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(total rain divided by number of days with rain), or frequency (number of days with rain divided by total number of days; not shown). Fig . 4. Values of R for each nonmodel product’s daily precipitation for each year vs WGEW: (top) gauge-based and satellite products and (bottom) reanalysis products. Following J. Liu et al. (2012) , Fig. 5 displays precipitation intensity of all of the products in five ranges: negligible (<0.1 mm day −1 ), drizzle (0.1–3 mm day −1 ), light (3–10 mm day −1
(total rain divided by number of days with rain), or frequency (number of days with rain divided by total number of days; not shown). Fig . 4. Values of R for each nonmodel product’s daily precipitation for each year vs WGEW: (top) gauge-based and satellite products and (bottom) reanalysis products. Following J. Liu et al. (2012) , Fig. 5 displays precipitation intensity of all of the products in five ranges: negligible (<0.1 mm day −1 ), drizzle (0.1–3 mm day −1 ), light (3–10 mm day −1
nocturnal peak for non-drizzle rainfall and both afternoon and nocturnal peaks for showery rainfall. Dai (2001) also shows that the afternoon rainfall peak is related to local instability as indicated by the presence of large values of convective available potential energy (CAPE). Using satellite brightness temperature as a proxy for rainfall, Yang and Slingo (2001) show that afternoon and evening rainfall peaks are dominant over West Africa and also explore connections with atmospheric instability
nocturnal peak for non-drizzle rainfall and both afternoon and nocturnal peaks for showery rainfall. Dai (2001) also shows that the afternoon rainfall peak is related to local instability as indicated by the presence of large values of convective available potential energy (CAPE). Using satellite brightness temperature as a proxy for rainfall, Yang and Slingo (2001) show that afternoon and evening rainfall peaks are dominant over West Africa and also explore connections with atmospheric instability
