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. More recently, O’Reilly and Czaja (2015) produced a more accurate KE index derived from a maximum covariance analysis between SST and SSH gradient observations, but SST observations with high spatial resolution were only available since June 2002, so that a longer KE index (1992–2011) was obtained by projecting the 2002–11 SSH spatial pattern onto the full SSH record. It is thus of interest to use data with higher temporal resolution that describe the KE variability over a longer duration, so
. More recently, O’Reilly and Czaja (2015) produced a more accurate KE index derived from a maximum covariance analysis between SST and SSH gradient observations, but SST observations with high spatial resolution were only available since June 2002, so that a longer KE index (1992–2011) was obtained by projecting the 2002–11 SSH spatial pattern onto the full SSH record. It is thus of interest to use data with higher temporal resolution that describe the KE variability over a longer duration, so
observations shows a distinct SLP trough along the KE ( Tanimoto et al. 2011 ). Enhanced surface wind convergence due to the vertical mixing effect and/or hydrostatic effect can locally strengthen upward motion, which can reach the midtroposphere in many occasions, enhancing cloud formation and precipitation ( Minobe et al. 2008 , 2010 ; Tokinaga et al. 2009 ; Frenger et al. 2013 ; Masunaga et al. 2015 ). Westward-propagating wind-forced oceanic Rossby waves are shown to play an important role in
observations shows a distinct SLP trough along the KE ( Tanimoto et al. 2011 ). Enhanced surface wind convergence due to the vertical mixing effect and/or hydrostatic effect can locally strengthen upward motion, which can reach the midtroposphere in many occasions, enhancing cloud formation and precipitation ( Minobe et al. 2008 , 2010 ; Tokinaga et al. 2009 ; Frenger et al. 2013 ; Masunaga et al. 2015 ). Westward-propagating wind-forced oceanic Rossby waves are shown to play an important role in
