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Global Chronostratigraphical Correlation Table for the Last 2.7

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Global Chronostratigraphical Correlation Table for the Last 2.7 Global chronostratigraphical correlation table for the last 2.7 million years International Union of Geological Sciences (IUGS), International Union for Quaternary Research (INQUA), International Commission on Stratigraphy (ICS), Stratigraphy and Chronology Commission (SACCOM). Subcommission on Quaternary Stratigraphy (SQS). http://www.geo.uu.nl/ http://www.cam.ac.uk/ K.M. Cohen & P.L. Gibbard v. 2012 http://www.inqua.tcd.ie/ http://www.stratigraphy.org/ Department of Physical Geography Quaternary Palaeoenvironments Group, Cambridge Quaternary Faculty of Geosciences, Utrecht University, The Netherlands Department of Geography, University of Cambridge, United Kingdom. The table provides a correlation of chronostratigraphical subdivisions of late Cenozoic geological time, spanning the last 2.7 million years. The formal division of the Quaternary is the responsibility of the IUGS International Commission on Stratigraphy’s (ICS) Subcommission on Quaternary http://www.quaternary.stratigraphy.org.uk Stratigraphy (SQS), in partnership with the International Union for Quaternary Research’s (INQUA) Commission on Stratigraphy and Chronology (SACCOM). Previous versions of the cores Vostok and Dome-C (EDC) benthic d18O records Section Jingbian ChiLoPart time scale http://www.stratigraphy.org normal reversed 18 chart were published as Gibbard et al. (2004, 2005) and Gibbard & Cohen (2008). Since then stack of 57 globally distributed 78.47ºS 106.86ºE Magnetic susceptibility 37º40’54”N 53º41’48”N 75.10ºS 123.35ºE 108º31’15”E 108º21’06”E biozonation biozonation ItalianMediterranean Marine Stages Sea Coarse grained admixture BiogenicComposite Silica record Content collating overlapping core segments annually updated versions have appeared on the web (e.g. Cohen & Gibbard, 2010). System Series Subseries, ChronsStages Palaeomagnetic record Marine Isotope Stages Planktonic Foraminifera Calcareous Nannoplankton Antarctic Isotope Record Chinese Loess Sequence Lake Baikal BDP-96-1 Sequence [4, 6, 7, 12-19, 22, 25-27, 29-33, 48-50];North West EuropeanBritish Stages Stages Russian Plain StagesNorth American StagesNew Zealand Stages Age ‘Standard Stages’ (super-stages)Age BDP-96-2 [GC-1,1-49]; BDP-98 [4] Age 18 (Ma) Age Subchrons, 5 4 (Ma) 1 0 O -450 -400 0 -8 3 100 75 0 0 10 20 30 40 50 (Ma) Stage atm.‰ SUS 10 m / kg % % weight D >63 mm % % Chronostratigraphy and the base of the Quaternary 0 Holocene (Ma) Excursion events Atlantic Indo-Pacific 0 0 ‘Standard stage’ (‘super-stage’) global divisions 0.5 km 0.5 km S0 depth composite 0.0117 L 2 Termination I - 14 ka down core depth The timescale is based on the internationally-recognised formal chronostratigraphical/geochronological subdivisions a L1 section Weichselian Devensian Valdaian Wisconsinan The desire to divide Quaternary/Pleistocene time into ‘standard stages’, that is units of approximately the same 4 5a 1.0 km 1.0 km of time: the Phanerozoic Eonathem/Eon; the Cenozoic Erathem/Era; the Quaternary System/Period; the Pleistocene t S1 duration as those in the pre-Quaternary time (i.e. Paleogene, Neogene), has been advocated on occasions. The 0.1 e Tyrrhenian 0.1 5 m_ Eemian Ipswichian Mikulinian Sangamonian 0.1 0.12 Blake 5e | MD95-2042 and Holocene Series/Epoch, and finally the Early/Lower, Middle, Late/Upper Pleistocene Subseries/Subepoch. NN21 CN15 CN15 Tarantian only succession that has been divided in this way is the shallow marine sequence in the Mediterranean region, 6 Termination II - 130 ka 2.0 km Warthe At present the Subseries (Subepoch) divisions of the Pleistocene are not formalised. Series, and thereby systems, 2.0 km L2 Drenthe ‘Tottenhill’ Moscovian Illinoian Haweran especially in southern Italy, based principally on faunal and protist biostratigraphy. For various reasons the 0.2 0.2 7a 0.2 14 m_ Dnieper 0.2 are formally-defined based on Global Stratotype Section and Points (GSSP) of which two divide the Quaternary 2.5 km S2 scheme was considered unsatisfactory for use beyond this region. Renewed investigation in recent years has led 7e LR04 stack 0.260 CR0 System into the Holocene and Pleistocene Series. The formal base of the Pleistocene, as ratified in 2009, coincides 8 Termination III - 243 ka PRZ to the proposal of units based on multidisciplinary investigation. The Italian shallow marine stages are derived 9a L3 with a GSSP at Monte San Nicola in southern Italy, marking the base of the Gelasian Stage (Rio et al., 1994, 0.3 0.3 2.5 km Wacken pre-Illinoian A 0.3 from Van Couvering (1997) modified by Cita et al. (2006) (cf. also Cita & Pillans, 2010). In view of their 0.319 CR1 3.0 km Saalian M 9e S3 / Dömnitz 1998). The Gelasian GSSP at 2.58 Ma replaces the previous Pleistocene base GSSP (~1.8 Ma, defined at Vrica, 10 Wolstonian duration, covering multiple climate cycles and periods for which regional stage units of markedly shorter duration Termination IV - 337 ka PT1b NN20 b Fuhne southern Italy), following 60 years of discussion in international stratigraphical commissions and congresses. i S4 have been defined, these ‘standard stages’ are considered as ‘super-stages’. 0.4 11 0.4 Holsteinian Hoxnian Likhvinian 0.4 However, the latter continues as the GSSP for the base of the Calabrian Stage. The chart extends to 2.7 million 12 3.3 km 20 m_ d Termination V - 424 ka 2.8 km L5 years to include the very end of the preceding Piacenzian Stage of the Pliocene Series . d Elsterian Anglian Okian pre-Illinoian B Early–Middle Pleistocene transition (‘mid-Pleistocene revolution’) 0.5 CR2 / 0.5 S5 Interglacial IV 0.5 The chart shows the time between c. 1.2 and 0.5 Ma to have been a transition period in which low-amplitude 14 Gt. truncatulinoides l 0.543Big Lost Termination VI - 533 ka Since 1948 there has been a consensus that the boundary should be placed at the first evidence of climatic cooling Ionian Glacial c 41-ka obliquity-forced climate cycles of the earlier Pleistocene were replaced progressively by high-amplitude Brunhes 15a Muchkapian pre-Illinoian C 0.593 CR3 3.0 km of ice-age magnitude. This was the original basis for placing the boundary at ~1.8 Ma in marine sediments at 0.6 e 0.6 15e CN14 0.6 Interglacial III Cromerian 0.6 100-ka cycles. These later cycles are indicative of slow ice build-up and subsequent rapid melting, and imply Vrica in Calabria, in Italy (Aguirre & Pasini, 1985). It is now known that a major cooling occurred earlier, at 16 Termination VII - 621 ka L6 Neopleistocene a strongly non-linear forced climate system compared to before, accompanied by substantially increased global 30 m_ Glacial b Donian pre-Illinoian D c. 2.55 million years (Cita, 2008), and even earlier cooling events are known from the Pliocene. The closure of a ice volume during glacials after 940 ka. The Early-Middle Pleistocene transition, through the increased severity 0.7 0.7 3.1 km S6 Interglacial II Ilynian 0.7 18 68 m_ Central American Seaways between the Pacific and Atlantic ocean, in three steps starting 3.2 Ma, significantly L7 S6’ Glacial a and duration of cold stages, had a profound effect on the biota and the physical landscape, especially in the IZ pre-Illinoian E restructured oceanic and atmospheric circulation on the Northern Hemisphere, causing increased high latitude 0.781 19 S7 B Pokrovian northern hemisphere (Head & Gibbard 2005). Orbital and non-orbital climate forcing, palaeoceanography, stable 0.8 20 0.8 L8 M Interglacial I 0.8 precipitation, freshening of the Arctic Ocean and increased sea-ice cover amplifying cooling through albedo Q P 3.2 km isotopes, organic geochemistry, marine micropalaeontology, glacial history, loess–palaeosol sequences, pollen feedbacks (Bartoli et al., 2005; Lunt et al., 2007; Sarnthein et al., 2009). Fully completed Panama Isthmus closure S8 ‘Cromerian complex’ Petropavlovian analysis, large and small mammal palaeoecology and stratigraphy, and human evolution provide a series of u l 22 by 2.7 Ma is believed to explain the palaeoenvironmental transitions observed at the Pliocene-Pleistocene 0.9 0.9 40 m_ pre-Illinoian F 0.9 discrete events identified from Marine Isotope Stage (MIS) 36 (c. 1.2 Ma) to MIS 13 (c. 540–460 Ma). Of these, 24 L9 Dorst boundary and to have culminated in the Quaternary glacial-interglacial oscillating climate mode. Since its a e S9 Leerdam the cold MIS 22 (c. 880–870 ka) is the most profound. On this basis Head & Gibbard (2005) and Head et al. 26 25 definition at 1.8 Ma there had been strong pressure for the basal Quaternary / Pleistocene boundary to be moved 0.99 Castlecliffian (2008), following earlier suggestions (e.g. Richmond 1996), concluded that on practical grounds the 1.0 t i 1.0 28 1.0 1.0 downwards better to reflect the initiation of major global cooling (Pillans and Naish 2004; Gibbard et al. 2005; S10 J Matuyama–Brunhes palaeomagnetic Chron boundary (mid-point at 773 ka, with an estimated duration of 7 ka; Jaramillo 30 Linge Bavelian e s ISZ Bowen & Gibbard 2007; Cita & Pillans, 2010), effectively corresponding to the Gauss / Matuyama magnetic 1.07 31 S11 Bavel within MIS 19; Channell et al. 2004) is the best overall point for establishing the Early–Middle Pleistocene Chron boundary (e.g. Partridge, 1997; Suc et al., 1997). See also: Ogg & Pillans (2008); Head et al. (2008); 1.1 r t 32 1.1 S12 50 m_ 1.1 Subseries boundary. 34 Sicilian L13 Lourens (2008); Gibbard & Head (2009a, b) and Gibbard et al. (2009). Krinitisian / Krinitsa n o Gd. fistulosus – Gt. truncatuloides S13 Beestonian 1.2 1.2 36 1.2 pre-Illinoian G 1.2 Major continental records: Antarctic ice, Chinese loess, Lake Baikal 1.22 Cobb PT1a NN19 L14 140 m_ 37 S14 Pleistocene GSSPs a c 1.24 Mountain 38 Menapian Two plots of isotope measurements from Antarctic ice-cores are shown.
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