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; Emanuel and Nolan 2004 ; Emanuel 2010 ; Tippett et al. 2011 ; Bruyère et al. 2012 ; Camargo et al. 2014 ), making improvements and modifications on the original predictors by Gray. These modifications include using potential intensity instead of sea surface temperature (SST) ( Emanuel and Nolan 2004 ; Emanuel 2010 ), determining a threshold effect for vorticity ( Tippett et al. 2011 ), considering the saturation deficit of the midtroposphere instead of relative humidity ( Emanuel 2010 ; Camargo
; Emanuel and Nolan 2004 ; Emanuel 2010 ; Tippett et al. 2011 ; Bruyère et al. 2012 ; Camargo et al. 2014 ), making improvements and modifications on the original predictors by Gray. These modifications include using potential intensity instead of sea surface temperature (SST) ( Emanuel and Nolan 2004 ; Emanuel 2010 ), determining a threshold effect for vorticity ( Tippett et al. 2011 ), considering the saturation deficit of the midtroposphere instead of relative humidity ( Emanuel 2010 ; Camargo
Rossby waves that propagate into the extratropics and significantly modulate the extratropical circulation (e.g., Matthews et al. 2004 ; Seo and Son 2012 ). The MJO modulates various aspects of weather and climate including regional temperatures (e.g., Vecchi and Bond 2004 ), precipitation (e.g., Jones et al. 2004 ; Donald et al. 2006 ), atmospheric blocking (e.g., Henderson et al. 2016 ), hurricanes (e.g., Maloney and Hartmann 2000 ; Liebmann et al. 1994 ), and global monsoons ( Lorenz and
Rossby waves that propagate into the extratropics and significantly modulate the extratropical circulation (e.g., Matthews et al. 2004 ; Seo and Son 2012 ). The MJO modulates various aspects of weather and climate including regional temperatures (e.g., Vecchi and Bond 2004 ), precipitation (e.g., Jones et al. 2004 ; Donald et al. 2006 ), atmospheric blocking (e.g., Henderson et al. 2016 ), hurricanes (e.g., Maloney and Hartmann 2000 ; Liebmann et al. 1994 ), and global monsoons ( Lorenz and
likely to occur about 5–15 days after MJO phase 3, and a negative NAO is likely to occur after phase 7 ( Cassou 2008 ; Lin et al. 2009 ). The MJO can thus modulate midlatitude weather systems via modulating these teleconnection patterns. Henderson et al. (2016) found a significant decrease in eastern Pacific and Atlantic blocking events following MJO phase 3, and an increase following phase 7. Deng and Jiang (2011) found a poleward shift of North Pacific storm track about two weeks after MJO
likely to occur about 5–15 days after MJO phase 3, and a negative NAO is likely to occur after phase 7 ( Cassou 2008 ; Lin et al. 2009 ). The MJO can thus modulate midlatitude weather systems via modulating these teleconnection patterns. Henderson et al. (2016) found a significant decrease in eastern Pacific and Atlantic blocking events following MJO phase 3, and an increase following phase 7. Deng and Jiang (2011) found a poleward shift of North Pacific storm track about two weeks after MJO