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  • Water budget/balance x
  • 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

radiation, 50–100 W m −2 for latent heat, and 1–2 W m −2 for sensible heat. The solar radiative flux averaged between 0700 and 1700 LT is from −400 to −600 W m −2 . Consequently, subsurface turbulent mixing is a major component in the surface heat budget, second only to absorption of solar radiation. However, when wind speeds are insufficiently strong to promote mixing, the heat tendency is a balance between solar radiation and surface heat loss to the atmosphere. This low-wind state has also been

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Jai Sukhatme, Dipanjan Chaudhuri, Jennifer MacKinnon, S. Shivaprasad, and Debasis Sengupta

Klymak et al. (2015) , we have added GM spectra to Fig. 4a . In fact, it is difficult to assess the contribution of internal waves near the ocean surface, where waves become evanescent in the mixed layer. It is thus unclear which stratification value would be appropriate to use for estimating the component of a GM spectrum that would be present in this depth range. Here we have used N = 0.02 s −1 , which is a typical averaged value over the top few hundred meters of the water column (GM estimates

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Corinne B. Trott, Bulusu Subrahmanyam, Heather L. Roman-Stork, V. S. N. Murty, and C. Gnanaseelan

, reanalysis products, and model simulations. Then, the identified events are dynamically investigated, first with the 30–90-day events, then the 10–20-day events, and then the 3–7-day events. We conclude our results by conducting a heat budget and salt budget analysis to understand the overall effect of each dynamical process on the BoB. The manuscript is organized as follows. Section 2 describes the datasets and methodology for studying ISOs. Section 3 explains our results. Section 4 summarizes the

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

end of the SW monsoon and the freshwater is eventually exported out along the Bay’s western and eastern margins ( Sengupta et al. 2006 ). The exported water is saline with S ≈ 34–35 psu. Hence maintaining the Bay’s long term salt balance requires both an inflow of salty water from outside the Bay and the upward turbulent transport of that imported salt so as to permanently modify the near-surface freshwater ( Vinayachandran et al. 2013 ). The western half of the north Indian Ocean, the Arabian

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