Recent Arctic change simulated with a coupled ice‐ocean model

Zhang, Yuxia; Hunke, Elizabeth

doi:10.1029/2000jc900159

Cited by 23 publications

(17 citation statements)

References 43 publications

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“…The temperature anomaly map given by Comiso [2001, Figure 5] shows very intense yearly warming in the Beaufort Sea region in 1995 and 1998. In addition a temperature change in the Arctic region is reported by Zhang and Hunke [2001]: A strong increase in the ECMWF 2‐m air temperature in the western Arctic from 1983–1988 to 1989–1997 is shown (their Plate 3).…”

Section: Discussionmentioning

confidence: 97%

Arctic sea ice regional albedo variability and trends, 1982–1998

Laine¹

2004

J. Geophys. Res.

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Whole‐summer and monthly sea ice regional albedo averages for June, July, and August from 1982 to 1998 have been processed from advanced very high resolution radiometer data. Time series for albedo, sea ice concentration, sea ice extent, and surface air temperature have been calculated for the sea ice cover for the Northern Hemisphere as a whole and for six subregions: the Arctic Ocean, the Kara and Barents Seas, the Greenland Sea, the Labrador Sea, Hudson Bay, and the Canadian archipelago. The slope of the summer albedo trend for the Northern Hemisphere is −0.0007 ± 0.0008/year. The largest monthly slope (−0.0016 ± 0.0011/year) is found for June, and the lowest slope (−0.0004 ± 0.0014/year) is found for August. Among the subregions the Greenland Sea has the steepest negative summer trend of −0.0038 ± 0.0012/year during the period, while for the Arctic Ocean the albedo trend is near zero. The calculated trends for the summer sea ice concentration and extent for the Northern Hemisphere are also negative, with a slopes of −0.093 ± 0.069%/year and −42,300 ± 15,200 km2/yr, respectively. In general, the albedo in the central Arctic is between 0.5 and 0.7. The highest albedo values are mainly found in the Arctic Ocean north of Greenland. The lowest albedo (0.2–0.3) occurs in the fringe area of the Arctic Ocean, e.g., on the coasts of Alaska and Siberia. Low albedo values also exist on the east coast of Greenland and in Hudson Bay.

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Section: Discussionmentioning

confidence: 97%

Arctic sea ice regional albedo variability and trends, 1982–1998

Laine¹

2004

J. Geophys. Res.

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“…Considerable freshening in some shelf regions also occurred over this time period (Steele and Ermold 2004). Some of these changes are likely related to variability in atmospheric circulation and temperature associated with the Arctic/North Atlantic Oscillation (e.g., Grotefendt et al 1998;Dickson et al 2000;Zhang and Hunke 2001). This atmospheric variability can modify sea ice transport and the Fram Strait ice flux (Slonosky et al 1997;Mysak and Venegas 1998;Kwok and Rothrock 1999;Rigor et al 2002;), although the relation to Fram Strait ice flux may not be robust on long time scales (Hilmer and Jung 2000).…”

Section: Introductionmentioning

confidence: 94%

Simulated Arctic Ocean Freshwater Budgets in the Twentieth and Twenty-First Centuries

2006

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The Arctic Ocean freshwater budgets in climate model integrations of the twentieth and twenty-first century are examined. An ensemble of six members of the Community Climate System Model version 3 (CCSM3) is used for the analysis, allowing the anthropogenically forced trends over the integration length to be assessed. Mechanisms driving trends in the budgets are diagnosed, and the implications of changes in the Arctic-North Atlantic exchange on the Labrador Sea and Greenland-Iceland-Norwegian (GIN) Seas properties are discussed. Over the twentieth and the twenty-first centuries, the Arctic freshens as a result of increased river runoff, net precipitation, and decreased ice growth. For many of the budget terms, the maximum 50-yr trends in the time series occur from approximately 1975 to 2025, suggesting that we are currently in the midst of large Arctic change. The total freshwater exchange between the Arctic and North Atlantic increases over the twentieth and twenty-first centuries with decreases in ice export more than compensated for by an increase in the liquid freshwater export. Changes in both the liquid and solid (ice) Fram Strait freshwater fluxes are transported southward by the East Greenland Current and partially removed from the GIN Seas. Nevertheless, reductions in GIN sea ice melt do result from the reduced Fram Strait transport and account for the largest term in the changing ocean surface freshwater fluxes in this region. This counteracts the increased ocean stability due to the warming climate and helps to maintain GIN sea deep-water formation.

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“…Wind forcing influences spatial distribution of sea ice, sea ice transport out of the Arctic Basin into the northern North Atlantic and summer Pacific warm water inflow into the Arctic Ocean, particularly when there is thinning of sea ice, which allows a more efficient coupling of surface winds and sea ice (Shimada et al, 2006). Previous observations and simulations have also suggested that sea ice thickness variability is controlled partly by wind forcing (Polyakov and Johnson, 2000;Zhang and Hunke, 2001;Holloway and Sou, 2002;Laxon et al, 2003;Stroeve et al, 2011;Spreen et al, 2011). Carmack and Melling (2011) indicated that anomalous wind patterns and albedo feedback played crucial roles in the rapid loss of Arctic sea ice in recent years.…”

Section: Introductionmentioning

confidence: 97%

Anomalous Arctic surface wind patterns and their impacts on September sea ice minima and trend

Wu¹,

D’Arrigo

2012

Tellus A: Dynamic Meteorology and Oceanography

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We used monthly mean surface wind data from the National Centers for Environmental Prediction/National Centers for Atmospheric Research (NCEP/NCAR) reanalysis dataset during the period 1979–2010 to describe the first two patterns of Arctic surface wind variability by means of the complex vector empirical orthogonal function (CVEOF) analysis. The first two patterns respectively account for 31 and 16% of its total anomalous kinetic energy. The leading pattern consists of the two subpatterns: the northern Laptev Sea (NLS) pattern and the Arctic dipole (AD) pattern. The second pattern contains the northern Kara Sea (NKS) pattern and the central Arctic (CA) pattern. Over the past two decades, the combined dynamical forcing of the first two patterns has contributed to Arctic September sea ice extent (SIE) minima and its declining trend. September SIE minima are mainly associated with the negative phase of the AD pattern and the positive phase of the CA pattern during the summer (July to September) season, and both phases coherently show an anomalous anticyclone over the Arctic Ocean. Wind patterns affect September SIE through their frequency and intensity. The negative trend in September SIE over the past two decades is associated with increased frequency and enhanced intensity of the CA pattern during the melting season from April to September. Thus, it cannot be simply attributed to the AD anomaly characterised by the second empirical orthogonal function mode of sea level pressure north of 70°N. The CA pattern exhibited interdecadal variability in the late 1990s, and an anomalous cyclone prevailed before 1997 and was then replaced by an anomalous anticyclone over the Arctic Ocean that is consistent with the rapid decline trend in September SIE. This paper provides an alternative way to identify the dominant patterns of climate variability and investigate their associated Arctic sea ice variability from a dynamical perspective. Indeed, this study investigates only the role of surface wind dynamical forcing in resulting September SIE minima and trend in terms of CVEOF, without even considering contributions from other factors

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Recent Arctic change simulated with a coupled ice‐ocean model

Cited by 23 publications

References 43 publications

Arctic sea ice regional albedo variability and trends, 1982–1998

Arctic sea ice regional albedo variability and trends, 1982–1998

Simulated Arctic Ocean Freshwater Budgets in the Twentieth and Twenty-First Centuries

Anomalous Arctic surface wind patterns and their impacts on September sea ice minima and trend

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