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Christopher C. Chapman and Rosemary Morrow

1. Introduction The circulation in the Southern Ocean is dominated by the Antarctic Circumpolar Current (ACC), which is composed of a series of strong, narrow eastward currents known as jets ( Rintoul et al. 2001 ). Jets are a common feature in geophysical fluids having been found in the midlatitude troposphere and stratosphere, in the atmospheres of gas giant planets, and numerous laboratory flows ( Thompson 2008 ). They consist of large-scale, predominantly zonal flow that persists with time

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Peter Hamilton and Antoine Badan

the slope topography. The interaction of a model anticyclonic eddy with a topographic slope that generates a subsurface jet is the main subject of their numerical study. DiMarco et al. (2004) discussed the possibility that high-speed subsurface currents could occur between 150- and 350-m depth, while surface currents remained weak. Drilling operators, as in the example given above, had reported cases of shutdowns caused by suspected high-speed subsurface flows, which have become known as jets

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Bo Qiu and Shuiming Chen

1. Introduction The Kuroshio Extension (KE) is an eastward-flowing inertial jet in the subtropical western North Pacific after the Kuroshio separates from the coast of Japan at 35°N, 140°E ( Fig. 1 ). Being the extension of a wind-driven western boundary current, the KE has long been recognized as a current system rich in large-amplitude meanders and energetic pinched-off eddies (e.g., Mizuno and White 1983 ; Qiu et al. 1991 ; Yasuda et al. 1992 , among others). An important feature emerging

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Toru Miyama, Humio Mitsudera, Hajime Nishigaki, and Ryo Furue

1. Introduction Recent studies have shown that two quasi-stationary jets exist along the subarctic frontal zone in the western North Pacific Ocean. Using satellite observations and hydrographic data, Isoguchi et al. (2006) identified two warm water tongues driven by these western and eastern quasi-stationary geostrophic jets: J1 and J2 in their paper. In this study, we focus on the western jet (J1), which we call the Western Isoguchi Jet. The existence of the Western Isoguchi Jet was also

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Lucia Bunge, Christine Provost, Bach Lien Hua, and Annie Kartavtseff

semiannual and annual signals are wind forced ( Brandt and Eden 2005 ). These signals are the result of vertically propagating Rossby and Kelvin waves (e.g., Thierry et al. 2004 ). Interannual variability is not as well documented. At least part of the interannual variability has been related to the so-called equatorial deep jets (EDJs), for which formation mechanisms are still not well understood. EDJs are characterized by vertically stacked alternating eastward and westward jets with small vertical

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Nathan Paldor and Yona Dvorkin

perturbations are nondivergent (a streamfunction exists). Our aim in this work is to reexamine Kuo’s theory of nondivergent flows on the β plane and to extend it numerically to divergent flows both on the β plane and on a rotating sphere in the framework of the shallow-water equations (SWEs). A brief summary of the assumptions and results of the relevant elements of Kuo’s classic theory is now in order. a. The β -plane barotropic instability theory for nondivergent perturbations on a cos 2 jet In his

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Carlowen A. Smith, Kevin G. Speer, and Ross W. Griffiths

carry a large fraction of the transport of the ACC, the Subantarctic Front (SAF) and the Polar Front (PF; e.g., Cunningham et al. 2003 ), but other fronts can have comparable transports in individual hydrographic sections. Numerous zonal jets in the ACC were dramatically resolved in the study of Sokolov and Rintoul (2007 , 2009) . Observational evidence is also growing that not only the ACC, but much of the deep ocean flow is permeated by zonal jets ( Nakano and Suginohara 2002 ; Treguier et al

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Madeleine K. Youngs and Gregory C. Johnson

1. Introduction Equatorial deep jets (EDJs) are equatorially trapped, stacked, zonal currents that alternate direction every few hundred meters in depth. The jets are present in all three ocean basins, throughout much of the water column ( Johnson et al. 2002 ; Johnson and Zhang 2003 ; Luyten and Swallow 1976 ). In recent years, the effects of the EDJs on water-mass property distributions have been studied in the Atlantic Ocean. For example, Schmid et al. (2005) find that EDJs affect zonal

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Talia Tamarin, James R. Maddison, Eyal Heifetz, and David P. Marshall

fundamental role in the dynamics of the large-scale circulation; for example, it is a leading-order term in the dynamics of the Southern Ocean (e.g., Johnson and Bryden 1989 ; Danabasoglu et al. 1994 ). While horizontal eddy momentum fluxes are less significant from a global perspective, they can play important roles in the dynamics of inertial jets. For example, they influence the dynamics of western boundary currents, where they are instrumental in transferring energy between the mean flow shear and

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S. M. Durski, R. M. Samelson, J. S. Allen, and G. D. Egbert

velocity vanished at days 0, 2.5, and 5; maximum upwelling-favorable wind occurred at day 1.25; and maximum downwelling-favorable wind occurred at day 3.75 in each 5-day period. The predominant circulation feature over the cycle is a southward alongshore jet that reaches 0.4 m s −1 on day 3 before weakening and disappearing under the influence of downwelling winds ( Fig. 1 ). The reverse, northward flow is significantly weaker. It develops earliest at the coast at about day 2.6 and largely remains

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