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averaged radiative fluxes observed by satellites to study the present-day meridional heat transport (MHT; e.g., Stone 1978 ; Trenberth and Caron 2001 ; Fasullo and Trenberth 2008 ). Some studies merge information from TOA fluxes and atmosphere or ocean reanalyses to provide a full description of the divergent energy transport in the both the atmosphere and the ocean (e.g., Trenberth and Solomon 1994 ; Trenberth and Stepaniak 2004 ). Most of these studies focus on the energy transport by the
averaged radiative fluxes observed by satellites to study the present-day meridional heat transport (MHT; e.g., Stone 1978 ; Trenberth and Caron 2001 ; Fasullo and Trenberth 2008 ). Some studies merge information from TOA fluxes and atmosphere or ocean reanalyses to provide a full description of the divergent energy transport in the both the atmosphere and the ocean (e.g., Trenberth and Solomon 1994 ; Trenberth and Stepaniak 2004 ). Most of these studies focus on the energy transport by the
more dense, quiescent lower layer of density ρ a ( Fig. 1b ). For this configuration, the transport is given by T = g ′ p h 2 /2 f , where h is the plume depth and g ′ p = g ( ρ a − ρ p )/ ρ a the reduced gravity. This frontal model has been extensively used in the development of theories and the scaling analysis of laboratory and numerical results ( Garvine 1999 ; Lentz and Helfrich 2002 ; Fong and Geyer 2002 ). Other studies have considered the transport of stratified fronts in the
more dense, quiescent lower layer of density ρ a ( Fig. 1b ). For this configuration, the transport is given by T = g ′ p h 2 /2 f , where h is the plume depth and g ′ p = g ( ρ a − ρ p )/ ρ a the reduced gravity. This frontal model has been extensively used in the development of theories and the scaling analysis of laboratory and numerical results ( Garvine 1999 ; Lentz and Helfrich 2002 ; Fong and Geyer 2002 ). Other studies have considered the transport of stratified fronts in the
1. Introduction Mesoscale eddies are one of the dominant processes in the ocean, with a typical length scale of dozens to hundreds of kilometers and a time scale of weeks to years. As revealed by many studies, mesoscale eddies play important roles in the transport of mass, salt, heat, and nutrients ( Amores et al. 2017 ; Berloff et al. 2002 ; Berloff and McWilliams 2002 , 2003 ; Dong et al. 2014 ; Holland 1978 ; Logerwell et al. 2001 ). Several studies have reported that mesoscale
1. Introduction Mesoscale eddies are one of the dominant processes in the ocean, with a typical length scale of dozens to hundreds of kilometers and a time scale of weeks to years. As revealed by many studies, mesoscale eddies play important roles in the transport of mass, salt, heat, and nutrients ( Amores et al. 2017 ; Berloff et al. 2002 ; Berloff and McWilliams 2002 , 2003 ; Dong et al. 2014 ; Holland 1978 ; Logerwell et al. 2001 ). Several studies have reported that mesoscale
fluxes (i.e., statistical correlations between velocity and tracer fluctuations, also known as Reynolds fluxes) play a significant role in the transport of heat, salt, momentum, and other tracers through the ocean. Because climate models generally do not resolve the mesoscale, the subgrid-scale mesoscale flux must be parameterized based on the large-scale flow properties, commonly using a diffusive closure ( Gent et al. 1995 ; Treguier et al. 1997 ; Visbeck et al. 1997 ; Vollmer and Eden 2013
fluxes (i.e., statistical correlations between velocity and tracer fluctuations, also known as Reynolds fluxes) play a significant role in the transport of heat, salt, momentum, and other tracers through the ocean. Because climate models generally do not resolve the mesoscale, the subgrid-scale mesoscale flux must be parameterized based on the large-scale flow properties, commonly using a diffusive closure ( Gent et al. 1995 ; Treguier et al. 1997 ; Visbeck et al. 1997 ; Vollmer and Eden 2013
1. Introduction In a stratified ocean, cross-isobath Ekman transport (associated with an along-isobath flow) causes vertical motions and therefore contributes to the development of a horizontal density gradient. In the initial stages of adjustment, turbulent mixing and dissipation are important; however, with time, a nonturbulent equilibrium can be established. Regardless of the upslope or downslope sense of the Ekman transport, the horizontal density gradient acts, through thermal wind balance
1. Introduction In a stratified ocean, cross-isobath Ekman transport (associated with an along-isobath flow) causes vertical motions and therefore contributes to the development of a horizontal density gradient. In the initial stages of adjustment, turbulent mixing and dissipation are important; however, with time, a nonturbulent equilibrium can be established. Regardless of the upslope or downslope sense of the Ekman transport, the horizontal density gradient acts, through thermal wind balance
1. Introduction Large-scale transport and mixing has a profound impact on the global distribution and chemistry of trace constituents in the atmosphere. In the upper troposphere and lower stratosphere (UTLS), a combination of large-scale, quasi-isentropic stirring and the eddy-driven meridional overturning ( Brewer 1949 ; Dobson 1956 ) is the main driver of global transport ( Plumb 2002 ; Haynes 2005 ; Shepherd 2007 ). Climate models represent these processes reasonably well, but the
1. Introduction Large-scale transport and mixing has a profound impact on the global distribution and chemistry of trace constituents in the atmosphere. In the upper troposphere and lower stratosphere (UTLS), a combination of large-scale, quasi-isentropic stirring and the eddy-driven meridional overturning ( Brewer 1949 ; Dobson 1956 ) is the main driver of global transport ( Plumb 2002 ; Haynes 2005 ; Shepherd 2007 ). Climate models represent these processes reasonably well, but the
distinct water masses, perhaps related to the winter and summer water masses on the Chukchi shelf ( Pickart et al. 2005 ). The heat and salt transported seaward by the most commonly observed eddies are believed to be fundamental to the ventilation of the interior Arctic halocline (e.g., Muench et al. 2000 ). These eddies also represent a source of nutrients and zooplankton to the central basin ( Llinas et al. 2008 ), and are potentially important for the off-shelf flux of organic carbon ( Mathis et al
distinct water masses, perhaps related to the winter and summer water masses on the Chukchi shelf ( Pickart et al. 2005 ). The heat and salt transported seaward by the most commonly observed eddies are believed to be fundamental to the ventilation of the interior Arctic halocline (e.g., Muench et al. 2000 ). These eddies also represent a source of nutrients and zooplankton to the central basin ( Llinas et al. 2008 ), and are potentially important for the off-shelf flux of organic carbon ( Mathis et al
evident. At 20 km offshore a large-wavelength wave is seen propagating onshore at about 0.3 m s −1 ; the leading edge of this wave appears to be borelike. A train of smaller-scale waves inshore at 1.5 km is aliased in our profiling observations. In both cases, the influence of the waves is clear throughout the water column. In winter, the water column is typically weakly stratified, from the combination of wind-driven mixing, onshore transport of light near-surface fluid in the upper Ekman layer, and
evident. At 20 km offshore a large-wavelength wave is seen propagating onshore at about 0.3 m s −1 ; the leading edge of this wave appears to be borelike. A train of smaller-scale waves inshore at 1.5 km is aliased in our profiling observations. In both cases, the influence of the waves is clear throughout the water column. In winter, the water column is typically weakly stratified, from the combination of wind-driven mixing, onshore transport of light near-surface fluid in the upper Ekman layer, and
1. Introduction The mean transport due to progressive waves here refers to the mean Lagrangian velocity generated by the waves. Longuet-Higgins (1953) presented a derivation of the mean Lagrangian transport, due to monochromatic waves, as an asymptotic series of averaged parcel paths and related the terms in the Lagrangian series to a series in the Eulerian framework. The asymptotic parameter was identified as the small distance traveled by a fluid parcel over a period of the wave motion. The
1. Introduction The mean transport due to progressive waves here refers to the mean Lagrangian velocity generated by the waves. Longuet-Higgins (1953) presented a derivation of the mean Lagrangian transport, due to monochromatic waves, as an asymptotic series of averaged parcel paths and related the terms in the Lagrangian series to a series in the Eulerian framework. The asymptotic parameter was identified as the small distance traveled by a fluid parcel over a period of the wave motion. The
1. Introduction The transport of heat is a fundamental phenomenon in planetary oceans and atmospheres. Transfer of heat from low to high latitudes has an intimate connection with nonuniform insolation, but its partitioning and variability stimulated decades of research and efforts to understand a surprisingly complex phenomenon. Outside of the tropics, a large fraction of heat transport is undertaken by the atmosphere ( Czaja and Marshall 2006 ; Trenberth and Caron 2001 ). Atmospheric heat
1. Introduction The transport of heat is a fundamental phenomenon in planetary oceans and atmospheres. Transfer of heat from low to high latitudes has an intimate connection with nonuniform insolation, but its partitioning and variability stimulated decades of research and efforts to understand a surprisingly complex phenomenon. Outside of the tropics, a large fraction of heat transport is undertaken by the atmosphere ( Czaja and Marshall 2006 ; Trenberth and Caron 2001 ). Atmospheric heat
