Observed Spatio‐Temporal Variability of the Eddy‐Sea Ice Interactions in the Arctic Basin

Abstract

In the Arctic Basin, the ocean dynamics at mesoscale and submesoscale under sea ice are poorly quantified and understood. Here, we analyze comprehensive data sets from Ice Tethered Profilers and moorings from the Beaufort Gyre Observing System spanning the period 2004–2019 in order to characterize the space and time variations of the (sub)mesoscale flow. In seasonally ice‐covered regions, the dynamics in the surface layer is largely determined by the presence of sea ice, with an increased eddy kinetic energy and numerous eddies in summer. Beyond these regions, the influence of the sea ice conditions on the first order dynamics is less clear. A wavenumber spectra analysis of observations at the surface and at depth under the sea ice pack reveals that a large variety of regimes can be found, independently of the time and space variations of the sea ice conditions. Focusing on a census of individual eddies, and their potential signature in sea ice, we found that around 500 eddies can be detected in the subsurface layer over 2004–2019, including both submesoscale (radius between 3 and 10 km) and mesoscale (up to 80 km) structures. Based on simple scaling calculations, we quantify the dynamical or thermodynamical signature that these eddies may imprint at the surface. While they do not induce any significant heat flux and subsequent sea ice melt, subsurface eddies can induce a dynamic height anomaly of the order of a few centimetres, resulting into a surface vorticity anomaly strong enough to impact sea ice locally.

Scale‐Dependent Air‐Sea Exchange in the Polar Oceans: Floe‐Floe and Floe‐Flow Coupling in the Generation of Ice‐Ocean Boundary Layer Turbulence

“…That shift might modify Ekman pumping, ocean overturning, and freshwater storage in the Arctic Ocean (Wang et al., 2019; Wu et al., 2021). It also would alter sub‐ice‐surface oceanic eddy fields (Armitage et al., 2020) and mixed layer depths, which are regulated in part by frictional effects in the ice‐ocean boundary layer (Cassianides et al., 2023; Gupta et al., 2020; Manucharyan & Thompson, 2022; Meneghello et al., 2020; Ou & Gordon, 1986).…”