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discusses the tropospheric responses emphasizing the modulation of local and downstream adjustments of extratropical weather systems and their aspects related to climate change. Section 4 probes into the oceanic responses due to thermal and mechanical feedback processes. The section emphasizes the need to develop new theories and parameterizations to account for rectified effects of eddy–atmosphere interaction. Section 5 explores the emerging observational platforms critical for accurate in situ and
discusses the tropospheric responses emphasizing the modulation of local and downstream adjustments of extratropical weather systems and their aspects related to climate change. Section 4 probes into the oceanic responses due to thermal and mechanical feedback processes. The section emphasizes the need to develop new theories and parameterizations to account for rectified effects of eddy–atmosphere interaction. Section 5 explores the emerging observational platforms critical for accurate in situ and
( Longuet-Higgins et al. 1967 ; Domaracki and Loesch 1977 ; Majda et al. 1999 ; Holm and Lynch 2002 ; Raupp and Silva Dias 2009 ; Ripa 1982 , 1983a , b ). The present study applies both multiscale methods and nonlinear wave interaction theory to formulate a model capable of describing scale interactions in a simplified coupled atmosphere–ocean system. The multiscale method adopted here is similar to that adopted by Majda and Klein (2003) for the atmosphere. Thus, our approach can be regarded as
( Longuet-Higgins et al. 1967 ; Domaracki and Loesch 1977 ; Majda et al. 1999 ; Holm and Lynch 2002 ; Raupp and Silva Dias 2009 ; Ripa 1982 , 1983a , b ). The present study applies both multiscale methods and nonlinear wave interaction theory to formulate a model capable of describing scale interactions in a simplified coupled atmosphere–ocean system. The multiscale method adopted here is similar to that adopted by Majda and Klein (2003) for the atmosphere. Thus, our approach can be regarded as
mixing and upwelling of the ocean, which cool the sea surface ( Sun et al. 2015 ; Yablonsky and Ginis 2009 ). Changes in SST can in turn affect TC intensification via the enthalpy fluxes within an effective radius (e.g., Miyamoto and Takemi 2010 ; Xu and Wang 2010 ). The dynamic processes of TC–ocean interactions in the coupling system have been investigated in detail using ocean–atmosphere coupled models (e.g., Chen et al. 2007 ; Lee and Chen 2012 , 2014 ; Li and Huang 2018 , 2019 ; Lin et
mixing and upwelling of the ocean, which cool the sea surface ( Sun et al. 2015 ; Yablonsky and Ginis 2009 ). Changes in SST can in turn affect TC intensification via the enthalpy fluxes within an effective radius (e.g., Miyamoto and Takemi 2010 ; Xu and Wang 2010 ). The dynamic processes of TC–ocean interactions in the coupling system have been investigated in detail using ocean–atmosphere coupled models (e.g., Chen et al. 2007 ; Lee and Chen 2012 , 2014 ; Li and Huang 2018 , 2019 ; Lin et
approximately linear relationships between the surface stress curl (divergence) and the crosswind (downwind) components of the local SST gradient. Recent studies also highlight how a mesoscale SST front may have an impact all the way up to the troposphere ( Minobe et al. 2008 ). The effect of oceanic currents is another aspect of interaction between atmosphere and ocean; however, its effects are not yet well known. Some work shows that the current effect on the surface stress can lead to a reduction of the
approximately linear relationships between the surface stress curl (divergence) and the crosswind (downwind) components of the local SST gradient. Recent studies also highlight how a mesoscale SST front may have an impact all the way up to the troposphere ( Minobe et al. 2008 ). The effect of oceanic currents is another aspect of interaction between atmosphere and ocean; however, its effects are not yet well known. Some work shows that the current effect on the surface stress can lead to a reduction of the
that further modulate the underlying atmosphere–ocean interactions. Spring and summer TP heating anomalies cause large-scale Asian–Pacific Oscillation (APO) teleconnection responses over the extratropical Asian–North Pacific sector ( Nan et al. 2009 ; Zhou et al. 2009 ; Zhao et al. 2011 ; S. Liu et al. 2017 ), and affect SST patterns over the North Pacific through interactions among the North Pacific subtropical high, the Hadley circulation, and the intertropical convergence zone (ITCZ) over the
that further modulate the underlying atmosphere–ocean interactions. Spring and summer TP heating anomalies cause large-scale Asian–Pacific Oscillation (APO) teleconnection responses over the extratropical Asian–North Pacific sector ( Nan et al. 2009 ; Zhou et al. 2009 ; Zhao et al. 2011 ; S. Liu et al. 2017 ), and affect SST patterns over the North Pacific through interactions among the North Pacific subtropical high, the Hadley circulation, and the intertropical convergence zone (ITCZ) over the
, sea ice reductions can serve as a response to the atmospheric forcing ( Park et al. 2015 ). For example, sea ice reductions can be induced by warm air from the lower latitudes, which can cause an increase in the surface downward longwave radiation and the surface downward THF. Therefore, analysis of the simultaneous relationship between the anomalies of the SIC and the surface THF in situ can provide physical insight into the predominant direction of the atmosphere–ocean–ice interaction, which can
, sea ice reductions can serve as a response to the atmospheric forcing ( Park et al. 2015 ). For example, sea ice reductions can be induced by warm air from the lower latitudes, which can cause an increase in the surface downward longwave radiation and the surface downward THF. Therefore, analysis of the simultaneous relationship between the anomalies of the SIC and the surface THF in situ can provide physical insight into the predominant direction of the atmosphere–ocean–ice interaction, which can
1. Introduction Interactions between the atmosphere and ocean play a crucial role in redistributing energy, thereby maintaining the energy balance of the climate system. Here, we study the compensation between the atmosphere’s and ocean’s heat transport variations. It influences large-scale dynamics by reshaping the energy budget. Many efforts have been made to determine heat transport. In the 1960s, Jacob Bjerknes suggested that energy transport in the atmosphere and ocean should compensate
1. Introduction Interactions between the atmosphere and ocean play a crucial role in redistributing energy, thereby maintaining the energy balance of the climate system. Here, we study the compensation between the atmosphere’s and ocean’s heat transport variations. It influences large-scale dynamics by reshaping the energy budget. Many efforts have been made to determine heat transport. In the 1960s, Jacob Bjerknes suggested that energy transport in the atmosphere and ocean should compensate
adjustment in the ocean–atmosphere system, which produces time-dependent oscillations at periods ranging from intraseasonal to subannual time scales ( Sobel and Gildor 2003 ; Maloney and Sobel 2007 ). Most previous studies on hot spots were based on either monthly analyses or numerical experiments. Observational evidence of the air–sea interactions on short time scales during hot spot evolution remains inconclusive. A possible cause is that the detection of fast-evolving SST, surface fluxes, atmospheric
adjustment in the ocean–atmosphere system, which produces time-dependent oscillations at periods ranging from intraseasonal to subannual time scales ( Sobel and Gildor 2003 ; Maloney and Sobel 2007 ). Most previous studies on hot spots were based on either monthly analyses or numerical experiments. Observational evidence of the air–sea interactions on short time scales during hot spot evolution remains inconclusive. A possible cause is that the detection of fast-evolving SST, surface fluxes, atmospheric
nonlinear models and also to configurations where the “Brownian particle” is some “slow” property of a system. The case considered here: the dynamics of two two-dimensional layers of fluid, in turbulent motion, coupled by frictional forces at their interface, is conceptually similar. When the mass (per unit area) in the lower layer (ocean) is much higher than in the upper layer (atmosphere), the interactions resemble those of a heavy Brownian particle surrounded by light molecules. The atmospheric
nonlinear models and also to configurations where the “Brownian particle” is some “slow” property of a system. The case considered here: the dynamics of two two-dimensional layers of fluid, in turbulent motion, coupled by frictional forces at their interface, is conceptually similar. When the mass (per unit area) in the lower layer (ocean) is much higher than in the upper layer (atmosphere), the interactions resemble those of a heavy Brownian particle surrounded by light molecules. The atmospheric
resolving ocean eddies enhances the realism in depicting air–sea interaction. To test this hypothesis, we repeat the local-LIM analysis using two recent coupled GCM simulations from CCSM3.5 ( Gent et al. 2010 ) that only differ in their oceanic model resolution. The HR (LR) simulation has an ocean model resolution of 0.1° (1.0°); both employ the 0.5° Community Atmosphere Model, version 3, for the atmosphere. Note the HR allows for oceanic eddies, which are parameterized by the large-scale flow in the LR
resolving ocean eddies enhances the realism in depicting air–sea interaction. To test this hypothesis, we repeat the local-LIM analysis using two recent coupled GCM simulations from CCSM3.5 ( Gent et al. 2010 ) that only differ in their oceanic model resolution. The HR (LR) simulation has an ocean model resolution of 0.1° (1.0°); both employ the 0.5° Community Atmosphere Model, version 3, for the atmosphere. Note the HR allows for oceanic eddies, which are parameterized by the large-scale flow in the LR
