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rule to the governing dynamics. Thus the signal, which originates as a sensitivity to the zonal velocity at Drake Passage, propagates backward in time via advection by the background state and wave dynamics throughout the ocean to be eventually damped by dissipation. The dynamics dictate that the sensitivity to the zonal velocity at Drake Passage has a signature in all model state variables and most forcing terms. The adjoint thus gives a response function of the Drake Passage transport at all
rule to the governing dynamics. Thus the signal, which originates as a sensitivity to the zonal velocity at Drake Passage, propagates backward in time via advection by the background state and wave dynamics throughout the ocean to be eventually damped by dissipation. The dynamics dictate that the sensitivity to the zonal velocity at Drake Passage has a signature in all model state variables and most forcing terms. The adjoint thus gives a response function of the Drake Passage transport at all
the zonal difference of the annular SLP pattern. The poleward and equatorward winds change alternately with the wave pattern. Fig . 12. Leading EOF modes of (a) zonal wind U (m s −1 ), (b) meridional wind V (m s −1 ), (c) SST ( T s , °C), and (d) SAT ( T a , °C) in the southern oceans during the austral winter. (e),(f) The PC1 of (e) U and SST and (f) V and SAT. Change of surface wind associated with SAM affects the ocean processes. The first EOF mode of SST ( Fig. 12c ) also shows a
the zonal difference of the annular SLP pattern. The poleward and equatorward winds change alternately with the wave pattern. Fig . 12. Leading EOF modes of (a) zonal wind U (m s −1 ), (b) meridional wind V (m s −1 ), (c) SST ( T s , °C), and (d) SAT ( T a , °C) in the southern oceans during the austral winter. (e),(f) The PC1 of (e) U and SST and (f) V and SAT. Change of surface wind associated with SAM affects the ocean processes. The first EOF mode of SST ( Fig. 12c ) also shows a
anomalous heat flux to the atmosphere, and it influences the large-scale atmospheric circulation through the propagation of stationary Rossby waves ( Honda et al. 1999 ). Although the Sea of Okhotsk is a marginal sea, the redistribution of heat and salt associated with the sea ice processes has a strong influence on the atmosphere and ocean on a hemispheric scale. 3. Methods and data A daily heat and salt flux dataset for 9 yr between 2002 and 2010 was created on the AMSR-E polar stereographic grid at a
anomalous heat flux to the atmosphere, and it influences the large-scale atmospheric circulation through the propagation of stationary Rossby waves ( Honda et al. 1999 ). Although the Sea of Okhotsk is a marginal sea, the redistribution of heat and salt associated with the sea ice processes has a strong influence on the atmosphere and ocean on a hemispheric scale. 3. Methods and data A daily heat and salt flux dataset for 9 yr between 2002 and 2010 was created on the AMSR-E polar stereographic grid at a
reduction (e.g., Porter et al. 2010 ). As noted in Cullather and Bosilovich (2011) , numerical reanalyses are widely used in polar research for evaluating polar processes, as boundary conditions for limited area atmosphere and ocean–sea ice models and as a first-order validation for climate models. However, reanalyses inevitably contain inaccuracies resulting from limitations in the observing system, inconsistencies between observing methods, and incomplete knowledge of the physical processes that are
reduction (e.g., Porter et al. 2010 ). As noted in Cullather and Bosilovich (2011) , numerical reanalyses are widely used in polar research for evaluating polar processes, as boundary conditions for limited area atmosphere and ocean–sea ice models and as a first-order validation for climate models. However, reanalyses inevitably contain inaccuracies resulting from limitations in the observing system, inconsistencies between observing methods, and incomplete knowledge of the physical processes that are
