Search Results

You are looking at 101 - 110 of 806 items for :

  • Journal of Physical Oceanography x
  • All content x
Clear All
Ryo Furue, Kévin Guerreiro, Helen E. Phillips, Julian P. McCreary Jr., and Nathaniel L. Bindoff

determined from CARS. We conclude by reporting volume budgets that demonstrate the linkages among these currents. a. Leeuwin Current 1) Horizontal structure Figure 3 illustrates the horizontal structure of the near-surface, annual-mean flow field offshore from WA, plotting depth integrals of from d LC to the surface (arrows) and indicating their meridional components (shading). There are two sources of water for the LC. One source is a southward inflow from the tropics (visible between 113° and 114

Full access
D. B. Enfield and J. S. Allen

sea level, coastal sea surface temperatureand alongshore wind stress for the eastern Pacific Ocean during the period 1950-74 have beenstudied. Sea level and temperature records from Yakutat, Alaska (59-N) to Valparaiso, Chile(33-S) and computed alongshore wind stress at near coastal grid points from Yakutat to Matzatlan,Mexico (23-N) have been utilized. The positive and negative sea level anomalies, corresponding toE1 Nifio-anti El Nifio cycles, are well correlated throughout the tropics of both

Full access
James A. Carton, Gennady Chepurin, and Xianhe Cao

comprehensive discussions of the alternatives in formulating updating algorithms. Malonote-Rizzoli (1996) reviews many current implementations. The general circulation ocean model on which our analysis is based uses the full Geophysical Fluid Dynamics Laboratory Modular Ocean Model 2.b primitive equation code, with conventional choices for mixing, etc. The domain of this analysis is global, extending from 62°S to 62°N. The model horizontal resolution is 2.5° × 0.5° in the Tropics, expanding to a uniform 2

Full access
Ryan M. Holmes, Jan D. Zika, and Matthew H. England

1. Introduction The ocean plays a critical role in the climate system by transferring heat from the tropics to higher latitudes ( Trenberth and Caron 2001 ) and from the surface to depth ( Gregory 2000 ). How this heat transport may change in response to future changes in surface forcing, both due to anthropogenic influences ( Trenberth et al. 2014 ) and due to natural variability acting on interannual ( Roemmich and Gilson 2011 ) and decadal ( England et al. 2014 ) time scales, remains a first

Full access
Hiroyuki Tsujino and Tamaki Yasuda

between the meridional velocity anomaly and the temperature anomaly cannot be neglected. The same can be said for the meridional overturn with potential density ( σ θ ) as a vertical axis (not shown). Meridional overturning circulation ( Fig. 12b ) is dominated by a circulation cell with subduction in the subtropics and upwelling in the Tropics. It seems that the meridional overturning circulation in the upper layer of the tropical–subtropical North Pacific is dominated by the “subtropical cell” (STC

Full access
Olga T. Sato and Paulo S. Polito

circles of the Atlantic Ocean and almost all of the total heat in the Tropics of the Pacific Ocean is dominated by the Ekman heat flux. Sato and Rossby (2000) , using historical hydrographic sections spanning almost 60 years, investigated the seasonal and low-frequency variability of the meridional heat flux at 36°N in the Atlantic. They found that the phase of the annual cycle of the total heat flux at the latitude is dominated by the Ekman heat flux. As pointed out by Montgomery (1974) , the

Full access
Qian Song, Arnold L. Gordon, and Martin Visbeck

, 2000, 3000, and 4000 m. Horizontal grid stretching is used in regions of interest, that is, latitudinal stretching in the tropical region (5°N– 15°S) and the longitudinal stretching in the Somali Current region, the Mozambique Channel, and the Leeuwin Current region ( Fig. 1b ). The zonal resolution is 0.5° in the Tropics and decreasing gradually to 1.7° in extratropics. The meridional resolution is about 0.8° in the Somali Current region, the Mozambique Channel, and in the Leeuwin Current region

Full access
Carsten Eden, Richard J. Greatbatch, and Jürgen Willebrand

10% of the mean flow in midlatitudes and on the same order of magnitude in the Tropics. The ν -related part of the eddy flux shows up when the lateral eddy fluxes cannot be described by isotropic diffusion only, pointing toward the need of anisotropic lateral mixing. Such an anisotropy has, indeed, been found in observations [see, for example, Stammer and Böning (1996) for a review], and thus it appears obvious, in retrospect, that the parameter ν becomes important in the present diagnosis

Full access
Lionel Renault, M. Jeroen Molemaker, Jonathan Gula, Sebastien Masson, and James C. McWilliams

1. Introduction The Gulf Stream (GS) is known to have a strong influence on the climate and the transport of heat from the tropics to middle and high latitudes. Understanding and modeling its mean path and variability is of uttermost importance for climate modeling. Upstream of Cape Hatteras the mean path is constrained by the topography ( Gula et al. 2015 ) and is generally well understood and resolved by numerical models. However, at separation—at Cape Hatteras and downstream—most models are

Full access
M. S. McCartney

hydrographic section near 37-W in the Atlantic Oceanshow the deep western boundary current (DWBC) in the North Atlantic Deep Water (NADW) establishedagainst the western boundary of the Brazil Basin immediately south of the equator (between 2 o and 5 -S). TheDWBC thus has directly crossed the equator to the South Atlantic following the east-southeast trend of thecontinental slope isobaths. The estimated DWBC transport of NADW is 35 x 106 m3 s-~, similar to otherestimates from the tropics discussed here

Full access