13 Flow and balance of the polar ice sheets

Huybrechts, Philippe; Miller, Heinrich

doi:10.1007/10730550_31

Cited by 4 publications

(5 citation statements)

References 30 publications

(21 reference statements)

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“…This gives rise to between 1.85 and 12.6 × 10 6 grid nodes for Greenland and Antarctica, respectively. Geometric datasets for surface elevation, ice thickness and bed elevation incorporate most of the recent observations up to 2001, such as ERS-1 derived satellite heights, BEDMAP and EPICA pre-site survey Antarctic ice thicknesses and the University of Kansas collection of airborne radio-echo-sounding flight tracks over Greenland (Huybrechts and Miller, 2005). The grids correspond to those discussed in Huybrechts and Miller (2005).…”

Section: Agism: the Polar Ice Sheet Componentmentioning

confidence: 99%

“…Geometric datasets for surface elevation, ice thickness and bed elevation incorporate most of the recent observations up to 2001, such as ERS-1 derived satellite heights, BEDMAP and EPICA pre-site survey Antarctic ice thicknesses and the University of Kansas collection of airborne radio-echo-sounding flight tracks over Greenland (Huybrechts and Miller, 2005). The grids correspond to those discussed in Huybrechts and Miller (2005). The finitedifference schemes are implicit in time, either alternatively in the x and y directions for the mass conservation equation or only along the vertical for the thermodynamic equations.…”

Section: Agism: the Polar Ice Sheet Componentmentioning

confidence: 99%

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Description of the Earth system model of intermediate complexity LOVECLIM version 1.2

et al. 2010

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Abstract. The main characteristics of the new version 1.2 of the three-dimensional Earth system model of intermediate complexity LOVECLIM are briefly described. LOVE-CLIM 1.2 includes representations of the atmosphere, the ocean and sea ice, the land surface (including vegetation), the ice sheets, the icebergs and the carbon cycle. The atmospheric component is ECBilt2, a T21, 3-level quasigeostrophic model. The ocean component is CLIO3, which consists of an ocean general circulation model coupled to a comprehensive thermodynamic-dynamic sea-ice model. Its horizontal resolution is of 3 • by 3 • , and there are 20 levels in the ocean. ECBilt-CLIO is coupled to VECODE, a vegetation model that simulates the dynamics of two main terrestrial plant functional types, trees and grasses, as well as desert. VECODE also simulates the evolution of the carbon cycle over land while the ocean carbon cycle is represented by LOCH, a comprehensive model that takes into acCorrespondence to: H. Goosse (hugues.goosse@uclouvain.be) count both the solubility and biological pumps. The ice sheet component AGISM is made up of a three-dimensional thermomechanical model of the ice sheet flow, a visco-elastic bedrock model and a model of the mass balance at the iceatmosphere and ice-ocean interfaces. For both the Greenland and Antarctic ice sheets, calculations are made on a 10 km by 10 km resolution grid with 31 sigma levels. LOVECLIM1.2 reproduces well the major characteristics of the observed climate both for present-day conditions and for key past periods such as the last millennium, the mid-Holocene and the Last Glacial Maximum. However, despite some improvements compared to earlier versions, some biases are still present in the model. The most serious ones are mainly located at low latitudes with an overestimation of the temperature there, a too symmetric distribution of precipitation between the two hemispheres, and an overestimation of precipitation and vegetation cover in the subtropics. In addition, the atmospheric circulation is too weak. The model also tends to underestimate the surface temperature changes (mainly at low latitudes) and to overestimate the ocean heat uptake observed over the last decades.

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Section: Agism: the Polar Ice Sheet Componentmentioning

confidence: 99%

Section: Agism: the Polar Ice Sheet Componentmentioning

confidence: 99%

Description of the Earth system model of intermediate complexity LOVECLIM version 1.2

et al. 2010

Self Cite

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show abstract

“…Geometric datasets for surface elevation, ice thickness and bed elevation incorporate most of the recent observations up to 2001, such as ERS-1 derived satellite heights, BEDMAP and EPICA pre-site survey Antarctic ice thicknesses and the University of Kansas collection of airborne radio-echo-sounding flight tracks over Greenland (Huybrechts and Miller 2005). The grids correspond to those discussed in Huybrechts and Miller (2005) and include modifications in marginal ice thickness around Greenland margins to remove known artefacts when subtracting an ice thickness field constructed for a more limited mask than the actual ice sheet surface elevation. Overdeepened fjord beds of important outlet glaciers were added manually when absent from the interpolated fields, both for Antarctica and Greenland.…”

Section: The Ice Sheet Modelmentioning

confidence: 99%

Response of the Greenland and Antarctic Ice Sheets to Multi-Millennial Greenhouse Warming in the Earth System Model of Intermediate Complexity LOVECLIM

Huybrechts¹,

Goelzer²,

Janssens³

et al. 2011

The Earth's Cryosphere and Sea Level Change

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Calculations were performed with the Earth system model of intermediate complexity LOVECLIM to study the response of the Greenland and Antarctic ice sheets to sustained multi-millennial greenhouse warming. Use was made of fully dynamic 3D thermomechanical ice-sheet models bidirectionally coupled to an atmosphere and an ocean model. Two 3,000-year experiments were evaluated following forcing scenarios with atmospheric CO 2 concentration increased to two and four times the pre-industrial value, and held constant thereafter. In the high concentration scenario the model shows a sustained mean annual warming of up to 10°C in both polar regions. This leads to an almost complete disintegration of the Greenland ice sheet after 3,000 years, almost entirely caused by increased surface melting. Significant volume loss of the Antarctic ice sheet takes many centuries to initiate due to the thermal inertia of the Southern Ocean but is equivalent to more than 4 m of global sea-level rise by the end of simulation period. By that time, surface conditions along the East Antarctic ice sheet margin take on characteristics of the present-day Greenland ice sheet. West Antarctic ice shelves have thinned considerably from subshelf melting and grounding lines have retreated over distances of several 100 km, especially for the Ross ice shelf. In the low concentration scenario, corresponding to a local warming of 3-4°C, polar ice-sheet melting proceeds at a much lower rate. For the first 1,200 years, the Antarctic ice sheet is even slightly larger than today on account of increased accumulation rates but contributes positively to sea-level rise after that. The Greenland ice sheet loses mass at a rate equivalent to 35 cm of global sea level rise during the first 1,000 years increasing to 150 cm during the last 1,000 years. For both scenarios,

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“…This gives rise to between 1.85 and 12.6 x IO6 grid nodes for Greenland and Antarc tica, respectively. Geometric datasets for surface elevation, ice thickness and bed elevation incorporate most of the re cent observations up to 2001, such as ERS-1 derived satel lite heights, BEDMAP and EPICA pre-site survey Antarc tic ice thicknesses and the University of Kansas collection of airborne radio-echo-sounding flight tracks over Green land (Huybrechts and Miller, 2005). The grids correspond to those discussed in Huybrechts and Miller (2005).…”

Section: Agism: the Polar Ice Sheet Componentmentioning

confidence: 99%

“…Geometric datasets for surface elevation, ice thickness and bed elevation incorporate most of the re cent observations up to 2001, such as ERS-1 derived satel lite heights, BEDMAP and EPICA pre-site survey Antarc tic ice thicknesses and the University of Kansas collection of airborne radio-echo-sounding flight tracks over Green land (Huybrechts and Miller, 2005). The grids correspond to those discussed in Huybrechts and Miller (2005). The finitedifference schemes are implicit in time, either alternatively in the x and y directions for the mass conservation equation or only along the vertical for the thermodynamic equations.…”

Section: Agism: the Polar Ice Sheet Componentmentioning

confidence: 99%

Description of the Earth system model of intermediate complexity LOVECLIM version 1.2

Goosse¹,

Brovkin²,

Fichefet³

et al. 2010

Preprint

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Abstract. The main characteristics of the new version 1.2 of the three-dimensional Earth system model of intermediate complexity LOVECLIM are briefly described. LOVECLIM 1.2 includes representations of the atmosphere, the ocean and sea ice, the land surface (including vegetation), the ice sheets, the icebergs and the carbon cycle. The atmospheric component is ECBilt2, a T21, 3-level quasi-geostrophic model. The oceanic component is CLIO3, which is made up of an ocean general circulation model coupled to a comprehensive thermodynamic-dynamic sea-ice model. Its horizontal resolution is 3° by 3°, and there are 20 levels in the ocean. ECBilt-CLIO is coupled to VECODE, a vegetation model that simulates the dynamics of two main terrestrial plant functional types, trees and grasses, as well as desert. VECODE also simulates the evolution of the carbon cycle over land while the oceanic carbon cycle is represented in LOCH, a comprehensive model that takes into account both the solubility and biological pumps. The ice sheet component AGISM is made up of a three-dimensional thermomechanical model of the ice sheet flow, a visco-elastic bedrock model and a model of the mass balance at the ice-atmosphere and ice ocean interfaces. For both the Greenland and Antarctic ice sheets, calculations are made on a 10 km by 10 km resolution grid with 31 sigma levels. LOVECLIM 1.2 reproduces well the major characteristics of the observed climate both for present-day conditions and for key past periods such as the last millennium, the mid-Holocene and the Last Glacial Maximum. However, despite some improvements compared to earlier versions, some biases are still present in the model. The most serious ones are mainly located at low latitudes with an overestimation of the temperature there, a too symmetric distribution of precipitation between the two hemispheres, an overestimation of precipitation and vegetation cover in the subtropics. In addition, the atmospheric circulation is too weak. The model also tends to underestimate the surface temperature changes (mainly at low latitudes) and to overestimate the ocean heat uptake observed over the last decades.

show abstract

13 Flow and balance of the polar ice sheets

Cited by 4 publications

References 30 publications

Description of the Earth system model of intermediate complexity LOVECLIM version 1.2

Description of the Earth system model of intermediate complexity LOVECLIM version 1.2

Response of the Greenland and Antarctic Ice Sheets to Multi-Millennial Greenhouse Warming in the Earth System Model of Intermediate Complexity LOVECLIM

Description of the Earth system model of intermediate complexity LOVECLIM version 1.2

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