Modeling Mesoscale Eddies Generated Over the Continental Slope, East Antarctica

Abstract

Mesoscale eddies are abundant over the Antarctic continental slope, with the potential to regulate the water masses transport, mixing, and energy transfer. Over the relatively cold and fresh shelf regions around the Antarctic margins, in the absence of dense overflows, the baroclinic instability of the Antarctic Slope Current is still favorable in the generation of mesoscale eddies. However, mesoscale eddies are barely observed over the fresh shelf regions due to the sparsity of in situ hydrographic observations. Based on an idealized eddy-resolving coupled ocean-ice shelf model, this study investigates the characteristics of mesoscale eddies and corresponding influences on the local hydrographic properties over the continental slope, East Antarctica. With the aid of an automated eddy detection algorithm, bowl-shaped eddies are identified from the simulated velocity vector geometry. The Cyclonic Eddies (CE) has a barotropic vertical structure extending to more than 2,500 m depth, while the vertical shear of the Anticyclonic Eddies (AE) velocity is strong at the upper 200 m layer. Mesoscale eddies can trap the cold and fresh water in the southern flank of the Antarctic slope front and flow offshore to the relatively warm and saline region. Therefore, the influences of eddies on the hydrographic properties are not only governed by the eddy polarities but also the eddy-induced heat and salt transport.

Interactions of Remotely Generated Internal Tides With the U.S. West Coast Continental Margin

“…Although continental margins (i.e., the ocean‐continent boundaries) occupy a modest proportion of the global ocean (28% by area; Symonds et al., 2000), they are highly relevant for numerous physical and bio‐geo‐chemical processes (e.g., Babu et al., 2002; Muller‐Karger et al., 2005; Townsend et al., 2004; Whitney et al., 2005). Water masses, sediments and nutrients in the continental margins are modulated by river discharges (e.g., Bianchi et al., 2010; Cohen et al., 2014; Hill et al., 2007; Lehrter et al., 2013; Mouyen et al., 2018), and by several oceanic processes such as mesoscale eddies (e.g., Chen et al., 2019; Yang et al., 2019; Zhang et al., 2022), submesoscale currents (e.g., Barkan et al., 2017; T. Wang et al., 2021), tidal and subtidal currents (e.g., Hermann et al., 2002; Spicer et al., 2021), hydraulic flows (e.g., Dorrell et al., 2016; Holland et al., 2002), and by internal waves (IWs, e.g., Friedrichs & Wrights, 1995; Miramontes et al., 2020; Villamaña et al., 2017).…”