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Thursday, July 30, 2020 | History

3 edition of The 14 month wind stressed residual circulation (pole tide) in the North Sea found in the catalog.

The 14 month wind stressed residual circulation (pole tide) in the North Sea

The 14 month wind stressed residual circulation (pole tide) in the North Sea

Subjects:
• Tides -- North Sea

• Edition Notes

The Physical Object ID Numbers Other titles Fourteen month wind stressed residual circulation (pole tide) in the North Sea. Statement William P. O"Connor. Series NASA technical memorandum -- 87800. Contributions United States. National Aeronautics and Space Administration. Scientific and Technical Information Branch. Format Microform Pagination 1 v. Open Library OL15282797M

Analysis of available buoy and coastal wind observations suggests that the shear stress due to wind over LIS is under-predicted by a factor of between 2 and 3 if shore station winds are used to.   [7] The wind stress distribution over the SWAS is characterized by relatively high mean values (∼ Pa) over the Patagonian Shelf and relatively low mean values (∼ Pa) farther north. Their magnitude and direction are modulated by the seasonal oscillations of the South Atlantic high-pressure system [Höflich, ].

The addition of wind drag affected the surface circulation, forcing W-bound (N-bound) currents in the spring-summer (fall-winter) months and generating a positive sea-level slope toward the continent. Standard deviation and linear trend of observed monthly eastward wind stress averaged over the Pacific Ocean from $$10^{\circ }\hbox {S}$$ to $$10^{\circ }\hbox {N}$$ and over the time period from January to December All wind stress trends are statistically significant except for values east of about $$^{\circ }\hbox {E}$$.The numerical values on the left (right) in parentheses.

In this study, a high-resolution circulation model based on POM was used to compare the influences of the tidal residual currents and wind-driven currents on Lagrangian trajectories during summer time in the southwestern Yellow Sea. The four kinds of tides (M 2, S 2, K 1, and O 1) and climatological wind stress forced the model from May to June. In physical oceanography and fluid dynamics, the wind stress is the shear stress exerted by the wind on the surface of large bodies of water – such as oceans, seas, estuaries and is the force component parallel to the surface, per unit area, as applied by the wind on the water wind stress is affected by the wind speed, the shape of the wind waves and the atmospheric.

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The 14 month wind stressed residual circulation (pole tide) in the North Sea Download PDF EPUB FB2

The 14 month wind stressed residual circulation (pole tide) in the North Sea From published research it is known that a quasi-periodic 14 month atmospheric pressure oscillation of a few tenths of a millibar exists in the region of the North and Baltic Seas.

At some time in the cycle the associated wind stress has a westerly component that drives a circulation in the North by: 9. Get this from a library. The 14 month wind stressed residual circulation (pole tide) in the North Sea.

[William P O'Connor; United States. National Aeronautics and Space Administration. Scientific and Technical Information Branch.]. The 14 month wind stressed residual circulation (pole tide) in the North Sea Oconnor, W. Abstract. From published research it is known that a quasi-periodic 14 month atmospheric pressure oscillation of a few tenths of a millibar exists in the region of the North and Baltic Seas.

At some time in the cycle the associated wind stress has a Cited by: 9. Wind stress curl can be large for water bodies surrounded by a complex terrain [Rueda et al., ]. If wind stress curl is one of the major driving forces, Ekman pumping is important for the excitation of horizontal circulation as well as residual by:   The first one is a portion of the wind-driven Subtropical cell between 30°S–40°S and 31 kg m −3 – kg m −3, with a maximum meridional flux of 18 Sv.

A second surface cell lies above the residual circulation, between 50°S and 60°S, having a maximum intensity of 10 by:   In the following "residual circulation" will refer to the climatic residual circulation (T 2 lo6 s) or the tidal and wind residual circulations (T 2 lo5 s) with the restrictions made above.

The equations for the residual flow may be obtained by taking the average of. wind stress on the eddy circulation in the northern Gulf of California was investigated by Monreal-Go´mez et al. [], Carbajal [], and Marinone [] using numerical models.

[5] Residual tidal currents are another outstanding feature of the tidal circulation in the Gulf of California. Argote et al.

With the westerly wind stress quadrupled (Fig. 4, bottom-right panel), the overturning circulation above m is reduced again, except at the latitudes of the wind stress maximum.

However, below m, the circulation is stronger for the quadrupled wind stress, and the circulation is strongly intensified near the northern boundary. In keeping with the analysis of KJM, we will discuss the budgets of the ACC in terms of ng from Levitus and Boyer () annual mean data for the potential temperature and salinity we calculate the potential density σ using the nonlinear equation of state (); the buoyancy is defined by b = −gσ/ρ 0, where ρ 0 = kg m −3 is the average density of seawater.

The second term is the wind stress contribution to the residual currents. An example of axial or longitudinal inputs for an up-estuary wind stress of T = 40 (corresponds to dyn cm −2 or equivalent to a wind speed of ∼6 m s −1) is shown in Figure 4, with corresponding salinity response in Figure 5.

Moderate wind stress modifies both. The wind stress climatology is taken from Hellerman and Rosenstein (). Their calculations were based upon surface observations obtained during the period through and a speed-dependent drag coefficient formulation (Bunker, ).

Fig. 8 displays their data for our model domain at the horizontal resolution of the data set (2. 1. Introduction.

The meridional residual circulation (MRC) is the result of the inter-hemisphere thermal gradient caused by a middle atmosphere out of radiative balance due to mechanical wave forcing (Houghton,Solomon et al., ).Postulated by Brewer (), the MRC explains the high concentration of ozone and water vapor at high latitudes even the production is larger at low.

In the 3‐D scheme of residual circulation forced by remote wind, which we have observed and described, the alongshore jet associated with upwelling or downwelling events and its interaction with the topographic features of the Ría de Vigo (two mouths generated by the presence of the Cies Islands and the funnel shape of the ria) have a key role.

In this coastal application a realistic barotropic–baroclinic simulation of the circulation and surge elevation is set-up, demonstrating greater accuracy occurs when using the Charnock relation, with a constant Charnock coefficient offor surface wind stress during this one month period.

Introduction [2] Since the pioneering numerical modeling studies of Rao and Murty and Murty and Rao on the steady state, wind‐induced circulation in the Great Lakes, there continues to be uncertainty about the relative effects of wind stress curl, topography, and stratification on large‐scale circulation in the Great Lakes and other water bodies.

The eddy-induced circulation exactly opposes the Eulerian circulation, and the residual circulation is zero (see Karsten et al. for a numerical illustration).

Marshall and Radko () present analytical models of the ACC in which there is a three-way balance between Coriolis torque (on the residual flow), eddy stresses, and wind stress. Nonidealized eddy-permitting OGCM studies suggest a doubling in wind stress should lead to a less than 50% increase in SO residual overturning (i.e., substantial eddy compensation): Spence et al.

() find that a 25% increase in SO wind stress leads to a similar increase in eddy heat fluxes, and Farneti et al. () find an only 15% increase. The wind stress is spatially uniform and is given by t W ¼ t p sin½wðÞt 25 25 ≤ t ≤ 0 other times; ð1Þ where t w is the along-channel wind stress, t the time (days), w ¼ 2p 5 day the frequency of the wind-forcing, and t p the peak wind stress.

Positive t W corresponds to up-estuary C LI AND LI: WIND-DRIVEN LATERAL. Similarly, the rate of the overturning circulation scales with wind stress as τ w −1 in the ɛ ≪ 1 limit and becomes independent of the wind stress in the ɛ ≫ 1 limit, although we are not able to completely explore the extreme parameter regimes with the numerical ocean model.

The circulation of the Gulf of Khambhat (GoK) is studied from a Lagrangian point of view using a 2D numerical model. The model-predicted tide elevation and current speed are in agreement with the observations. Seasonal variations of advection of particles are simulated by releasing particles homogeneously distributed over the Gulf.

After one month of simulation, no particles escaped from. Other authors have explored the influence of river discharge and wind stress in the establishment of residual flows (Garvine et al., ;Jay and Flinchem, ;Lopes and Dias, ).Recent observations of satellite-tracked drogued buoys in the Gulf of Carpentaria indicate a slow, clockwise mean circulation, which appears to be a permanent feature in the Gulf.

Residual currents, derived from months of recent current-meter observations, and from a numerical tidal model of the Gulf, are compared with the motions deduced from the buoys. North-west monsoon winds and.The work performed by sea surface wind to the global oceanic general circulation is calculated as: ∬τ w ∙ v s dxdy, where τ w is monthly wind stress and v s is surface current velocity.

Here, we calculated the wind work applying wind stress from the ECMWF and WASWind and 5 .