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  • Air–Sea Interactions from the Diurnal to the Intraseasonal during the PISTON, MISOBOB, and CAMP2Ex Observational Campaigns in the Tropics x
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Kenneth G. Hughes, James N. Moum, and Emily L. Shroyer

reduces to a counterclockwise path, a result that holds across the entire dataset (1). This pathway neatly illustrates the sequence shown by Moulin et al. (2018) . Nighttime convection leaves small N and comparatively large ϵ χ early in the day. The building diurnal stratification quenches ϵ χ as N increases. At depths below z T z max , there is warming by local absorption of solar radiation, but presumably negligible shear from the diurnal jet. This state may last several hours. On the

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Kenneth G. Hughes, James N. Moum, and Emily L. Shroyer

, consequently, shear because the now-warmed layer traps the momentum input from wind. Contours and current arrows are derived from an idealized simulation (see section 3 ). Termed the diurnal jet, the near-surface velocity anomaly has been observed to be 0.1–0.3 m s −1 ( Price et al. 1986 ; Kraus 1987 ; Sutherland et al. 2016 ; Shcherbina et al. 2019 ). By isolating the near surface, DWLs (and rain layers) make the surface slippery. For both types of layers, Shcherbina et al. (2019) showed that

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D. A. Cherian, E. L. Shroyer, H. W. Wijesekera, and J. N. Moum

altimeters by the Copernicus Marine Environment Monitoring Service (CMEMS). 2 Apart from the EICC, one other major circulation feature is the Summer or Southwest Monsoon Current (SMC). The SMC is visible in the seasonal mean during the SW monsoon as an eastward jet along 8°N between 85° and 92°E in Fig. 2d (vectors). Peak velocity in the SMC can exceed 1.5 m s −1 and northward transport has been estimated to be in the range 10–27 Sv (1 Sv ≡ 10 6 m 3 s −1 ), likely an overestimate due to the

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