Greenland during the last interglacial: the relative importance of insolation and oceanic changes

Pedersen, Rasmus A.; Langen, Peter L.; Vinther, Bo M.

doi:10.5194/cp-12-1907-2016

Cited by 4 publications

(4 citation statements)

References 60 publications

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“…Regarding the reconstructed LIG temperatures at the NEEM 65 and GISP2 66 ice-core sites, there is uncertainty in which dδ 18 Oice/dT relationship should be used to reconstruct LIG temperatures, and this uncertainty is exacerbated when applying the modern dδ 18 Oice-dT 583 relationship to past climates, where differences in orbital forcing, moisture transport pathways, 584 ice-sheet topography, and sea-ice extent can change the relationship [67][68][69][70][71][72] . To illustrate some of 585 these uncertainties, we have compared our simulated temperatures for the NEEM and GISP2 ice-586 core sites with the temperature reconstructions for these sites based on δ 18 Oice (Extended Data Fig.…”

Section: Evidence For Warming Over the Greenland Ice Sheet During Thementioning

confidence: 99%

Oceanic forcing of penultimate deglacial and last interglacial sea-level rise

Clark

Golledge

et al. 2020

Nature

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Climate evolution over the last two terminations shares a number of similarities (Extended Data Fig. 1). Proxy records of ocean circulation show that the last two terminations were accompanied by large reductions of the AMOC. Climate responses to these reductions show the characteristic bi-polar seesaw due to reduced northerly ocean heat transport and the weakening of the Asian monsoon due to the cooling of the Northern Hemisphere. Other similarities include an increase in the rate of sea-level rise when the AMOC begins to decrease and the occurrence of a Heinrich event during the period of reduced AMOC. Similar climate changes accompanied earlier terminations over the last 640 ka 18 , suggesting that an AMOC reduction is a characteristic feature 46 of these periods of rapid deglaciation. 47 259 grants AGS-1503032 (to P.U.C.), AGS-1502990 (to F.H.) OCE-1702684 (to J.X.M.), and 260 (to A.D.); the NOAA Climate and Global Change Postdoctoral Fellowship program, 261 administered by the University Corporation for Atmospheric Research (to F.H.); contract 262 VUW1501 from the Royal Society Te Aparangi with support from the Antarctic Research Centre, Victoria University of Wellington (to N.R.G.); contract CO5X1001 to GNS Science from the Ministry for Business, Innovation and Employment (to N.R.G.); and Harvard University (J.X.M.). We acknowledge high-performance computing support from Yellowstone (ark:/85065/d7wd3xhc) provided by NCAR's Computational and Information Systems Laboratory, sponsored by the NSF. This research used resources of the Oak Ridge Leadership Computing Facility at the Oak Ridge National Laboratory, which is supported by the Office of Science of the US Department of Energy under Contract No. DE-AC05-00OR22725. PISM is supported by NASA grants NNX13AM16G and NNX13AK27G. We thank Jason Box, Christo Buizert, and Anais Orsi for discussions. Author contributions F.H. performed the GCM modeling; N.R.G. performed the ice-sheet modeling; J.X.M. performed the sea-level modeling with help from S.

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Section: Evidence For Warming Over the Greenland Ice Sheet During Thementioning

confidence: 99%

Oceanic forcing of penultimate deglacial and last interglacial sea-level rise

Clark

Golledge

et al. 2020

Nature

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“…Several attempts to solve this paradox have been made by suggesting possible biases in the interpretation of the relationship between isotope ratio and temperature, which may not be assumed temporally and spatially constant (e.g. Merz et al, 2014;Sjolte et al, 2014;SteenLarsen et al, 2014;Masson-Delmotte et al, 2015) or may be affected by changes in the precipitation regime and sea ice conditions Pedersen et al, 2016). From a modelling point of view, the decisive question is over what spatial extent and when during the year the temperature reconstruction (and possible future reinterpretations) for the NEEM site should be assumed.…”

Section: Greenland Ice Sheet Evolutionmentioning

confidence: 99%

“…Several studies have therefore attempted to identify possible biases in the NEEM reconstructions (e.g. Merz et al, 2014Merz et al, , 2016Sjolte and Hoffmann, 2014;Steen-Larsen et al, 2014;Masson-Delmotte et al, 2015;Pedersen et al, 2016). Furthermore, the minimum extent and margin position of the north-eastern part of the ice sheet is not well constrained, leaving room for alternative retreat scenarios (e.g.…”

mentioning

confidence: 99%

Last Interglacial climate and sea-level evolution from a coupled ice sheet–climate model

et al. 2016

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Abstract. As the most recent warm period in Earth's history with a sea-level stand higher than present, the Last Interglacial (LIG, ∼ 130 to 115 kyr BP) is often considered a prime example to study the impact of a warmer climate on the two polar ice sheets remaining today. Here we simulate the Last Interglacial climate, ice sheet, and sea-level evolution with the Earth system model of intermediate complexity LOVECLIM v.1.3, which includes dynamic and fully coupled components representing the atmosphere, the ocean and sea ice, the terrestrial biosphere, and the Greenland and Antarctic ice sheets. In this setup, sea-level evolution and climate-ice sheet interactions are modelled in a consistent framework.Surface mass balance change governed by changes in surface meltwater runoff is the dominant forcing for the Greenland ice sheet, which shows a peak sea-level contribution of 1.4 m at 123 kyr BP in the reference experiment. Our results indicate that ice sheet-climate feedbacks play an important role to amplify climate and sea-level changes in the Northern Hemisphere. The sensitivity of the Greenland ice sheet to surface temperature changes considerably increases when interactive albedo changes are considered. Southern Hemisphere polar and sub-polar ocean warming is limited throughout the Last Interglacial, and surface and sub-shelf melting exerts only a minor control on the Antarctic sea-level contribution with a peak of 4.4 m at 125 kyr BP. Retreat of the Antarctic ice sheet at the onset of the LIG is mainly forced by rising sea level and to a lesser extent by reduced ice shelf viscosity as the surface temperature increases. Global sea level shows a peak of 5.3 m at 124.5 kyr BP, which includes a minor contribution of 0.35 m from oceanic thermal expansion. Neither the individual contributions nor the total modelled sea-level stand show fast multi-millennial timescale variations as indicated by some reconstructions.

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“…Huybrechts, 2002) or with interest on longer timescales (e.g. Pollard and DeConto, 2009;de Boer et al, 2013de Boer et al, , 2014. A recent study by DeConto and Pollard (2016) utilises simulations of the AIS during the LIG to constrain future sea-level projections.…”

Section: Introductionmentioning

confidence: 99%

Last Interglacial climate and sea-level evolution from a coupled ice sheet-climate model

Goelzer¹,

Huybrechts²,

Loutre³

et al. 2016

Preprint

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Abstract. As the most recent warm period in Earth’s history with a sea-level stand higher than present, the Last Interglacial period (~130 to 115 kyr BP) is often considered a prime example to study the impact of a warmer climate on the two polar ice sheets remaining today. Here we simulate the Last Interglacial climate, ice sheet and sea-level evolution with the Earth system model of intermediate complexity LOVECLIM v.1.3, which includes dynamic and fully-coupled components representing the atmosphere, the ocean and sea ice, the terrestrial biosphere and the Greenland and Antarctic ice sheets. In this set-up, sea-level evolution and climate-ice sheet interactions are modelled in a consistent framework. Surface mass balance changes are the dominant forcing for the Greenland ice sheet, which shows a peak sea-level contribution of 1.4 m at 123 kyr BP in the reference experiment. Our results indicate that ice sheet-climate feedbacks play an important role to amplify climate and sea-level changes in the Northern Hemisphere. The sensitivity of the Greenland ice sheet to surface temperature changes considerably increases when interactive albedo changes are considered. Southern Hemisphere polar and sub-polar ocean warming is limited throughout the Last Interglacial and surface and sub-shelf melting exerts only a minor control on the Antarctic sea-level contribution with a peak of 4.4 m at 125 kyr BP. Retreat of the Antarctic ice sheet at the onset of the LIG is mainly forced by rising sea-level and reduced ice shelf viscosity as the surface temperature increases. Global sea level shows a peak of 5.3 m at 124.5 kyr BP, which includes a minor contribution of 0.35 m from oceanic thermal expansion. Neither the individual contributions nor the total modelled sea-level stand show multi millennial time scale variations as indicated by some reconstructions.

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Greenland during the last interglacial: the relative importance of insolation and oceanic changes

Cited by 4 publications

References 60 publications

Oceanic forcing of penultimate deglacial and last interglacial sea-level rise

Oceanic forcing of penultimate deglacial and last interglacial sea-level rise

Last Interglacial climate and sea-level evolution from a coupled ice sheet–climate model

Last Interglacial climate and sea-level evolution from a coupled ice sheet-climate model

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