Search Results

You are looking at 51 - 60 of 30,532 items for :

  • Boundary currents x
  • All content x
Clear All
Cyril Germineaud, Alexandre Ganachaud, Janet Sprintall, Sophie Cravatte, Gérard Eldin, Marion S. Alberty, and Emilien Privat

1. Introduction The low-latitude western boundary currents (LLWBCs) of the southwest Pacific establish a major connection between the subtropics and the equator ( McCreary and Lu 1994 ; Fine et al. 1994 ; Johnson and McPhaden 1999 ; Grenier et al. 2014 ). They cross the semienclosed Solomon Sea east of Papua New Guinea (PNG; Fig. 1a ) before redistributing waters to the equatorial band, where LLWBCs are considered to be an important component of the equatorial Pacific water mass budget

Full access
Shane Elipot, Chris Hughes, Sofia Olhede, and John Toole

, anomalies should also be distributed by advective means, either by the Deep Western Boundary Current (DWBC) or via interior routes, as partly evidenced by numerical simulations ( Zhang 2010 ), Lagrangian observations ( Bower et al. 2009 ), or water mass diagnostics ( Peña-Molino et al. 2011 ). Simultaneous observations of MOC variability as a function of time and latitude are lacking to verify these theoretical expectations, derived for idealized or approximated oceanic configurations. Furthermore, the

Full access
Alexandre Ganachaud, Lionel Gourdeau, and William Kessler

itself.) These two island groups form a broad channel about 500 km wide with the Loyalty Islands in between. Linear ocean dynamics require the incoming SEC waters to form boundary currents against the east side of islands or seamount ridges ( Godfrey 1989 ), which then cross the Coral Sea zonally as narrow currents ( Webb 2000 ). This “island rule” of Godfrey (1989) is a linear calculation that determines the net meridional wind-driven Sverdrup mass transport between an island and the coast to its

Full access
Stephanie Waterman, Nelson G. Hogg, and Steven R. Jayne

their interactions that are unprecedented in both their spatial and temporal resolution. It presents a unique opportunity to improve our understanding of the nature and importance of eddy–mean flow interactions in western boundary current (WBC) jet systems. A study of the role of eddies and their interaction with the mean flow in WBC jet systems is important because eddy variability likely plays a critical role in WBC jet dynamics. For example, we expect eddies and their nonlinear interactions to

Full access
Peter Brandt, Andreas Funk, Lars Czeschel, Carsten Eden, and Claus W. Böning

potential density range of LSW. The deep LC has a strong barotropic component and extends approximately out to the 3300-m depth contour ( Fischer et al. 2004 ). Offshore of the deep LC, several cyclonic recirculation cells exist that are associated with an interior anticyclonic circulation around the central Labrador Sea as well as a doming of the isopycnals off the boundary current ( Lavender et al. 2000 ). While there are different export routes of LSW out of the Labrador Sea, that is, into the

Full access
Matt C. Wilbanks, Sandra E. Yuter, Simon P. de Szoeke, W. Alan Brewer, Matthew A. Miller, Andrew M. Hall, and Casey D. Burleyson

context of the evolving mesoscale cloud and precipitation structures. Density currents occur in the atmosphere when cooler, negatively buoyant air descends to the surface, diverges, and propagates radially into the surrounding boundary layer. The dynamics that drive density current flows are very similar throughout a broad spectrum of interactions between fluids of different densities. The kinematic structure and evolution of density currents have been described extensively in both laboratory and

Full access
Renske Gelderloos, Caroline A. Katsman, and Sybren S. Drijfhout

by warming due to solar radiation in summer and lateral influx of heat from the boundary current. On average, about 60% of the total annual heat input over the upper 1600 m is provided by lateral heat fluxes ( Yashayaev and Loder 2009 ), but solar radiative warming is limited to the upper 200 m ( Straneo 2006a ). Furthermore, the fact that restratification already starts when the atmosphere is still cooling the ocean in early spring (generally in April) ( Lilly et al. 1999 ; Avsic et al. 2006

Full access
Volodymyr Zharkov and Doron Nof

. Under some conditions, the meanders grow exponentially, close upon themselves, and pinch off a closed loop with either cyclonic or anticyclonic circulation (depending on whether the meander is convex or concave, looking northward). Note that by “instability,” we refer to the classical definition, that is, the breakup of a known steady solution , not a mere transfer of energy from the mean flow to the eddy field—a definition sometimes used by numerical modelers. At times, western boundary currents

Full access
David P. Marshall and Claire E. Tansley

“triple deck” structure, in which the separation of the boundary layer is an integral component of the solution. An excellent review of the triple-deck theory of boundary layer separation is given by Smith (1982) . In the ocean there has been much recent interest in understanding the dynamics of boundary current separation, and in particular the separation of the Gulf Stream from the North American coastline at Cape Hatteras [see Dengg et al. (1996) and references therein]. However relatively

Full access
Joseph Pedlosky

; LaCasce 2004 ). However, in these earlier studies, the sinking was supposed to occur in boundary regions with significant vertical stratification. The importance of boundary mixing for the meridional overturning circulation has been emphasized by Marotzke (1997) and Marotzke and Scott (1999) . In each of these studies the zones of upwelling or sinking have been substantially stratified. In a recent paper ( Spall 2008 ), the downwelling induced by buoyancy loss in a boundary current was studied in

Full access