On the Response of Sea Ice to the Arctic Oscillation

 

1,2, 2, and 3

1Applied Physics Laboratory, University of Washington, Seattle, Washington

2Department of Atmospheric Sciences, University of Washington, Seattle, Washington

3 Frontier Research System for Global Change, International Arctic Research Center, University of Alaska, Fairbanks, Alaska

 

[The full text of this paper can be obtained from J. Climate, v. 15, no. 18, pp. 2648 - 2668, 2002.]

 

 

Introduction

 

Dramatic changes in Arctic climate have been noted during the past two decades. For example:

1.)   Sea level pressure decreased by 5 mb. (Walsh et al. 1996) between the periods 1986-1994 and 1979-1985 (Fig. 1).

2.)   Surface air temperature warmed from 1979 – 1997 (Rigor et al. 2000) during win­ter and spring, with values as high as 2°C/decade in the eastern Arctic during spring (Fig. 2).

3.)   Sea ice area and extent decreased (Parkinson et al. 1999, Fig. 3), and

4.)   Sea ice thinned (Rothrock et al. 1999, Fig. 4).

 

In this study we address the question “Did the warming of air temperature melt the sea ice, or did the thinner sea ice allow more heat to pass from the ocean to warm the air?

 

 

Arctic Oscillation

 

Many of the changes in Arctic climate have been linked to changes in the Arctic Oscillation (AO, Thompson and Wallace 1998), whose index is defined as the leading principal component (PC) of Northern Hemisphere SLP. The AO can be characterized as an exchange of atmospheric mass between the Arctic Ocean and the sur­rounding zonal ring centered ~45°N. The observed trend in the AO toward its “high index” polarity (i.e. toward stronger westerlies at subpolar latitudes and lower SLP over the Arctic) is a way of interpreting the observed decrease in SLP over the North Pole and the associated cyclonic tendency in the surface winds over the Arctic.

 

In this study we show how the changes in surface wind associated with the fluctua­tions and trend in the AO affect sea ice motion (SIM) in the central Arc­tic and how the changes in SIM, in turn, affect the thickness and concentration of sea ice, and the distribution of SAT over the Arctic.

 

Climatology and Climate Change

 

Data collected by the International Arctic Buoy Programme from 1979–1998 are analyzed to obtain statistics of sea level pressure (SLP, Fig. 5) and sea ice motion (SIM, Fig. 5). The annual and seasonal mean fields agree with those obtained in previous studies of Arctic climatology (Fig. 6). The data show a decrease of 3 hPa in decadal mean SLP over the central Arctic Ocean between 1979–1988 and 1989–1998 (Fig. 7, left column). This decrease in SLP drives a cyclonic trend in SIM, which resembles the structure of the AO (Fig. 7, right column).

 

Regression maps of SIM on the wintertime (January – March) AO index (E.g. Fig. 8) show (1) an increase in ice advection away from the coast of the East Siberian and Laptev seas, which should have the effect of producing more new, thin ice in the coastal flaw leads, (2) a decrease in ice advection from the western Arctic into the eastern Arctic, and (3) a slight increase in ice advection out of the Arctic through Fram Strait. Taken together, these changes suggest that at least part of the thinning of sea ice recently observed over the Arctic Ocean can be attributed to the trend in the AO toward the high index polarity. Maps of the circulation of sea ice (regimes of ice motion, Fig. 9), and the residence time of sea ice (Fig. 10), also show these changes.

 

Seasonal Memory of the Prior Winter Arctic Oscillation

 

Rigor et al. (2000) showed that year-to-year variations in the wintertime AO imprint a distinctive signature on surface air temperature (SAT) anomalies over the Arctic, which is reflected in the spatial pattern of temperature change from the 1980's to the 1990's (Fig. 11). Here it is shown that the memory of the wintertime AO persists through most of the subsequent year: spring and autumn SAT (Figs. 12 and 13) and summertime sea-ice concentration (Fig. 14) are all strongly correlated with the AO-index for the previous winter.

 

It is hypothesized that these delayed responses reflect the dynamical influence of the AO on the thickness of the wintertime sea-ice, whose persistent 'footprint' is reflected in the heat fluxes during the subsequent spring, in the extent of open water during the subsequent summer, and the heat liberated in the freezing of the open water during the subsequent autumn (Fig. below).

 

 

 

References

 

Parkinson, C. L., D. J. Cavalieri, P. Gloersen, H. J. Zwally, and J. Comiso, 1999: Arctic sea ice extents, areas, and trends, 1978–1996. J. Geophys. Res., 104(C9), 20 837–20 856.

 

Rigor, I. G., R. L. Colony, and S. Martin, 2000: Variations in surface air temperature observations in the Arctic, 1979–97. J. Climate, 13(5), 896–914.

 

Rigor, I. G., J.M. Wallace, and R. L. Colony, 2002: On the Response of Sea Ice to the Arctic Oscillation, J. Climate, 15(18), 2546–2663.

 

Rothrock, D. A., Y. Yu, and G. A. Maykut, 1999: Thinning of the Arctic sea-ice cover. Geophys. Res. Lett., 26(23), 3469–3472.

 

Thompson, D. W. J., and J. M. Wallace, 1998: The Arctic Oscillation signature in the wintertime geopotential height and temperature fields. Geophys. Res. Lett., 25(9), 1297–1300.

 

Walsh, J. E., W. L. Chapman, and T. L. Shy, 1996: Recent decrease of sea level pressure in the Central Arctic. J. Climate, 9(2), 480–485.