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northern Australia, with “monsoon” versus “break” convection taking on characteristics of the maritime versus continental archetypes, respectively ( Rutledge et al. 1992 ; Williams et al. 1992 ; Randell et al. 1994 ; May and Ballinger 2007 ; May et al. 2008 ). These are but a few of the many examples of variability in convective structure seen throughout the tropics ( Houze and Cheng 1977 ; Zipser 1994 ; DeMott and Rutledge 1998 ; Johnson et al. 1999 ; Nesbitt et al. 2000 ; Petersen and
northern Australia, with “monsoon” versus “break” convection taking on characteristics of the maritime versus continental archetypes, respectively ( Rutledge et al. 1992 ; Williams et al. 1992 ; Randell et al. 1994 ; May and Ballinger 2007 ; May et al. 2008 ). These are but a few of the many examples of variability in convective structure seen throughout the tropics ( Houze and Cheng 1977 ; Zipser 1994 ; DeMott and Rutledge 1998 ; Johnson et al. 1999 ; Nesbitt et al. 2000 ; Petersen and
. E. Barndorff-Nielsen et al., Eds., World Scientific, 25–72 . Georgakakos, K. P. , and Krajewski W. F. , 1996 : Statistical-microphysical causes of rainfall variability in the tropics. J. Geophys. Res. , 101 , (D21) . 26165 – 26180 . 10.1029/96JD01613 Groisman, P. Ya , Knight R. W. , Karl T. R. , Easterling D. R. , Sun B. , and Lawrimore J. H. , 2004 : Contemporary changes of the hydrological cycle over the contiguous United States: Trends derived from in situ observations
. E. Barndorff-Nielsen et al., Eds., World Scientific, 25–72 . Georgakakos, K. P. , and Krajewski W. F. , 1996 : Statistical-microphysical causes of rainfall variability in the tropics. J. Geophys. Res. , 101 , (D21) . 26165 – 26180 . 10.1029/96JD01613 Groisman, P. Ya , Knight R. W. , Karl T. R. , Easterling D. R. , Sun B. , and Lawrimore J. H. , 2004 : Contemporary changes of the hydrological cycle over the contiguous United States: Trends derived from in situ observations
1992 ; Nakazawa and Rajendran 2007 ). We selected four atmospheric variables as input for SOM: 850-hPa equivalent-potential temperature θ e , 850-hPa zonal and meridional wind, and 200-hPa geopotential height GH anomalies. The variable θ e is a thermodynamic parameter involving both temperature and humidity, and its low-level advection to the region from the tropics can significantly intensify rainfall over the baiu front. Previous studies (e.g., Ninomiya 2000 ; Ninomiya and Shibagaki 2007
1992 ; Nakazawa and Rajendran 2007 ). We selected four atmospheric variables as input for SOM: 850-hPa equivalent-potential temperature θ e , 850-hPa zonal and meridional wind, and 200-hPa geopotential height GH anomalies. The variable θ e is a thermodynamic parameter involving both temperature and humidity, and its low-level advection to the region from the tropics can significantly intensify rainfall over the baiu front. Previous studies (e.g., Ninomiya 2000 ; Ninomiya and Shibagaki 2007
the mountainous U.S. west coast. The more intense precipitation events are related to “atmospheric rivers” ( Zhu and Newell 1998 ), narrow plumes of moisture associated with fronts on oceanic cyclones ( Bao et al. 2006 ). These enhanced bands of vertically integrated water vapor typically form as the result of local moisture convergence ( Bao et al. 2006 ). Under a subset of environmental conditions, the moisture can be traced back from the U.S. west coast to the tropics ( Bao et al. 2006 ). These
the mountainous U.S. west coast. The more intense precipitation events are related to “atmospheric rivers” ( Zhu and Newell 1998 ), narrow plumes of moisture associated with fronts on oceanic cyclones ( Bao et al. 2006 ). These enhanced bands of vertically integrated water vapor typically form as the result of local moisture convergence ( Bao et al. 2006 ). Under a subset of environmental conditions, the moisture can be traced back from the U.S. west coast to the tropics ( Bao et al. 2006 ). These
