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1. Introduction Submesoscale currents with a horizontal scale of O (0.1–50) km and a time scale of O (1) days are ubiquitous in the ocean. They occur preferentially near the surface of the ocean in the form of fronts, filaments and small-scale eddies, characterized by large variances of vertical velocity and vorticity ( Thomas et al. 2013 ; McWilliams 2016 ). Submesoscale processes can be generated through various mechanisms such as mixed layer instabilities (e.g., Boccaletti et al. 2007
1. Introduction Submesoscale currents with a horizontal scale of O (0.1–50) km and a time scale of O (1) days are ubiquitous in the ocean. They occur preferentially near the surface of the ocean in the form of fronts, filaments and small-scale eddies, characterized by large variances of vertical velocity and vorticity ( Thomas et al. 2013 ; McWilliams 2016 ). Submesoscale processes can be generated through various mechanisms such as mixed layer instabilities (e.g., Boccaletti et al. 2007
submesoscale-resolving simulations of a North Atlantic region between Greenland and Iceland and compute as we do the cross-scale energy flux using a Helmholtz decomposition. They find similar results to ours and conclude, with the help of an asymptotic theory, that the primary mechanism for the forward energy flux at fronts is frontogenesis. While frontogenesis is an effective means of transferring energy to smaller scales, other processes can be considered, such as ageostrophic frontal instabilities
submesoscale-resolving simulations of a North Atlantic region between Greenland and Iceland and compute as we do the cross-scale energy flux using a Helmholtz decomposition. They find similar results to ours and conclude, with the help of an asymptotic theory, that the primary mechanism for the forward energy flux at fronts is frontogenesis. While frontogenesis is an effective means of transferring energy to smaller scales, other processes can be considered, such as ageostrophic frontal instabilities
which its center diameter is around 5.1 mm. Like other types of disdrometers, it requires power and a shelter for its processor, which is linked to a personal computer. This limits site location choices when designing a study for the small-scale variability of DSDs. It is possible, however, to utilize a cable as long as 100 m between the sensor and processor, to provide some flexibility for the site selection. Considering the data processing, a registering raindrop is recorded on one of the 127
which its center diameter is around 5.1 mm. Like other types of disdrometers, it requires power and a shelter for its processor, which is linked to a personal computer. This limits site location choices when designing a study for the small-scale variability of DSDs. It is possible, however, to utilize a cable as long as 100 m between the sensor and processor, to provide some flexibility for the site selection. Considering the data processing, a registering raindrop is recorded on one of the 127
representation of processes related to thermodynamical feedbacks, for example, cloud feedbacks, water vapor feedback, and surface albedo feedbacks ( Colman 2003 ; Soden and Held 2006 ; Webb et al. 2006 ; Bony et al. 2006 ). However, other factors also affect the modeled climate sensitivity. In a previous study ( Seiffert and von Storch 2008 , hereafter SS08 ), we showed that the presence of enhanced small-scale fluctuations can affect the model’s sensitivity to a doubling of CO 2 concentration. Using
representation of processes related to thermodynamical feedbacks, for example, cloud feedbacks, water vapor feedback, and surface albedo feedbacks ( Colman 2003 ; Soden and Held 2006 ; Webb et al. 2006 ; Bony et al. 2006 ). However, other factors also affect the modeled climate sensitivity. In a previous study ( Seiffert and von Storch 2008 , hereafter SS08 ), we showed that the presence of enhanced small-scale fluctuations can affect the model’s sensitivity to a doubling of CO 2 concentration. Using
apparent wave–vortex decomposition is credible as a wave–vortex decomposition because the summertime submesoscale processes leading to vortex motions are relatively weak ( Callies et al. 2015 ) or probably have smaller length scales ( Dong et al. 2020 ) that cannot be well resolved here. But in the wintertime ML, the ageostrophic aspects of submesoscale eddies or fronts (i.e., USMs) may also importantly contribute to the divergent (apparent wave) components. This violates the assumption that horizontal
apparent wave–vortex decomposition is credible as a wave–vortex decomposition because the summertime submesoscale processes leading to vortex motions are relatively weak ( Callies et al. 2015 ) or probably have smaller length scales ( Dong et al. 2020 ) that cannot be well resolved here. But in the wintertime ML, the ageostrophic aspects of submesoscale eddies or fronts (i.e., USMs) may also importantly contribute to the divergent (apparent wave) components. This violates the assumption that horizontal
observations, continuously performed at two measurement stations to sample the MBL and FT during the 1-month period of the ACORES campaign, were combined with high-resolution helicopter-borne measurements of aerosol, cloud, turbulence, and radiation properties collected during 16 flights around Graciosa/Azores. This multilevel and multiscale approach has been exploited to investigate small-scale entrainment processes under cloudy and cloudless conditions with respect to the boundary layer and aerosol
observations, continuously performed at two measurement stations to sample the MBL and FT during the 1-month period of the ACORES campaign, were combined with high-resolution helicopter-borne measurements of aerosol, cloud, turbulence, and radiation properties collected during 16 flights around Graciosa/Azores. This multilevel and multiscale approach has been exploited to investigate small-scale entrainment processes under cloudy and cloudless conditions with respect to the boundary layer and aerosol
1. Introduction Lateral processes have frequently been invoked as potentially responsible for the excess restratification in the surface mixed layer (SML) that cannot be explained by solar insolation and vertical turbulent fluxes ( Brainerd and Gregg 1993a , 1997 ; Caldwell et al. 1997 ). Typically only 60% ± 15% of observed restratification in the SML can be attributed to the vertical divergence of penetrative solar radiation, with a much smaller proportion due to vertical divergence of
1. Introduction Lateral processes have frequently been invoked as potentially responsible for the excess restratification in the surface mixed layer (SML) that cannot be explained by solar insolation and vertical turbulent fluxes ( Brainerd and Gregg 1993a , 1997 ; Caldwell et al. 1997 ). Typically only 60% ± 15% of observed restratification in the SML can be attributed to the vertical divergence of penetrative solar radiation, with a much smaller proportion due to vertical divergence of
Observing Plumes and Overturning Cells with a New Coastal Bottom Driftermeasurements include physical parameters, such as temperature and salinity, as well as biological and chemical measurements. Moored instruments have made a general understanding of the frequency spectrum of currents throughout the water column; unfortunately, these sampling strategies are often unable to provide the sampling needed to assess large variability in both space and time. While models often neglect detailed bottom topography and associated small-scale flow that is forced by topography, they
measurements include physical parameters, such as temperature and salinity, as well as biological and chemical measurements. Moored instruments have made a general understanding of the frequency spectrum of currents throughout the water column; unfortunately, these sampling strategies are often unable to provide the sampling needed to assess large variability in both space and time. While models often neglect detailed bottom topography and associated small-scale flow that is forced by topography, they
implies an assumption about the scale selectivity of cold-pool formation. In fact, cold pools may form in very small terrain concavities or equally in broad mountain basins. Of course, a 4-km scale coincides with the driving NWP-model grid length, and valley features on a larger scale than this should start to become resolved, with cold-pooling processes beginning to be represented explicitly in the driving model. However, it is unclear at what point valleys and cold-pooling processes are effectively
implies an assumption about the scale selectivity of cold-pool formation. In fact, cold pools may form in very small terrain concavities or equally in broad mountain basins. Of course, a 4-km scale coincides with the driving NWP-model grid length, and valley features on a larger scale than this should start to become resolved, with cold-pooling processes beginning to be represented explicitly in the driving model. However, it is unclear at what point valleys and cold-pooling processes are effectively
OCTOI~ER 1983 JEAN-CLAUDE GASCARD AND R. ALLYN CLARKE 1779The Formation of Labrador Sea Water. Part II: Mesoscale and Smaller-Scale Processes JEAN-CLAUDE GASCARDLaboratoire d'Oc~anographie Physique du Museum National d'Histoire Naturelle, 75231, Paris, France R. ALLYN CLARKEAtlantic Oceanographic Laboratory, Bedford Institute of Oceanography, Dartmouth, N.S., Canada B2Y 4A
OCTOI~ER 1983 JEAN-CLAUDE GASCARD AND R. ALLYN CLARKE 1779The Formation of Labrador Sea Water. Part II: Mesoscale and Smaller-Scale Processes JEAN-CLAUDE GASCARDLaboratoire d'Oc~anographie Physique du Museum National d'Histoire Naturelle, 75231, Paris, France R. ALLYN CLARKEAtlantic Oceanographic Laboratory, Bedford Institute of Oceanography, Dartmouth, N.S., Canada B2Y 4A
