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M. Årthun, T. Eldevik, L. H. Smedsrud, Ø. Skagseth, and R. B. Ingvaldsen

1. Introduction The Arctic sea ice cover is a sensitive indicator of climate variability and change ( Serreze et al. 2007 ), and the diminishing Arctic sea ice has had a leading role in recent Arctic temperature amplification ( Screen and Simmonds 2010a ). In the Barents Sea ( Fig. 1a ), winter sea ice extent has decreased since 1850 ( Shapiro et al. 2003 ), and the retreat observed during the recent decades ( Fig. 2 ) has been the largest decrease in the Arctic ( Parkinson and Cavalieri 2008

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Haixia Dai, Ke Fan, and Jiping Liu

the winter temperature of Northeast China ( Wu and Wang 2002 ; Liu et al. 2010 ; Wang and Chen 2010 ; Chen et al. 2013 ; He et al. 2017 ). Moreover, the phase transition of the North Atlantic Oscillation (NAO)/AO accompanied by a super ENSO event ( Geng et al. 2017 ) has also been found to be related to a phase reversal of the Siberian high and EAWM in boreal winter, which may further affect cold blocking events and local cooling over East Asia ( Chang and Lu 2012 ). Anomalous Arctic sea ice

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Camille Li, David S. Battisti, and Cecilia M. Bitz

1. Introduction Sea ice is an important element in the glacial climate system because of its pivotal role in the surface heat, moisture, and momentum budgets of the polar regions. The presence of sea ice lowers surface temperature by insulating the atmosphere from the ocean heat reservoir and by increasing surface albedo. Sea ice also affects the vertical structure of the upper ocean, alters deep-water formation sites, and regulates the availability of moisture for building continental ice

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Mitchell Bushuk, Michael Winton, F. Alexander Haumann, Thomas Delworth, Feiyu Lu, Yongfei Zhang, Liwei Jia, Liping Zhang, William Cooke, Matthew Harrison, Bill Hurlin, Nathaniel C. Johnson, Sarah B. Kapnick, Colleen McHugh, Hiroyuki Murakami, Anthony Rosati, Kai-Chih Tseng, Andrew T. Wittenberg, Xiaosong Yang, and Fanrong Zeng

1. Introduction The Arctic and the Antarctic are Earth’s two natural sea ice environments. These regions differ in a number of fundamental aspects, including their continental geometry, ocean stratification and ventilation, atmospheric and oceanic circulations, tropical teleconnections, sea ice thickness, atmospheric chemistry, and interactions with ice sheets (e.g., Maksym 2019 ; Meredith et al. 2019 ). While the observed Arctic sea ice extent (SIE) decline was generally projected by climate

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Arlan Dirkson, William J. Merryfield, and Adam Monahan

1. Introduction Seasonal forecasting of Arctic sea ice has received increased attention in recent years because of a growing demand for forecasts from an array of stakeholders. This demand has grown largely as a result of the increased access to Arctic waterways ( Ellis and Brigham 2009 ), owing to the reduction in sea ice coverage, which is most prominent in the summer months ( Serreze et al. 2007 ). The overall negative trend in pan-Arctic sea ice extent (SIE) is consistent with climate

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N. Joss Matthewman and Gudrun Magnusdottir

with the WP pattern have a characteristically short time scale of approximately 7.4 days, slightly shorter than the 9.5-day time scale of its Atlantic sector counterpart, the North Atlantic Oscillation (NAO) ( Feldstein 2000 ). Sea ice variability in the Pacific sector is primarily confined to the Bering Sea and Sea of Okhotsk, with the leading mode appearing as a dipole in sea ice concentration between seas ( Cavalieri and Parkinson 1987 ; Fang and Wallace 1994 ; Liu et al. 2007 ; Ukita et al

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James A. Renwick, Alison Kohout, and Sam Dean

1. Introduction The annual cycle of Antarctic sea ice extent is one of the largest seasonal variations on Earth. The maximum areal extent varies by a factor of 5, from ~4 million km 2 in late summer to ~19 million km 2 in late winter, effectively doubling the ice-covered area of Antarctica from minimum to maximum extent ( Thomas and Dieckmann 2003 ; Wadhams 2000 ). Moreover, sea ice in the Antarctic grows around the perimeter of a continent, unconstrained in the equatorward direction by any

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Erica Rosenblum and Ian Eisenman

fall within the range of the ensemble of simulations. Modeling groups from around the world have contributed to each phase of the Coupled Model Intercomparison Project (CMIP). In the third phase (CMIP3; Meehl et al. 2007 ), virtually none of the models simulated a summer Arctic sea ice cover that diminished as fast as in the observations under historical natural and anthropogenic climate forcing ( Stroeve et al. 2007 ). However, Stroeve et al. (2007) suggested the possibility that the observed

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Yongli Zhang, Hao Wei, Youyu Lu, Xiaofan Luo, Xianmin Hu, and Wei Zhao

1. Introduction Since 1979, satellite observations have revealed significant variations of sea ice in the Arctic Ocean including the Beaufort Sea (BS; Rigor and Wallace 2004 ; Babb et al. 2016 ; Howell et al. 2016 ; Babb et al. 2019 ). Starting from the mid-1990s, the summer (September) ice edge in the Beaufort Sea has retreated northward rapidly ( Stroeve et al. 2005 ; Maslanik et al. 2007 ; Onarheim et al. 2018 ), accompanied with a sharp decrease in the coverage of multiyear ice (MYI

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Sungwook Hong and Inchul Shin

1. Introduction Sea ice is one of the most important parameters of the global climate system and covers a significant portion of the global oceans. Sea ice with its snow cover is an effective insulator that limits the exchange of energy and momentum between the ocean and the atmosphere ( Comiso et al. 2003 ). Satellite-board passive microwave sensors ( Zwally et al. 1983 ; Parkinson et al. 1987 ; Gloersen et al. 1992 ) have been observing global sea ice comprehensively and consistently. The

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