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to SSTs in the North Atlantic. A second zonal mechanism, occurring at higher latitudes, can be identified using the December 500-mb geopotential height anomaly (calculated from the average over all Decembers during the final 10 yr of the FWF event). Figure 4c clearly indicates that the stationary planetary wave response induced by the cooling over the North Atlantic has a hemispheric impact with a Northern Hemisphere wavenumber 2 form. In other words, strong negative geopotential height
to SSTs in the North Atlantic. A second zonal mechanism, occurring at higher latitudes, can be identified using the December 500-mb geopotential height anomaly (calculated from the average over all Decembers during the final 10 yr of the FWF event). Figure 4c clearly indicates that the stationary planetary wave response induced by the cooling over the North Atlantic has a hemispheric impact with a Northern Hemisphere wavenumber 2 form. In other words, strong negative geopotential height
associated with the propagation of atmospheric planetary waves excited during El Niño, which may give rise to the Pacific–North American (PNA) pattern ( Straus and Shukla 2002 ). Recent studies on the dynamics of ENSO teleconnections have investigated the effects of transient eddies, diabatic cooling processes ( DeWeaver and Nigam 2004 ; Trenberth et al. 2002 ), and sources of nonlinear ENSO variability (e.g., Hannachi 2001 ; Wu and Hsieh 2004 ), all of which likely contribute to the development of
associated with the propagation of atmospheric planetary waves excited during El Niño, which may give rise to the Pacific–North American (PNA) pattern ( Straus and Shukla 2002 ). Recent studies on the dynamics of ENSO teleconnections have investigated the effects of transient eddies, diabatic cooling processes ( DeWeaver and Nigam 2004 ; Trenberth et al. 2002 ), and sources of nonlinear ENSO variability (e.g., Hannachi 2001 ; Wu and Hsieh 2004 ), all of which likely contribute to the development of
