FN Archimer Export Format
PT J
TI Interglacials of the last 800,000 years
BT 
AF BERGER, A.
   CRUCIFIX, M.
   HODELL, D. A.
   MANGILI, C.
   MCMANUS, J. F.
   OTTO-BLIESNER, B.
   POL, K.
   RAYNAUD, D.
   SKINNER, L. C.
   TZEDAKIS, P. C.
   WOLFF, E. W.
   YIN, Q. Z.
   ABE-OUCHI, A.
   BARBANTE, C.
   BROVKIN, V.
   CACHO, I.
   CAPRON, E.
   FERRETTI, P.
   GANOPOLSKI, A.
   GRIMALT, J. O.
   HOENISCH, B.
   KAWAMURA, K.
   LANDAIS, A.
   MARGARI, V.
   MARTRAT, B.
   MASSON-DELMOTTE, V.
   MOKEDDEM, Zohra
   PARRENIN, F.
   PROKOPENKO, A. A.
   RASHID, H.
   SCHULZ, M.
   RIVEIROS, N. Vazquez
AS 1:1;2:1;3:2;4:3;5:3;6:4;7:5;8:6;9:6;10:7;11:2;12:1;13:8;14:9;15:10;16:11;17:5;18:9;19:12;20:13;21:13;22:14;23:15;24:7;25:13;26:15;27:16;28:6;29:17;30:18;31:19;32:15;
FF 1:;2:;3:;4:;5:;6:;7:;8:;9:;10:;11:;12:;13:;14:;15:;16:;17:;18:;19:;20:;21:;22:;23:;24:;25:;26:;27:PDG-REM-GM-LGS;28:;29:;30:;31:;32:;
C1 Catholic Univ Louvain, Earth & Life Inst, Louvain La Neuve, Belgium.
   Univ Cambridge, Dept Earth Sci, Cambridge CB2 3EQ, England.
   Lamont Doherty Earth Observ, Palisades, NY USA.
   Natl Ctr Atmospher Res, POB 3000, Boulder, CO 80307 USA.
   British Antarctic Survey, Cambridge CB3 0ET, England.
   CNRS UJF, Lab Glaciol & Geophys Environm, Grenoble, France.
   UCL, Dept Geog, London, England.
   Univ Tokyo, Atmosphere & Ocean Res Inst, Tokyo, Japan.
   CNR IDPA, Venice, Italy.
   Max Planck Inst Meteorol, Bundesstr 55, D-20146 Hamburg, Germany.
   Univ Barcelona, Dept Stratig Paleontol & Marine Geosci, Barcelona, Spain.
   Potsdam Inst Climate Impact Res, Potsdam, Germany.
   CSIC, Barcelona, Spain.
   Natl Inst Polar Res, Tokyo, Japan.
   Lab Sci Climat & Environm, Gif Sur Yvette, France.
   Inst Francais Rech Exploitat Mer, Plouzane, France.
   Univ S Carolina, Dept Earth & Ocean Sci, Columbia, SC 29208 USA.
   Mem Univ Newfoundland, Earth Sci, St John, NF, Canada.
   Univ Bremen, Ctr Marine Environm Sci, D-28359 Bremen, Germany.
C2 UNIV CATHOLIC LOUVAIN, BELGIUM
   UNIV CAMBRIDGE, UK
   LDEO, USA
   NCAR NATL CTR ATMOSPHER RES, USA
   BRITISH ANTARCTIC SURVEY, UK
   CNRS UJF, FRANCE
   UNIV COLL LONDON, UK
   UNIV TOKYO, JAPAN
   IAMC CNR, ITALY
   MAX PLANCK INST METEOROL, GERMANY
   UNIV BARCELONA, SPAIN
   POTSDAM INST CLIMATE IMPACT RES, GERMANY
   CSIC, SPAIN
   NATL INST POLAR RES, JAPAN
   LAB SCI CLIMAT & ENVIRONM, FRANCE
   IFREMER, FRANCE
   UNIV S CAROLINA, USA
   UNIV MEM NEWFOUNDLAND, CANADA
   UNIV BREMEN MARUM, GERMANY
SI BREST
SE PDG-REM-GM-LGS
IN WOS Ifremer jusqu'en 2018
   copubli-france
   copubli-europe
   copubli-int-hors-europe
IF 12.34
TC 315
UR https://archimer.ifremer.fr/doc/00340/45150/44547.pdf
   https://archimer.ifremer.fr/doc/00340/45150/44548.pdf
   https://archimer.ifremer.fr/doc/00340/45150/44549.csv
LA English
DT Article
CR IMAGES 3-IPHIS-MD106
   MOZAPHARE-MD104
BO Marion Dufresne
DE ;interglacials;review;quaternary
AB Interglacials, including the present (Holocene) period, are warm, low land ice extent (high sea level), end-members of glacial cycles. Based on a sea level definition, we identify eleven interglacials in the last 800,000years, a result that is robust to alternative definitions. Data compilations suggest that despite spatial heterogeneity, Marine Isotope Stages (MIS) 5e (last interglacial) and 11c (similar to 400ka ago) were globally strong (warm), while MIS 13a (similar to 500ka ago) was cool at many locations. A step change in strength of interglacials at 450ka is apparent only in atmospheric CO2 and in Antarctic and deep ocean temperature. The onset of an interglacial (glacial termination) seems to require a reducing precession parameter (increasing Northern Hemisphere summer insolation), but this condition alone is insufficient. Terminations involve rapid, nonlinear, reactions of ice volume, CO2, and temperature to external astronomical forcing. The precise timing of events may be modulated by millennial-scale climate change that can lead to a contrasting timing of maximum interglacial intensity in each hemisphere. A variety of temporal trends is observed, such that maxima in the main records are observed either early or late in different interglacials. The end of an interglacial (glacial inception) is a slower process involving a global sequence of changes. Interglacials have been typically 10-30ka long. The combination of minimal reduction in northern summer insolation over the next few orbital cycles, owing to low eccentricity, and high atmospheric greenhouse gas concentrations implies that the next glacial inception is many tens of millennia in the future.
PY 2016
PD MAR
SO Reviews Of Geophysics
SN 8755-1209
PU Amer Geophysical Union
VL 54
IS 1
UT 000374690300005
BP 162
EP 219
DI 10.1002/2015RG000482
ID 45150
ER

EF