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The sea surface temperature(SST)anomaly of the eastern Indian Ocean(EIO)exhibits cold anomalies in the boreal summer or fall during El Ni(?)o development years and warm anomalies in winter or spring following the El Ni(?)o events.There also tend to be warm anomalies in the boreal summer or fall during La Ni(?)a development years and cold anomalies in winter or spring following the La Ni(?)a events.The seasonal phase-locking of SST change in the EIO associated with El Ni(?)o/Southern Oscillation is linked to the variability of convection over the maritime continent,which induces an atmospheric Rossby wave over the EIO.Local air-sea interaction exerts different effects on SST anomalies,depending on the relationship between the Rossby wave and the mean flow related to the seasonal migration of the buffer zone,which shifts across the equator between summer and winter. The summer cold events start with cooling in the Timor Sea,together with increasing easterly flow along the equator.Negative SST anomalies develop near Sumatra,through the interaction between the atmospheric Rossby wave and the underneath sea surface.These SST anomalies are also contributed to by the increased upwelling of the mixed layer and the equatorward temperature advection in the boreal fall.As the buffer zone shifts across the equator towards boreal winter,the anomalous easterly flow tends to weaken the mean flow near the equator,and the EIO SST increases due to the reduction of latent heat flux from the sea surface.As a result,wintertime SST anomalies appear with a uniform and nearly basin-wide pattern beneath the easterly anomalies.These SST anomalies are also caused by the increase in solar radiation associated with the anticyclonic atmospheric Rossby wave over the EIO.Similarly,the physical processes of the summer warm events,which are followed by wintertime cold SST anomalies,can be explained by the changes in atmospheric and oceanic fields with opposite signs to those anomalies described above.
The sea surface temperature (SST) anomaly of the eastern Indian Ocean (EIO) exhibits cold anomalies in the boreal summer or fall during El Ni (?) O development years and warm anomalies in winter or spring the the El Ni (?) O events .There also tend to be warm anomalies in the boreal summer or fall during La Ni (?) A development years and cold anomalies in winter or spring following the La Ni (?) A events. Seasonal period-locking of SST change in the EIO associated with El Ni (?) O / Southern Oscillation is linked to the variability of convection over the maritime continent, which induces an atmospheric Rossby wave over the EIO. Local air-sea interaction exerts different effects on SST anomalies, depending on the relationship between the Rossby wave and the mean flow related to the seasonal migration of the buffer zone, which shifts across the equator between summer and winter. The summer cold events start with cooling in the Timor Sea, together with increasing easterly flow along the equator. Negativ e SST anomalies develop near Sumatra, through the interaction between the atmospheric Rossby wave and the underneath sea surface. se SST anomalies are also contributed to by the increased upwelling of the mixed layer and the equatorward temperature advection in the boreal fall. As the buffer zone shifts across the equator towards boreal winter, the anomalous easterly flow tends to weaken the mean flow near the equator, and the EIO SST increases due to the reduction of latent heat flux from the sea surface. As a result, wintertime SST anomalies appear with a uniform and nearly basin-wide pattern beneath the easterly anomalies. the SST anomalies are also caused by the increase in solar radiation associated with the anticyclonic atmospheric Rossby wave over the EIO.Similarly, the physical processes of the summer warm events, which are followed by wintertime cold SST anomalies, can be explained by the changes in atmospheric and oceanic fields with opposite signs to those anomalies described abovOh.