages documented earlier by Fuglewicz (1979) for the same section. An age interpretation of the Low­ er Buntsandstein flora (p. 178) alternative to that given by Fuglewicz (1980), is presented. Table I Palynological zones distinguished in three investigated regions of Poland Fore - Sudetic area West Pomerania North - Eastern Poland Litho- T I 0 a T I 0 a I 0 r a 11st982rat igrI: I!;e Ir-;;;;e;;---:-;=-.-~~--=---- I' "~-_._-,, I""Jewsl<a . ~o' ~r~~,,~ - ~.~:' £ i2 Fn:Gbz, characteristic spec ies characteristic species Vo/lziacl'al'sporitl's heteromorpha ,g Vottz iaceaes pori tes het~omorpha Voltziaceae5porites heteromorpharJI Z ~I.c:" " Klausipollenites sp. di v. Z Z l ~ " Klausipollenites sp, diY, Microcachry idites doubing.,i D ~ Microcochryidite s doubinger i 0­ ~ Microcachryidites daubing.,i Q 0­ Q " Microcachryidites sittteri E Microcochryidites fastidiosus Microcachryidite s lastidiosus rJI ::J Microcachryidites lastidio$us rJI ~ Ii~ - .... ~ ... , 0 . Succinctisporites grandior Succincti5porites grandior rJI ~ Succinctisporites grondior 0 GJ U .::; Krarosl'lisporitl's ullrichi .c:i Kraeuselisporites ullrichi l: Kraeuselisporites ullrichi R Aratrisporites tenuispinosus Aratrisporites tenuispinosus s Aratrisp orites tenuisp inosus: w 01:;:: ~ : I ' ~ ~E s R w c" R W 1O-I '~ ,~ Hexasaccites muelleri ~ 'c :OE . ~ .. ::; m~" Q Glli;; (; 0- Q C>. Brachysaccus ovalis a. Brachysaccus ovalis ~~~fa"{,}a"t;;ri~esoVb~fmei u, lit I-I::J ~ S triatoobietites balmei 1-1::J I- Striatoabietitl's balmei D i Angustisulcites klausii CJ i Angustisulcites kla usi i t Angustisulcites klaus ii D ~ g Angustisulcites gorpii . ~ Angustisu lcites gorpii :: Angus tisulcites gorp "" 11'1 ° '\! ~ ~ I.f) 5 (W I.f) Triodisporo crossa ~ I.f) Q - Triadispora crosse Triadispora crassa Isingl.} t.J ~ Triadispora plicata ~ Triadispora plicata ~ ~'" c c 0 "' , ~ prt's~""nsisrJI l >0 :;:; 0 '''0 o Cycloverrutriletes 0 B~ GI '_PIlI Densoisporites . nejburgii C. vN"E P III not distinqu ishl'd 'p, & others as In: PH Cll5 GI~ :::EE- Z,- S Z Z ·'O D. nso isporites nejburg ii C. ~ Densoisporites n1cburgii - .. Densoi$porites praylordi e tt,,"ct~a;;r,(,z~s p~p~l!gr:1 rJI ,~ , _ Endosporites papillatus "0 I ';: ~ Lundbladispora brevicuta <{ I'O c ::; 'p, Lundbladispo ra bre vicuta ~ ~ microflora not f ound <t: P II Punctatisporifes trassic us ._ c . _ 0 <t: ~ ' ~ ' ~~ :.a a Cyclotriletes microgran;fer s P II Cye/otriletes microgran ifer l ~ "0 I § .2 ::::~ .a 0 .2 ~ ~ ... Platysoccus lesch,ki "0 C>. Platysaccus leschiki _ "Q;"O I"';:~~ I.f) ~ ~ ~ I.f) ~ ' ~ Prot9haploXlpinus p'ellucid,usD I.f) g s <: Protohaploxypinus p'ellucidus D ~ raemoespo n tes nov/au/ens/s , _ , EE ~ :JE :.J(i ; ~ Q Toeniaesp ofltes noviaulensis 0 o 0 a. ... <:l::. ~ ~ EI I- I ~ Densoispor ites nejburg jj 1- 1;:[ P I Endospor ites pap illatus I- ] Acr itarcha rJI .. Protohaploxypinus pantii rJI Z , ... 0::» Taen;aes pori'es noviaulensis Z .... Z , ... unstudied interval .. .S Protohaploxypinus pellucidus c c GIl ,2 GI ~ I ~ Protohaptoxypinus somoilovichii ~ ::: ~ c; .l!! tJ P Cycadopites tot licul aris GI l v ~ ~ Explanat ions: ::J I ~ '8~ g.Cl Lundblcdispora ob,soleta,D ::J I ~ ~ ~ unstudied intervnt ::J I c E :Q Q-<: 8. Lundblad,spora wlilmottl O ICD & CJ rl'lativl'ly abundant o -g~.e Endosporites papillotus o lD .l:' []I a bundant CO 1..1 ::. Q.t Oenso,sporites playlordi COl ..... COl ..... ..... Kraeuselispo rites cuspidus • vl'ry abundant 164 TERESA ORLOWSKA-ZWOLINSKA The sections of western Poland have relatively complete sequences of deposits and contain index fauna; for this reason the palynostratigraphic scheme established for them is now accepted as a base for biostratigraphic correlations of the sections of North-east Poland, and of the Peribaltic Syneclize in particular. The assemblages distinguished in the latter area are of similar composition as those of western Poland (table 1). The present paper has been written in 1979. The data published after 1979 are introduced partly into the text. The specimens described are stored in the Museum of the Geological Institute -In Warsaw (abbreviated as Muz. IG). Acknowledgements. - The a uthor extends her cordial thanks to Dr. 1. Ga­ jewska, Dr. H. Senkowiczowa, Dr. A. Szyperko-Teller and M.Sc. R. Strzelecki for supplying the material for study, for the access to core descriptions, often unpub­ lished, as well as for discussions and kind cooperation during the work. Thanks are due to Dr. A. Szyperko-Teller for her helpful comments and advices about the manuscript. The gratitude is al so extended to Prof. Dr. Sonia Dybowa-Jacho­ wicz for the discussion regarding the palynological part of the paper. Thanks are due to Professor B. E. Balme of University of Western Australia, Nedlands for his helpful written comments facilitating the comparison of the lowermost Triassic as semblages, and for his aid in determining the miospores Lundbladispora willmotti and L. obsoleta. The author is indebted to Dr. B. C. Foster of Geological Survey, Queensland and Dr. G. Playford of Queensland University for their help in solving the prob­ lems related to taxonomy of some pollen grains of Striatiti. METHODS Samples (10-20 grammes) were crushed and treated with 100/0 HCI, . then, for 3 days with cold 400/0 HF, washed with boric acid solution, heated at 70°C for 2 hours in 10% HCI, and the residues were concentrat­ ed in heavy liquid (CdI 2 +KI, 2.1 g/cm"). Oxidation was carried out on all samples using 300/0 HNO a, anhydrous HNO a, or Schultze solution, accord­ ing to the degree of coalification. The residues were mounted in glycerine gelly. Only samples bearing microflora are included in diagrams. Constituent species are recorded as percentages, based on a count of 200 specimens. At low frequency of miospores in the sample, either only 100 specimens were counted in the preparation, or only those species were noted which occurred in at least three preparations. Plankton counts are recorded as numbers of individuals per 200 or 100 microspores. Percentages of low­ frequency species belonging to one genus are sometimes recorded col­ lectively under their generic name. The species occurring sporadically, and those of little stratigraphical value, are placed together with un­ determinated forms under headings Sporites sp. div . and Disaccites sp. div. B u N T 5 A L o w ...~ 3_. 0~~qq C 0::l • ::I~ ~ ~ IllOY' · ~~<.n~ ~ Y' 3 o· "'1 ......~ en 3 "' '1'0 _ . 0 Vi ~ ::I < - ~ ~~'" 0. '1 0 ~uzg:~:= ~=~r'WA~e O" .;:. = g + + ,•• • • KroNSe(i5PO!"ir es cuspidus 80lme +K.opiculo rus . '< ~ 3 C , cf Kra rosel isporrtes punc totus J onSOftius .)anSMIJS T . Stro ters DOrires ric ht er; {Kbus} WIlson ::r:: .? ~ ::l + ...... c-+l1) I ' + I • Prorohoploxypinus ponti; (Ja nlOn;us) com b.new.
Recommended publications
  • R~;: PHYSIOLOGICAL, MIGRATORIAL

    R~;: PHYSIOLOGICAL, MIGRATORIAL

    ....----------- 'r~;: i ! 'r; Pa/eont .. 62(4), 1988, pp. 64~52 Copyright © 1988, The Paleontological Society 0022-3360/88/0062-0640$03.00 PHYSIOLOGICAL, MIGRATORIAL, CLIMATOLOGICAL, GEOPHYSICAL, SURVIVAL, AND EVOLUTIONARY IMPLICATIONS OF CRETACEOUS POLAR DINOSAURS GREGORY S. PAUL 3109 North Calvert Street, Baltimore, Maryland 21218 ABSTRACTT- he presence of Late Cretaceous social dinosaurs in polar regions confronted them with winter conditions of extended dark, coolness, breezes, and precipitation that could best be coped with via an endothermic homeothermic physiology of at least the tenrec level. This is true whether the dinosaurs stayed year round in the polar regime-which in North America extended from Alaska south to Montana-or if they migrated away from polar winters. More reptilian physiologies fail to meet the demands of such winters -in certain key ways, a· point tentatively confirmed by the apparent failure of giant Late Cretaceous phobosuchid crocodilians to dwell north of Montana. Low metabolisms were also insufficient for extended annual migrations away from and towards the poles. It is shown that even high metabolic rate dinosaurs probably remained in their polar habitats year-round. The possibility that dinosaurs had avian-mammalian metabolic systems, and may have borne insulation at least seasonally, severely limits their use as polar paleoclimatic and Earth axial tilt indicators. Polar dinosaurs may have been a center of dinosaur evolution. The possible ability of polar dinosaurs to cope with conditions of cool and dark challenges theories that a gradual temperature decline, or a sudden, meteoritic or volcanic induced collapse in temperature and sunlight, destroyed the dinosaurs. INTRODUCTION America suggests that dinosaurs were regularly crossing, and NCREASINGNUMBERSof remains show that dinosaurs lived living upon, the Bering Land Bridge within a few degrees of the I near the North and South Poles during the Cretaceous.
  • A Possible Late Pleistocene Impact Crater in Central North America and Its Relation to the Younger Dryas Stadial

    A Possible Late Pleistocene Impact Crater in Central North America and Its Relation to the Younger Dryas Stadial

    A POSSIBLE LATE PLEISTOCENE IMPACT CRATER IN CENTRAL NORTH AMERICA AND ITS RELATION TO THE YOUNGER DRYAS STADIAL SUBMITTED TO THE FACULTY OF THE UNIVERSITY OF MINNESOTA BY David Tovar Rodriguez IN PARTIAL FULFILLMENT OF THE REQUIREMENTS FOR THE DEGREE OF MASTER OF SCIENCE Howard Mooers, Advisor August 2020 2020 David Tovar All Rights Reserved ACKNOWLEDGEMENTS I would like to thank my advisor Dr. Howard Mooers for his permanent support, my family, and my friends. i Abstract The causes that started the Younger Dryas (YD) event remain hotly debated. Studies indicate that the drainage of Lake Agassiz into the North Atlantic Ocean and south through the Mississippi River caused a considerable change in oceanic thermal currents, thus producing a decrease in global temperature. Other studies indicate that perhaps the impact of an extraterrestrial body (asteroid fragment) could have impacted the Earth 12.9 ky BP ago, triggering a series of events that caused global temperature drop. The presence of high concentrations of iridium, charcoal, fullerenes, and molten glass, considered by-products of extraterrestrial impacts, have been reported in sediments of the same age; however, there is no impact structure identified so far. In this work, the Roseau structure's geomorphological features are analyzed in detail to determine if impacted layers with plastic deformation located between hard rocks and a thin layer of water might explain the particular shape of the studied structure. Geophysical data of the study area do not show gravimetric anomalies related to a possible impact structure. One hypothesis developed on this works is related to the structure's shape might be explained by atmospheric explosions dynamics due to the disintegration of material when it comes into contact with the atmosphere.
  • Formal Ratification of the Subdivision of the Holocene Series/ Epoch

    Formal Ratification of the Subdivision of the Holocene Series/ Epoch

    Article 1 by Mike Walker1*, Martin J. Head 2, Max Berkelhammer3, Svante Björck4, Hai Cheng5, Les Cwynar6, David Fisher7, Vasilios Gkinis8, Antony Long9, John Lowe10, Rewi Newnham11, Sune Olander Rasmussen8, and Harvey Weiss12 Formal ratification of the subdivision of the Holocene Series/ Epoch (Quaternary System/Period): two new Global Boundary Stratotype Sections and Points (GSSPs) and three new stages/ subseries 1 School of Archaeology, History and Anthropology, Trinity Saint David, University of Wales, Lampeter, Wales SA48 7EJ, UK; Department of Geography and Earth Sciences, Aberystwyth University, Aberystwyth, Wales SY23 3DB, UK; *Corresponding author, E-mail: [email protected] 2 Department of Earth Sciences, Brock University, 1812 Sir Isaac Brock Way, St. Catharines, Ontario LS2 3A1, Canada 3 Department of Earth and Environmental Sciences, University of Illinois, Chicago, Illinois 60607, USA 4 GeoBiosphere Science Centre, Quaternary Sciences, Lund University, Sölveg 12, SE-22362, Lund, Sweden 5 Institute of Global Change, Xi’an Jiaotong University, Xian, Shaanxi 710049, China; Department of Earth Sciences, University of Minne- sota, Minneapolis, MN 55455, USA 6 Department of Biology, University of New Brunswick, Fredericton, New Brunswick E3B 5A3, Canada 7 Department of Earth Sciences, University of Ottawa, Ottawa K1N 615, Canada 8 Centre for Ice and Climate, The Niels Bohr Institute, University of Copenhagen, Julian Maries Vej 30, DK-2100, Copenhagen, Denmark 9 Department of Geography, Durham University, Durham DH1 3LE, UK 10
  • International Chronostratigraphic Chart

    International Chronostratigraphic Chart

    INTERNATIONAL CHRONOSTRATIGRAPHIC CHART www.stratigraphy.org International Commission on Stratigraphy v 2018/08 numerical numerical numerical Eonothem 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) / Eon Erathem / 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 152.1 ±0.9 ~ 635 Upper 0.0117 Famennian Neo- 0.126 Upper Kimmeridgian Cryogenian Middle 157.3 ±1.0 Upper proterozoic ~ 720 Pleistocene 0.781 372.2 ±1.6 Calabrian Oxfordian Tonian 1.80 163.5 ±1.0 Frasnian Callovian 1000 Quaternary Gelasian 166.1 ±1.2 2.58 Bathonian 382.7 ±1.6 Stenian Middle 168.3 ±1.3 Piacenzian Bajocian 170.3 ±1.4 Givetian 1200 Pliocene 3.600 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 Devonian Calymmian 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- 2050 Burdigalian Hettangian 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 27.82 Gorstian
  • INTERNATIONAL CHRONOSTRATIGRAPHIC CHART International Commission on Stratigraphy V 2020/03

    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
  • Meghalayan Age

    Meghalayan Age

    Meghalayan Age drishtiias.com/printpdf/meghalayan-age Why in news? Geologists have decided to classify the past 4,200 years as the Meghalayan Age. It is the most recent unit of the Geologic Time Scale in the 4.6 billion-year history of the Earth. Following this, the International Chronostratigraphic Chart, which depicts the timeline for Earth's history will be updated. What is Meghalayan Age? The “Meghalayan Age” began 4,200 years ago and experienced an abrupt mega- drought and cooling around the globe. The drought and the cooling lasted two centuries and severely impacted agricultural- based societies that developed in several regions after the end of the last Ice Age. It resulted in the collapse of civilisations in Egypt, Greece, Syria, Palestine, Mesopotamia, the Indus Valley, and the Yangtze River Valley. Evidence of the 4,200-year climatic event has been found on all seven continents. This age is considered unique as this was the only age which began with a global cultural event produced by a global climatic event. Geologists have also introduced two other age classifications: 1. Greenlandian Age (11,700 - 8,326 years ago) - began when the last ice age ended and the world began to warm up. 2. Northgrippian Age (8,326 – 4,200 years ago) – began after an abrupt global cooling started following the Greenlandian Age. Together, these three stages stretch across the Holocene Epoch, which is the current geological time unit - having started 11,700 years ago. The Holocene epoch falls under Cenozoic Era and is the time after Ice Age. Methods of Classification 1/3 Each subdivision of the Holocene Epoch is marked out by sediments accumulated on sea floors, lake bottoms, glacial ice and in stalactites and stalagmites across the world.
  • International Chronostratigraphic Chart

    International Chronostratigraphic Chart

    INTERNATIONAL CHRONOSTRATIGRAPHIC CHART www.stratigraphy.org International Commission on Stratigraphy v 2018/07 numerical numerical numerical Eonothem 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) / Eon Erathem / 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 152.1 ±0.9 ~ 635 Upper 0.0117 Famennian Neo- 0.126 Upper Kimmeridgian Cryogenian Middle 157.3 ±1.0 Upper proterozoic ~ 720 Pleistocene 0.781 372.2 ±1.6 Calabrian Oxfordian Tonian 1.80 163.5 ±1.0 Frasnian Callovian 1000 Quaternary Gelasian 166.1 ±1.2 2.58 Bathonian 382.7 ±1.6 Stenian Middle 168.3 ±1.3 Piacenzian Bajocian 170.3 ±1.4 Givetian 1200 Pliocene 3.600 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 Devonian Calymmian 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- 2050 Burdigalian Hettangian 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 27.82 Gorstian
  • International Commission on Stratigraphy SUMMARY REPORT 2017-2020

    International Commission on Stratigraphy SUMMARY REPORT 2017-2020

    International Commission on Stratigraphy SUMMARY REPORT 2017-2020 1. Ratification of GSSPs (boundary stratotypes) created (in stratigraphical order) i. Bases of the Greenlandian, Northgrippian and Meghalayan stages (Holocene), the first two in NGRIP ice cores, central Greenland and the third in a Mawmluh Cave speleothem, Meghalaya, India. 2018 ii. Base of the Chibanian (Pleistocene), Chiba, Japan. 2019 iii. Base of the C hattian (O ligocene) Italy. 2017 iv. Base of the Priabonian (Eocene) Italy. 2020 v. Base of the Hauterivian (Cretaceous) France. 2019 vi. Base of the Sakmarian (Permian) Siberia, Russia. 2018 vii. Base of the Wuliuan Stage (formerly provisional Stage 5) and the Miaolingian Series (formerly provisional Series 3) (Cambrian) Miaoling Mountains, eastern Guizhou, C hina. 2018 2. Other updates to the ICS International Chronostratigraphic Chart i. Bases of the Lower/Early, Middle/Mid-, and Upper/Late Holocene Subseries/Subepochs at the same GSSPs as the stages (above i). 2018 ii. Bases of the Lower/Early, Middle/Mid-, and Upper/Late Pleistocene Subseries/Subepochs at the same GSSPs as the Pleistocene stages (above ii; and the previously defined Gelasian Stage GSSP, i.e. base Pleistocene/Quaternary, and the marker base of the Late Pleistocene stage yet to be defined). 2019 iii. Voting by the ISSC on the adoption of the S ubseries and S ubepochs as formal divisions to be adopted at the discretion of the individual system/period subcommissions. 2019 iv. Voting on a proposal to ISSC to adopt astrochronozones and unit-stratotypes for the Cenozoic Erathem/Era. Proposal was withdrawn by the proposer after ISSC voting resulted in rejection of the unit-stratotype proposal.
  • A New Formal Subdivision of the Holocene Series/Epoch in Estonia

    A New Formal Subdivision of the Holocene Series/Epoch in Estonia

    Estonian Journal of Earth Sciences, 2020, 69, 4, 269–280 https://doi.org/10.3176/earth.2020.15 A new formal subdivision of the Holocene Series/Epoch in Estonia Tiit Hanga, Siim Veskib, Jüri Vassiljevb, Anneli Poskab, Aivar Kriiskac and Atko Heinsalub a Institute of Ecology and Earth Sciences, University of Tartu, Ravila 14A, 50114 Tartu, Estonia; [email protected] b Department of Geology, Tallinn University of Technology, Ehitajate tee 5, 19086 Tallinn, Estonia c Institute of History and Archaeology, University of Tartu, Jakobi 2, 51005 Tartu, Estonia Received 20 May 2020, accepted 15 July 2020, available online 11 November 2020 Abstract. Over the past 25 years since the ratification of the last official Holocene Stratigraphic Chart in Estonia, the stratigraphic framework of global Quaternary geology has significantly progressed. The Pleistocene/Holocene boundary is defined in the NGRIP2 ice core from Greenland, with an age of 11 700 calendar yr b2k (before AD 2000). The International Subcommission on Quaternary Stratigraphy developed a formal tripartite stratigraphical subdivision of the Holocene into the Greenlandian, Northgrippian and Meghalayan stages/ages, each supported by a Global Boundary Stratotype Section and Point (GSSP). All three GSSPs are defined on the basis of geochemical markers reflecting abrupt global climatic events dated with high accuracy and serving as a reliable foundation for cross correlation. In the light of this development we present a new formal subdivision for the Holocene in Estonia. The new chart is climatostratigraphic with tripartite subdivision. The chronological boundaries and corresponding names for the stages/ages are aligned with the International Holocene Stratigraphic Chart.
  • Anthropocene Epoch

    Anthropocene Epoch

    Anthropocene Epoch drishtiias.com/printpdf/anthropocene-epoch Anthropocene Working Group (AWG) voted in favour of designating a new geological epoch i.e, the Anthropocene. The term 'Anthropocene' was coined in 2000 by Nobel Laureate Paul Crutzen and Eugene Stoermer to denote the present geological time interval in which human activity has profoundly altered many conditions and processes on Earth. The word combines the root "anthro", meaning "human" with the root "cene", the standard suffix for "epoch" in geologic time. The Anthropocene is distinguished as a new period either after or within the Holocene, the current epoch, which began approximately 10,000 years ago (about 8000 BC) with the end of the last glacial period. Anthropocene Epoch, unofficial interval of geologic time, making up the third worldwide division of the Quaternary Period (2.6 million years ago to the present), characterized as the time in which the collective activities of human beings (Homo sapiens) began to substantially alter Earth’s surface, atmosphere, oceans, and systems of nutrient cycling. A growing group of scientists argue that the Anthropocene Epoch should follow the Holocene Epoch (11,700 years ago to the present) and begin in the year 1950. The name Anthropocene is derived from Greek and means the “recent age of man.” International Union of Geologic Sciences (IUGS) voted to recommend the Anthropocene as a formal geologic epoch at the 35th International Geological Congress. In order for this interval to be made official, it first must be adopted by the IUGS and the International Commission on Stratigraphy. 1/4 Geologic Marker or Golden Spike 2/4 It is technically called the Global Boundary Stratotype Section and Point (GSSP) that is used to define the lower boundary of a stage on the geologic time scale.
  • Index to the Geologic Names of North America

    Index to the Geologic Names of North America

    Index to the Geologic Names of North America GEOLOGICAL SURVEY BULLETIN 1056-B Index to the Geologic Names of North America By DRUID WILSON, GRACE C. KEROHER, and BLANCHE E. HANSEN GEOLOGIC NAMES OF NORTH AMERICA GEOLOGICAL SURVEY BULLETIN 10S6-B Geologic names arranged by age and by area containing type locality. Includes names in Greenland, the West Indies, the Pacific Island possessions of the United States, and the Trust Territory of the Pacific Islands UNITED STATES GOVERNMENT PRINTING OFFICE, WASHINGTON : 1959 UNITED STATES DEPARTMENT OF THE INTERIOR FRED A. SEATON, Secretary GEOLOGICAL SURVEY Thomas B. Nolan, Director For sale by the Superintendent of Documents, U.S. Government Printing Office Washington 25, D.G. - Price 60 cents (paper cover) CONTENTS Page Major stratigraphic and time divisions in use by the U.S. Geological Survey._ iv Introduction______________________________________ 407 Acknowledgments. _--__ _______ _________________________________ 410 Bibliography________________________________________________ 410 Symbols___________________________________ 413 Geologic time and time-stratigraphic (time-rock) units________________ 415 Time terms of nongeographic origin_______________________-______ 415 Cenozoic_________________________________________________ 415 Pleistocene (glacial)______________________________________ 415 Cenozoic (marine)_______________________________________ 418 Eastern North America_______________________________ 418 Western North America__-__-_____----------__-----____ 419 Cenozoic (continental)___________________________________
  • Formal Subdivision of the Holocene Series/Epoch

    Formal Subdivision of the Holocene Series/Epoch

    Formal subdivision of the Holocene Series/Epoch It has been announced that the proposals for the subdivision of the Holocene Series/Epoch (11 700 years ago to the present day) into three stages/ages and their corresponding subseries/subepochs by the International Subcommission on Quaternary Stratigraphy (ISQS) (a subcommission of the International Commission on Stratigraphy – ICS) have been ratified unanimously by the International Union of Geological Sciences (IUGS). The subdivisions now formally defined are: 1. Greenlandian Stage/Age = Lower/Early Holocene Subseries/Subepoch Boundary Stratotype (GSSP): NorthGRIP2 ice core, Greenland (coincident with the Holocene Series/Epoch GSSP, ratified 2008). Age: 11,700 yr b2k (before AD 2000). 2. Northgrippian Stage/Age = Middle/Mid-Holocene Subseries/Subepoch Boundary Stratotype (GSSP): NorthGRIP1 ice core, Greenland. Global AuXiliary Stratotype: Gruta do Padre Cave speleothem, Brazil. Age: 8326 yr b2k. 3. Meghalayan Stage/Age = Upper/Late Holocene Subseries/Subepoch Boundary stratotype (GSSP): Mawmluh Cave speleothem, Meghalaya, India. Global AuXiliary Stratotype, Mount Logan ice core, Canada. Age: 4250 yr b2k. These divisions are now each defined by Global Stratotype Sections and Points (GSSPs), which means that they are fiXed in time in sedimentary sequences. The terms Greenlandian Stage/Age, Northgrippian Stage/Age, Meghalayan Stage/Age, Lower/Early Holocene Subseries/Subepoch, Middle/Mid-Holocene Subseries/Subepoch and Late/Upper Holocene Subseries/Subepoch therefore have formal definitions and boundaries. These definitions represent the first formal geological subdivision of the Holocene Series/Epoch, resulting from over a decade of labour by members of the joint ISQS (International Subcommission on Quaternary Stratigraphy) - INTIMATE Members Working Group (Integration of Ice-core, Marine and Terrestrial Records), led by Professor Mike Walker (University of Aberystwyth).