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• W1490391373 abstract "[3] The long‐term annual mean Arctic SLP field features an anticyclone centered over the northern Beaufort Sea, known as the Beaufort Sea High (BSH), and a trough of low pressure extending from the Icelandic Low northeastward into the Kara Sea. Associated surface winds drive the clockwise Beaufort Gyre ice motion, and the Transpolar Drift Stream (TDS), representing ice motion from the Siberian coast across the Arctic and then into the North Atlantic through Fram Strait. When the winter AO is in its positive mode, SLP over the Icelandic Low region and extending into the Arctic is anomalously low and the BSH is weak, promoting a cyclonic (counter‐clockwise) sea ice circulation anomaly. This is expressed as decreased ice transport from the Beaufort Sea westward across the dateline into the Chukchi Sea, increased ice transport out of the Arctic Ocean through Fram Strait, and increased transport of ice away from the Siberian coast, leaving open water areas that foster new iceformation[Rigoretal.,2002].Bypromotingmorethinice in spring, the positive AO sets the stage for negative summer ice extent anomalies. Conversely, during a negative AO phase, SLP is above normal over the Arctic, most prominent in the vicinity of the Icelandic Low. Ice motion tends to have an anticyclonic (clockwise) anomaly. Ice flow through Fram Strait is reduced, and the Beaufort Gyre is stronger, leading to enhanced ice transport from the western to the eastern Arctic where ice thickens by ridging and rafting against the Siberian coast. The stronger Beaufort Gyre also sequesters and thickens ice in the Canada Basin. Collectively, these processes favor survival of sea ice through summer." @default.
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• W1490391373 date "2011-01-01" @default.
• W1490391373 modified "2023-10-14" @default.
• W1490391373 title "Sea ice response to an extreme negative phase of the Arctic Oscillation during winter 2009/2010" @default.
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• W1490391373 doi "https://doi.org/10.1029/2010gl045662" @default.
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