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Volumn 299, Issue 5613, 2003, Pages 1728-1731

Timing of atmospheric CO2 and antarctic temperature changes across termination III

Author keywords

[No Author keywords available]

Indexed keywords

ARGON; CARBON DIOXIDE; COMPOSITION; GLACIAL GEOLOGY; ICE;

EID: 0037436505     PISSN: 00368075     EISSN: None     Source Type: Journal    
DOI: 10.1126/science.1078758     Document Type: Article
Times cited : (168)

References (45)
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    • note
    • 2 lagged Vostok temperature by 600 ± 400 ± 400 years at the start of the last three Terminations, but the gas age-ice age difference at Vostok may be uncertain by 1000 years (1) and thus obscures the phasing of gas variations with climate signals borne by the ice.
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    • The firn is the uppermost part of an ice sheet. It can be schematically divided into three zones with different properties concerning the movement of air: the convective zone in which the air is well mixed, the diffusive zone in which vertical transport is driven by molecular diffusion, and the nondiffusive zone in which air does not migrate vertically, and at the bottom of which the air is trapped (17). This entrapped air is younger than the surrounding ice, which results in an age difference (Δage) between the ice and the air bubbles that it contains.
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    • 40Ar record as precise as that which we obtained during the Termination (i.e., between 2830 and 2775 m) and does not allow a peak-to-peak correlation.
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    • 15N for Termination III is not available (fig. S1).
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    • The deuterium content of the snow in East Antarctica is linearly related to the surface temperature of the precipitation site. Jouzel and colleagues (43) have reviewed all relevant information focusing on the East Antarctic Plateau where both model and empirical isotope-temperature estimates are available. Combining arguments coming from the isotopic composition of the air bubbles, from constraints with respect to ice core chronologies, from atmospheric general circulation models, and from isotopic general circulation models (see references herein), the authors suggest that, unlike for Greenland, the present-day spatial isotope-temperature slope can be taken as a surrogate of the temporal slope to interpret glacial-interglacial isotopic changes at sites such as Vostok.
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    • The nondiffusive zone is at the bottom of the fim and thus warms several hundred years after the surface because of the slow diffusion of heat through the firn (4). Additionally, the low accumulation rates at Vostok make the downward transport of firn physical properties rather slow (potentially spanning thousands of years). For example, if strong winds during the glacial periods created wind-packed layers that later impeded gas diffusion, thus creating a very thick nondiffusive zone, these layers would take several thousand years to be transported down to the nondiffusive zone.
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    • note
    • We acknowledge the effort of the Russian Antarctic expeditions (RAE), the division of Polar Programs (NSF), and the Institut Polaire Paul Emile Victor (IPEV) for their participation in the Vostok Project. We thank T. Sowers, M. Leuenberger, and J. Schwander for their pertinent and useful reviews; and J. Chappellaz, V. Masson-Delmotte, J.-R. Petit, F. Parrenin, H. Gildor, L. Pépin, M. Bender, R. Keeling, A. Landais, V. Caillon, C. Gougon, and B. Bellier for help and for fruitful comments and discussions. This work was supported by the French Programme National d'Études de la Dynamique du Climat (PNEDC), the CEA, the Balzam Foundation, the European program Pole-Ocean-Pole (POP EVK2-2000-00089), by NSF grants OPP 9725305 and ATM 9905241 (J.P.S.), and by recruitment funds from the Scripps Institution of Oceanography.


* 이 정보는 Elsevier사의 SCOPUS DB에서 KISTI가 분석하여 추출한 것입니다.