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Fig. 3. The 10-day average of south-north distributions of (a) the AIRS humidity at
1000 hPa (g/kg), (b) SST ( C), (c) latent heat flux from the ocean to the atmosphere
(w/m 2 ), (d) divergence calculated from the QuikSCAT surface wind (10 6 s), and
(e) TMI rain rate (mm/day) along 105 E-120 E during May 1-10 (solid thin line),
May 11-20 (dashed line), and May 21-30 (thick solid line) in 2003.
(Fig. 3(b)). This implies that the ocean and atmospheric physical
processes associated with development of the strong monsoon rainfall
tend to decrease the underlying SST, but to warm the SST in front of
the rainfall maximum.
(3) The decrease of the moisture in ABL in the southern SCS in middle
May (Fig. 3(a), dashed line) and in the northern SCS in late May
(Fig. 3(c), solid thick line) are concurrent with an increase of the latent
heat flux (Fig. 3(c)) relevant to a burst of westerly in these two regions
(Figs. 2(b) and (c), blue lines), indicating that the moisture change at
ABL is not attributed to the surface evaporation.
(4) While a strong convection maximum co-locates with a strong
convergence near the surface, convergence also occurs in front of the
 
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