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Kate Snow, Andrew McC. Hogg, Bernadette M. Sloyan, and Stephanie M. Downes

Atlantic Ocean, with zonally reentrant boundary conditions at Drake Passage latitudes to permit a representative Antarctic Circumpolar Current (ACC) flow. Within these boundaries the domain is deformed laterally to fit a 60°-wide sector with matching conditions set at the periodic boundaries ( Fig. 1 ). The Modular Ocean Model, version 5 (MOM5; Griffies 2012 ), provides the ocean component of the model and is coupled to the GFDL sea ice simulator (SIS; Winton 2000 ). Version 2 of CORE phase 2 (CORE2v

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Robert A. Tomas, Clara Deser, and Lantao Sun

the same). The SST, precipitation, and SLP responses in ICE21_SOM_ΔQ are shown in Fig. 7 . Note that these response patterns are shaped by thermodynamic air–sea interaction, although they originate from dynamical ocean changes. The SST response shows, not surprisingly, that ocean heat transport changes in response to Arctic sea ice loss act to cool the NH and warm the SH ( Fig. 7a ). The NH cooling is strongest in the midlatitudes and in the vicinity of the western boundary currents and their

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Bradford S. Barrett, Gina R. Henderson, and Joshua S. Werling

et al. 2015 ). Given the role spring snow plays in a wide range of current and time-lagged atmospheric and hydrologic processes, it is critical to understand its variability on the intraseasonal time scale. Three publicly available datasets are used to establish these connections between the MJO and snow depth. They are each described below. a. Atmospheric data To explore the state of the atmosphere under different lagged phases of the MJO, both at the surface and midtropospheric levels

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Changhyun Yoo, Sungsu Park, Daehyun Kim, Jin-Ho Yoon, and Hye-Mi Kim

concentration. For our simulations, such boundary conditions are prescribed for 27 yr from January 1979 to December 2005. In this study we focus on December–February (DJF), the boreal winter season in which the MJO and its teleconnection to the extratropics are the most pronounced. Identical settings are used except for the choice of convective parameterization schemes. One simulation uses the default shallow ( Park and Bretherton 2009 ) and deep ( Zhang and McFarlane 1995 ) convection schemes in the CAM5

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Xiaojun Yuan, Michael R. Kaplan, and Mark A. Cane

wave train emanating from the tropics leads a high SLP anomaly in the southeast Pacific. Because of the warm SST, the Hadley cell is enhanced and contracted in the South Pacific while weakened and expanded in the South Atlantic. It results in the jet stream moving equatorward in the Pacific but poleward in the Atlantic. This change in the jet stream leads to the changes of storm distribution. Driven by the Antarctic Circumpolar Current (ACC) and air–sea interactions, some ADP anomalies propagate

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