Global Climate and Sea Level: ENDURING VARIABILITY AND RAPID FLUCTUATIONS OVER THE PAST 150,000 YEARS

Yokoyama, Yūsuke; Esat, T. M.

doi:10.5670/oceanog.2011.27

Cited by 98 publications

(59 citation statements)

References 55 publications

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“…Given large enough ice sheets prior to MIS 3, the evolution of the Northern Hemisphere ice sheets in CTR with prescribed time-varying GHG and orbital forcing is in good agreement with sea level proxies (Waelbroeck et al, 2002;Peltier, 2004;Yokoyama and Esat, 2011) and ice sheet reconstructions (Peltier, 2004) during the subsequent glacial ice sheet buildup, the LGM, the deglaciation, and the Holocene (Figs. 2a and 3).…”

Section: Ice Sheet Evolution During the Last 78 Kamentioning

confidence: 67%

“…The last glacial termination (∼ 25-10 ka BP) is a welldocumented period of global climate reorganization and ice sheet retreat based on extensive paleo-data coverage (Waelbroeck et al, 2002;Peltier and Fairbanks, 2006;Yokoyama and Esat, 2011;Shakun et al, 2012;Masson-Delmotte et al, 2013). It provides an optimal test bed to study the combined effects of orbital forcing (Milankovitch, 1941;Berger, 1978) and greenhouse gas (GHG) feedbacks on the ice sheet-climate system.…”

Section: Introductionmentioning

confidence: 99%

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Deglacial ice sheet meltdown: orbital pacemaking and CO<sub>2</sub> effects

et al. 2014

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Abstract.One hundred thousand years of ice sheet buildup came to a rapid end ∼ 25-10 thousand years before present (ka BP), when ice sheets receded quickly and multi-proxy reconstructed global mean surface temperatures rose by ∼ 3-5 • C. It still remains unresolved whether insolation changes due to variations of earth's tilt and orbit were sufficient to terminate glacial conditions. Using a coupled three-dimensional climate-ice sheet model, we simulate the climate and Northern Hemisphere ice sheet evolution from 78 ka BP to 0 ka BP in good agreement with sea level and ice topography reconstructions. Based on this simulation and a series of deglacial sensitivity experiments with individually varying orbital parameters and prescribed CO 2 , we find that enhanced calving led to a slowdown of ice sheet growth as early as ∼ 8 ka prior to the Last Glacial Maximum (LGM). The glacial termination was then initiated by enhanced ablation due to increasing obliquity and precession, in agreement with the Milankovitch theory. However, our results also support the notion that the ∼ 100 ppmv rise of atmospheric CO 2 after ∼ 18 ka BP was a key contributor to the deglaciation. Without it, the presentday ice volume would be comparable to that of the LGM and global mean temperatures would be about 3 • C lower than today. We further demonstrate that neither orbital forcing nor rising CO 2 concentrations alone were sufficient to complete the deglaciation.

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Section: Ice Sheet Evolution During the Last 78 Kamentioning

confidence: 67%

Section: Introductionmentioning

confidence: 99%

Deglacial ice sheet meltdown: orbital pacemaking and CO<sub>2</sub> effects

et al. 2014

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“…In general, we know most about the LGM, and information decreases markedly for older glacial maxima. Even for the PGM, information is so limited that studies often invoke an LGM-like ice volume (e.g., Lambeck and Chappell, 2001;Yokoyama and Esat, 2011). Initial assessment of Red Sea glacial sea-level lowstands seemed to support that view (Rohling et al, 1998), but only constrained the LGM sea-level drop to have been at least as low as that of the PGM, without giving a maximum value.…”

Section: Introductionmentioning

confidence: 99%

Differences between the last two glacial maxima and implications for ice-sheet, δ18O, and sea-level reconstructions

Rohling

Hibbert

Williams

et al. 2017

Quaternary Science Reviews

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115

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Arctic ice shelf Last Interglacial Glacioisostatic adjustment a b s t r a c t Studies of past glacial cycles yield critical information about climate and sea-level (ice-volume) variability, including the sensitivity of climate to radiative change, and impacts of crustal rebound on sealevel reconstructions for past interglacials. Here we identify significant differences between the last and penultimate glacial maxima (LGM and PGM) in terms of global volume and distribution of land ice, despite similar temperatures and radiative forcing. Our analysis challenges conventional views of relationships between global ice volume, sea level, seawater oxygen isotope values, and deep-sea temperature, and supports the potential presence of large floating Arctic ice shelves during the PGM. The existence of different glacial 'modes' calls for focussed research on the complex processes behind ice-age development. We present a glacioisostatic assessment to demonstrate how a different PGM ice-sheet configuration might affect sea-level estimates for the last interglacial. Results suggest that this may alter existing last interglacial sea-level estimates, which often use an LGM-like ice configuration, by several metres (likely upward).

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“…In particular, the duration of melting on Greenland during the Eemian is not wellconstrained by proxy data (e.g. Yokoyama and Esat, 2011). To estimate this duration, a transient simulation with the SICOPOLIS GrIS model is carried out spanning the period 130 ka to 110 ka, forced with two time-slice simulations of IPSL CM4 at 126 ka and 115 ka.…”

Section: Simulated Greenland Ice Sheet Covermentioning

confidence: 99%

Melting of Northern Greenland during the last interglaciation

Born

Nisancioglu

2012

The Cryosphere

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Abstract. Using simulated climate data from the comprehensive coupled climate model IPSL CM4, we simulate the Greenland ice sheet (GrIS) during the Eemian interglaciation with the three-dimensional ice sheet model SICOPOLIS. The Eemian is a period 126 000 yr before present (126 ka) with Arctic temperatures comparable to projections for the end of this century. In our simulation, the northeastern part of the GrIS is unstable and retreats significantly, despite moderate melt rates. This result is found to be robust to perturbations within a wide parameter space of key parameters of the ice sheet model, the choice of initial ice temperature, and has been reproduced with climate forcing from a second coupled climate model, the CCSM3. It is shown that the northeast GrIS is the most vulnerable. Even a small increase in melt removes many years of ice accumulation, giving a large mass imbalance and triggering the strong ice-elevation feedback. Unlike the south and west, melting in the northeast is not compensated by high accumulation. The analogy with modern warming suggests that in coming decades, positive feedbacks could increase the rate of mass loss of the northeastern GrIS, exceeding the recent observed thinning rates in the south.

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Global Climate and Sea Level: ENDURING VARIABILITY AND RAPID FLUCTUATIONS OVER THE PAST 150,000 YEARS

Cited by 98 publications

References 55 publications

Deglacial ice sheet meltdown: orbital pacemaking and CO<sub>2</sub> effects

Deglacial ice sheet meltdown: orbital pacemaking and CO<sub>2</sub> effects

Differences between the last two glacial maxima and implications for ice-sheet, δ18O, and sea-level reconstructions

Melting of Northern Greenland during the last interglaciation

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Global Climate and Sea Level: ENDURING VARIABILITY AND RAPID FLUCTUATIONS OVER THE PAST 150,000 YEARS

Cited by 98 publications

References 55 publications

Deglacial ice sheet meltdown: orbital pacemaking and CO&lt;sub&gt;2&lt;/sub&gt; effects

Deglacial ice sheet meltdown: orbital pacemaking and CO&lt;sub&gt;2&lt;/sub&gt; effects

Differences between the last two glacial maxima and implications for ice-sheet, δ18O, and sea-level reconstructions

Melting of Northern Greenland during the last interglaciation

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Product

Resources

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Deglacial ice sheet meltdown: orbital pacemaking and CO<sub>2</sub> effects

Deglacial ice sheet meltdown: orbital pacemaking and CO<sub>2</sub> effects