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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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Jacob O. Sewall

the climate system, including atmospheric CO 2 concentrations, were held constant) of a reduction in Arctic sea ice cover of up to 50%. That study was similar to other work investigating the impact of prescribed changes in Arctic ice cover on climate in an atmospheric GCM ( Rind et al. 1995 ; Alexander et al. 2004 ; Deser et al. 2004 ; Magnusdottir et al. 2004 ). However, unlike Deser et al. ( Deser et al. 2004 ) and Magnusdottir et al. ( Magnusdottir et al. 2004 ), Sewall and Sloan ( Sewall

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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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Till J. W. Wagner and Ian Eisenman

1. Introduction Arctic sea ice is undergoing a striking, closely monitored, and highly publicized decline. A recurring theme in the debate surrounding this decline is the question of how stable the ice cover is, and specifically whether it can become unstable. This question is often linked to the ice–albedo feedback, which is expected to play a key role in the observed sea ice retreat. The ice–albedo feedback has been studied since at least the nineteenth century, when Croll (1875

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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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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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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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Yueng-Djern Lenn, Tom P. Rippeth, Chris P. Old, Sheldon Bacon, Igor Polyakov, Vladimir Ivanov, and Jens Hölemann

et al. 1981 ). Consequently, Arctic halocline formation theories have focused on mechanisms for diapycnal and lateral mixing of the shelf and oceanic waters (e.g., Rudels et al. 2000 ; Woodgate et al. 2005 ; Shimada et al. 2005 ; Itoh et al. 2007 ). These halocline formation and maintenance mechanisms are critical to Arctic upper-ocean stratification that in turn influences Arctic circulation, sea ice, and climate. Mixing between the different water masses during halocline formation is

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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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