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El Nino $B$*$h$S(B La Nina $B$KBP$9$kBg@>MNBg5$3$MN7k9g7O$N1~Ez(B ($B6aK\(B $B4n8w(B) $BH/I=MW;](B :
$BE_5($K$*$1$k(BEl Nino$B$*$h$S(BLa Nina$B$NJQF0$H=U5($K$*$1$kG.BSKLBg@>MN$N3$LL(B $B?e29JQF0$H$N4V$K$O@5$NAj4X$,$"$k!#2a5n$N8&5f$G$O!"G.BSKLBg@>MN$K$*$1$k(B $B3$LL?e29JP:9$N7A@.$KBP$7(BENSO$B$KH<$&@xG.%U%i%C%/%9$NJQF0$,=EMW$G$"$j!"$3(B $B$N@xG.%U%i%C%/%9$N@.J,$H$7$FIwB.$NJQF0$,:G$b4sM?$9$k$3$H$r<($7$?!#$3(B $B$NIwB.$O(BPNA$B%Q%?!<%s$d(BWalker$B=[4D$H$$$C$?(BENSO $B$KH<$C$FJQF0$9$kBg5$=[4D>l(B $B$K$h$C$F7A@.$5$l$k$H9M$($i$l$F$$$k!#$7$+$7$J$,$i!":G6a$N%b%G%k8&5f$G$O(B $BBg5$3$MN4V$NHf<>:9$N8z2L$bG.BSKLBg@>MN$K$*$1$k3$LL?e29JP:9$N7A@.$K4sM?(B $B$7$F$$$k$3$H$r<(:6$7$F$*$j!"(BENSO$B$KH<$&G.BS0h$NBPN.7w5$29$NJQ2=$,G.BS0h$NHf(B $B<>:9$r%3%s%H%m!<%k$9$k$H$$$&%a%+%K%:%`(B(TT-mechanisum)$B$,Ds0F$5$l$?!#$^(B $B$?!"(BENSO$B$KH<$&Bg5$>l$NJQF0$O(BEl Nino $B$H(BLa Nina$B$G0[$J$k$3$H$b<(:6$5$l$F(B $B$*$j!"(BENSO$B$r(BEl Nino$B$H(BLa Nina$B$KJ,$1$F9M$($kI,MW$,$"$k!#$=$3$GK\8&5f$G$O!"(B $BG.%U%i%C%/%9$N3F@.J,$r8+@Q$b$j!"(BEl Nino$B$*$h$S(BLa Nina$B$,G.BSBg@>MN$NBg5$(B $B3$MN7O$K5Z$\$91F6A$K$D$$$F(BNCEP-NCAR$B:F2r@O$*$h$S(BGISST$B%G!<%?$rMQ$$$F8!F$(B $B$7$?!#(B ENSO$B$N1F6A$,:G$b82Cx$K8=$l$?NN0h$O%+%j%V3$$G$"$C$?!#%+%j%V3$$N3$LL?e29(B $BJP:9$O(B1$B7n$+$i(B2$B7n$K$+$1$F(BNino3$B$N3$LL?e29JQF0$HM-0U$J@5$NAj4X$H$J$j!"$[(B $B$\@xG.%U%i%C%/%9JP:9$G@bL@$G$-$k!#@xG.%U%i%C%/%9JP:9$N@.J,$H$7$F!"(BEl Nino$B$G$OBg5$3$MN4V$NHf<>:9$N8z2L$,:G$b4sM?$7$?$N$KBP$7!"(BLa Nina$B$G$OIw(B $BB.$N8z2L$,:G$b4sM?$7$?!#$3$N$h$&$J(BEl Nino$B$H(BLa Nina$B$K$h$k0c$$$O(BWalker$B=[(B $B4D$NG.E*$*$h$SNO3XE*9=B$$K$b$_$i$l!"(BEl Nino$B$H(BLa Nina$B$GG.BSBg@>MN$KBP$9(B $B$k6/@)%W%m%;%9$,0[$J$k$3$H$r<(:6$7$F$$$k!#(B Title : The responses of atmosphere-ocean system in the Atlantic associated with El Nino and La Nina. Abstract: Asymmetric remote influence between warm and cold phases of El Nino-Southern Oscillation (ENSO) on the tropical Atlantic sea surface temperature (SST) field is examined using NCEP-NCAR reanalysis and GISST datasets from 1948 to 1999. Regressed SST anomalies (SSTA) in the Caribbean Sea onto the Nino 3 SST index are significant during January-February period just after the mature phase of the ENSO cycle, and then persist for several months. In both of phases of the ENSO cycle, spatial structures of the composite SSTA are almost antisymmetric to one another, and correspond to those in surface latent heat flux anomalies, respectively. In the warm phases, changes in air-sea humidity difference are responsible for those heat flux changes. Whereas, in the cold phases, changes in scalar wind speed contribute as a major component to induce the latent heat flux anomalies. Thus the major atmospheric variables that induce changes in the latent heat flux are different between warm and cold phases of the ENSO in the Caribbean region. We will discuss associated changes of thermal and dynamical structures in Walker circulation to explain different ways of the remote influence between two phases of the ENSO cycle.
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