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On Characterizing Ocean Kinematics from Surface Drifters1. Introduction Measuring kinematic properties is of particular interest at submesoscales (0.1ā10 km length scales), where lateral buoyancy gradients are intensified by surface forcing, topographic interaction, frontogenesis, baroclinic instability, and turbulent thermal wind. Large local Rossby number Ro = Ī¶ / f ā¼ O ( 1 ) can be generated, where Ī¶ = Ļ x ā u y is the relative vorticity and f is the Coriolis frequency (e.g., Thomas etĀ al. 2008 ; McWilliams 2016 ), along with
1. Introduction Measuring kinematic properties is of particular interest at submesoscales (0.1ā10 km length scales), where lateral buoyancy gradients are intensified by surface forcing, topographic interaction, frontogenesis, baroclinic instability, and turbulent thermal wind. Large local Rossby number Ro = Ī¶ / f ā¼ O ( 1 ) can be generated, where Ī¶ = Ļ x ā u y is the relative vorticity and f is the Coriolis frequency (e.g., Thomas etĀ al. 2008 ; McWilliams 2016 ), along with
secondary low are identified from the horizontal and vertical velocity components and from the deformation profiles, depending on the considered area. The description of the system is consistent with the analysis of LemaƮtre et al. (1999) done using MANDOP. Moreover, an analysis of the deformation parameters indicates that frontogenesis occurs on the west side of the cloud head, and frontolysis occurs on its east side. This is in agreement with the temperature pattern of LemaƮtre et al. (1999) who
secondary low are identified from the horizontal and vertical velocity components and from the deformation profiles, depending on the considered area. The description of the system is consistent with the analysis of LemaƮtre et al. (1999) done using MANDOP. Moreover, an analysis of the deformation parameters indicates that frontogenesis occurs on the west side of the cloud head, and frontolysis occurs on its east side. This is in agreement with the temperature pattern of LemaƮtre et al. (1999) who
