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  • American Geophysical Union (AGU)  (13)
  • 1
    Online-Ressource
    Online-Ressource
    A model study of wind‐ and buoyancy‐driven coastal circulation
    American Geophysical Union (AGU) ; 1988
    In:  Journal of Geophysical Research: Oceans Vol. 93, No. C5 ( 1988-05-15), p. 5078-5092
    Details
    In: Journal of Geophysical Research: Oceans, American Geophysical Union (AGU), Vol. 93, No. C5 ( 1988-05-15), p. 5078-5092
    Kurzfassung: A two‐level model with a flat bottom on a β‐plane is employed to examine wind‐ and buoyancy‐driven coastal circulation on the western boundary of the ocean. The model of the ocean interior receives wind stress through the surface Ekman layer, which is purely determined from wind stress. Buoyancy flux is given to the upper level. Momentum equations are linear, and geostrophy in cross‐shore momentum is assumed. Density equations retain horizontal and vertical advection terms as well as horizontal diffusion. This cost‐effective three‐dimensional model is capable of a case study of a seasonal time‐scale simulation with various parameters varied. Oceanic responses to wind stress and buoyancy flux occur only along the coast to right of the forcing area facing offshore. A barotropic component merging to the western boundary is responsible for elimination of the undercurrent in the wind‐driven flow in most cases. The widths of the barotropic and baroclinic components are proportional to (horizontal viscosity) 1/3 and (horizontal diffusion) 1/2 , respectively. Thus the undercurrent exists with a small diffusion coefficient. A wind‐driven current in a stratified system is insensitive to bottom friction, while a homogeneous system is sensitive to the friction. A buoyancy flux produces a baroclinic eddylike feature in the forcing area plus a baroclinic coastal flow. A significant barotropic component is produced by bottom friction in the buoyancy‐driven case, increasing (reducing) the upper (lower) level flow. Model sensitivity to assumed interactions between the Ekman layer and upper level and vertical finite‐difference scheme is examined. The flow field is insensitive to the assumptions and scheme, while vertical stratification is sensitive.
    Materialart: Online-Ressource
    ISSN: 0148-0227
    URL: Article
    DOI: 10.1029/JC093iC05p05078
    Sprache: Englisch
    Verlag: American Geophysical Union (AGU)
    Publikationsdatum: 1988
    ZDB Id: 2033040-6
    ZDB Id: 3094104-0
    ZDB Id: 2130824-X
    ZDB Id: 2016813-5
    ZDB Id: 2016810-X
    ZDB Id: 2403298-0
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    ZDB Id: 161666-3
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    ZDB Id: 2969341-X
    ZDB Id: 161665-1
    ZDB Id: 3094268-8
    ZDB Id: 710256-2
    ZDB Id: 2016804-4
    ZDB Id: 3094181-7
    ZDB Id: 3094219-6
    ZDB Id: 3094167-2
    ZDB Id: 2220777-6
    ZDB Id: 3094197-0
    SSG: 16,13
    Standort Signatur Einschränkungen Verfügbarkeit
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  • 2
    Online-Ressource
    Online-Ressource
    A mixed layer beneath melting sea ice in the marginal ice zone using a one‐dimensional turbulent closure model
    American Geophysical Union (AGU) ; 1986
    In:  Journal of Geophysical Research: Oceans Vol. 91, No. C4 ( 1986-04-15), p. 5054-5060
    Details
    In: Journal of Geophysical Research: Oceans, American Geophysical Union (AGU), Vol. 91, No. C4 ( 1986-04-15), p. 5054-5060
    Kurzfassung: A level 2 second‐order turbulent closure model is employed to study the surface mixed layer developing between sea ice and a relatively warmer background water in the marginal ice zone. The model is driven by a suddenly imposed ice‐water stress and warming in the water. The mixed layer rapidly develops in 1 day and afterwards is gradually eroded at its bottom mainly by an inertial oscillation. The ice velocity is larger with the stronger stress, but the mixed layer is thicker. Hence the length scale of ice travel before complete melting is nearly independent of the ice‐water stress. Higher temperature of the background water gives more heat to ice but produces a thinner mixed layer. The product of the travel distance and (the background temperature minus the freezing point) is larger for the warmer water. Heat flux through the ice due to atmospheric forcing is a minor mechanism for melting in the marginal ice zone.
    Materialart: Online-Ressource
    ISSN: 0148-0227
    URL: Article
    DOI: 10.1029/JC091iC04p05054
    Sprache: Englisch
    Verlag: American Geophysical Union (AGU)
    Publikationsdatum: 1986
    ZDB Id: 2033040-6
    ZDB Id: 3094104-0
    ZDB Id: 2130824-X
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    ZDB Id: 2403298-0
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    ZDB Id: 161666-3
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    ZDB Id: 2969341-X
    ZDB Id: 161665-1
    ZDB Id: 3094268-8
    ZDB Id: 710256-2
    ZDB Id: 2016804-4
    ZDB Id: 3094181-7
    ZDB Id: 3094219-6
    ZDB Id: 3094167-2
    ZDB Id: 2220777-6
    ZDB Id: 3094197-0
    SSG: 16,13
    Standort Signatur Einschränkungen Verfügbarkeit
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  • 3
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    Online-Ressource
    Changes of total CO 2 and p CO 2 in the surface ocean during the mixed layer development in the northern North Pacific
    American Geophysical Union (AGU) ; 2000
    In:  Journal of Geophysical Research: Oceans Vol. 105, No. C2 ( 2000-02-15), p. 3465-3481
    Details
    In: Journal of Geophysical Research: Oceans, American Geophysical Union (AGU), Vol. 105, No. C2 ( 2000-02-15), p. 3465-3481
    Kurzfassung: A main objective is to simulate the seasonal variations in a carbon cycle during the mixed layer development from a fall through winer over the northern North Pacific. A bulk mixed layer model is employed, which is initialized with the historical data and forced by the observed atmospheric data. The model retains the following mechanisms: cooling and freshwater flux through the sea surface, kinetic energy input due to wind stresses, and air‐sea CO 2 flux as well as turbulent vertical mixing of heat, salt, total CO 2 , and carbonate alkalinity at the bottom of the mixed layer. Total CO 2 , carbonate alkalinity, and p CO 2 are related to each other under the assumption of chemical equilibrium. Since biological processes are secondary for the p CO 2 evolution during winter, they are omitted. The evolution of p CO 2 in the model mixed layer shows a rapid increase of p CO 2 in the subpolar region due to mixing of deep water rich in CO 2 before exceeding the atmospheric p CO 2 , and then the CO 2 flux stays almost constant during the winter. In the subtropical region the CO 2 is transported always from the atmosphere to the ocean, as the p CO 2 decreases from cooling. The ocean is a CO 2 sink (−0.18 GtC half‐year −1 ) over the entire model domain north of 30°N. However, in the subpolar region the ocean is a CO 2 source (0.04 GtC half‐year −1 ). The CO 2 flux varies from year to year, while there is no qualitative difference in the flux distribution.
    Materialart: Online-Ressource
    ISSN: 0148-0227
    URL: Article
    DOI: 10.1029/1999JC900302
    Sprache: Englisch
    Verlag: American Geophysical Union (AGU)
    Publikationsdatum: 2000
    ZDB Id: 2033040-6
    ZDB Id: 3094104-0
    ZDB Id: 2130824-X
    ZDB Id: 2016813-5
    ZDB Id: 2016810-X
    ZDB Id: 2403298-0
    ZDB Id: 2016800-7
    ZDB Id: 161666-3
    ZDB Id: 161667-5
    ZDB Id: 2969341-X
    ZDB Id: 161665-1
    ZDB Id: 3094268-8
    ZDB Id: 710256-2
    ZDB Id: 2016804-4
    ZDB Id: 3094181-7
    ZDB Id: 3094219-6
    ZDB Id: 3094167-2
    ZDB Id: 2220777-6
    ZDB Id: 3094197-0
    SSG: 16,13
    Standort Signatur Einschränkungen Verfügbarkeit
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  • 4
    Online-Ressource
    Online-Ressource
    Comparison of mesoscale meanders and eddies simulated by quasi‐geostrophic and primitive equation models: A case study
    American Geophysical Union (AGU) ; 1994
    In:  Journal of Geophysical Research: Oceans Vol. 99, No. C11 ( 1994-11-15), p. 22645-22663
    Details
    In: Journal of Geophysical Research: Oceans, American Geophysical Union (AGU), Vol. 99, No. C11 ( 1994-11-15), p. 22645-22663
    Kurzfassung: A comparison is made between meanders and eddies simulated by a two‐layer, quasi‐geostrophic numerical model and those simulated by a Bryan‐Cox type primitive equation model at various values of the Rossby number. The model geometry and parameter settings are based on a previous study of the Norwegian Coastal Current by Ikeda et al. (1989). The aim is to identify the dynamical effects of increasing the Rossby number and to assess the performance of the quasi‐gestrophic (QG) model when applied to meandering currents which are outside its formal range of validity. The growth rates of meanders in the primitive equation (PE) model are particularly sensitive to the vertical resolution used; this sensitivity is strongest at short wavelengths, and suggests that very fine vertical resolution may be needed in the Bryan‐Cox model for accurate simulation of meander growth. The QG model simulates the phase speed of meanders in the PE model well but overestimates the growth rate at moderate Rossby number (by about 25% when the Rossby number is 0.69). As the Rossby number is increased, the asymmetry of the primitive equation vorticity equation comes increasingly into play, and at finite meander amplitude this results in small, intense cyclones and large, weak anticyclones. This effect, which is absent in the quasi‐geostrophic model, can lead to significant changes in the potential vorticity field (and hence, by implication, in the concentration fields of other tracers). The principal trends in the solutions as the Rossby number is increased are as follows: (1) the disturbance becomes less energetic (in a dimensionless sense) at all stages of its life cycle; (2) the effects of the disturbance become increasingly trapped near the position of the original frontal jet; and (3) cross‐frontal transport, particularly offshore transport of coastal water, is inhibited as coastal water is wrapped around the intense cyclones. Our results provide guidance in interpreting the results of Ikeda et al. and those of other eddy models.
    Materialart: Online-Ressource
    ISSN: 0148-0227
    URL: Article
    DOI: 10.1029/94JC01834
    Sprache: Englisch
    Verlag: American Geophysical Union (AGU)
    Publikationsdatum: 1994
    ZDB Id: 2033040-6
    ZDB Id: 3094104-0
    ZDB Id: 2130824-X
    ZDB Id: 2016813-5
    ZDB Id: 2016810-X
    ZDB Id: 2403298-0
    ZDB Id: 2016800-7
    ZDB Id: 161666-3
    ZDB Id: 161667-5
    ZDB Id: 2969341-X
    ZDB Id: 161665-1
    ZDB Id: 3094268-8
    ZDB Id: 710256-2
    ZDB Id: 2016804-4
    ZDB Id: 3094181-7
    ZDB Id: 3094219-6
    ZDB Id: 3094167-2
    ZDB Id: 2220777-6
    ZDB Id: 3094197-0
    SSG: 16,13
    Standort Signatur Einschränkungen Verfügbarkeit
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  • 5
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    Online-Ressource
    A simple model of subsurface mesoscale eddies
    American Geophysical Union (AGU) ; 1982
    In:  Journal of Geophysical Research: Oceans Vol. 87, No. C10 ( 1982-09-20), p. 7925-7931
    Details
    In: Journal of Geophysical Research: Oceans, American Geophysical Union (AGU), Vol. 87, No. C10 ( 1982-09-20), p. 7925-7931
    Kurzfassung: Motion in and around small mesoscale eddies is studied. The model is composed of an upper layer, a motionless and infinitely deep lower layer, and the water mass that intrudes between the two layers. This water mass is deformed from a cylinder to a lenslike shape during intrusion. Assuming that potential vorticity (with a relative vorticity of zero before the intrusion) is conserved during the process of intrusion, rotation in and above the radially symmetric intruding mass is determined for a steady state established after intrusion. The rotation is anticyclonic in and above the intruding mass and is fastest at the rim of the mass. In the asymptotic case of the small intruding mass, the azimuthal velocity in the mass exceeds the velocity in the water above the mass. The velocity above the mass tends to be comparable to the velocity in the mass as the mass radius approaches the deformation radius.
    Materialart: Online-Ressource
    ISSN: 0148-0227
    URL: Article
    DOI: 10.1029/JC087iC10p07925
    Sprache: Englisch
    Verlag: American Geophysical Union (AGU)
    Publikationsdatum: 1982
    ZDB Id: 2033040-6
    ZDB Id: 3094104-0
    ZDB Id: 2130824-X
    ZDB Id: 2016813-5
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    ZDB Id: 2403298-0
    ZDB Id: 2016800-7
    ZDB Id: 161666-3
    ZDB Id: 161667-5
    ZDB Id: 2969341-X
    ZDB Id: 161665-1
    ZDB Id: 3094268-8
    ZDB Id: 710256-2
    ZDB Id: 2016804-4
    ZDB Id: 3094181-7
    ZDB Id: 3094219-6
    ZDB Id: 3094167-2
    ZDB Id: 2220777-6
    ZDB Id: 3094197-0
    SSG: 16,13
    Standort Signatur Einschränkungen Verfügbarkeit
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    Online-Ressource
  • 6
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    Coastal flows driven by a local density flux
    American Geophysical Union (AGU) ; 1984
    In:  Journal of Geophysical Research: Oceans Vol. 89, No. C5 ( 1984-09-20), p. 8008-8016
    Details
    In: Journal of Geophysical Research: Oceans, American Geophysical Union (AGU), Vol. 89, No. C5 ( 1984-09-20), p. 8008-8016
    Kurzfassung: A two‐layer model with a rigid lid and a flat bottom on an f plane is employed to study a flow field driven by a density flux through the sea surface or the coast; for example, freshwater discharged from a river. The negative (positive) density flux into the upper layer is represented by the water beneath (over) the interface changing from the lower (upper) layer to the upper (lower) layer, that is, entrainment of the lower (upper) layer by the upper (lower) layer. The subinertial flow pattern constrained by the coast has two components: one is a baroclinic eddy nearby that matches the entrainment region, and the other is a forced, internal Kelvin wave along the appropriate half of the coast.
    Materialart: Online-Ressource
    ISSN: 0148-0227
    URL: Article
    DOI: 10.1029/JC089iC05p08008
    Sprache: Englisch
    Verlag: American Geophysical Union (AGU)
    Publikationsdatum: 1984
    ZDB Id: 2033040-6
    ZDB Id: 3094104-0
    ZDB Id: 2130824-X
    ZDB Id: 2016813-5
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    ZDB Id: 2403298-0
    ZDB Id: 2016800-7
    ZDB Id: 161666-3
    ZDB Id: 161667-5
    ZDB Id: 2969341-X
    ZDB Id: 161665-1
    ZDB Id: 3094268-8
    ZDB Id: 710256-2
    ZDB Id: 2016804-4
    ZDB Id: 3094181-7
    ZDB Id: 3094219-6
    ZDB Id: 3094167-2
    ZDB Id: 2220777-6
    ZDB Id: 3094197-0
    SSG: 16,13
    Standort Signatur Einschränkungen Verfügbarkeit
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  • 7
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    A coupled ice‐ocean mixed layer model of the marginal ice zone responding to wind forcing
    American Geophysical Union (AGU) ; 1989
    In:  Journal of Geophysical Research: Oceans Vol. 94, No. C7 ( 1989-07-15), p. 9699-9709
    Details
    In: Journal of Geophysical Research: Oceans, American Geophysical Union (AGU), Vol. 94, No. C7 ( 1989-07-15), p. 9699-9709
    Kurzfassung: A free‐drifting thermodynamic sea ice model is coupled with a continuously stratified ocean model, whose vertical mixing coefficients are determined by a turbulent closure scheme. The system has variability in the cross‐ice‐edge direction, while two‐dimensionality (along‐ice‐edge homogeneity) is assumed. The model is initially motionless and has no horizontal variability in ocean interior, whereas ice covers only a half portion. A uniform wind stress is imposed suddenly to drive the coupled system. The surface mixed layer is developed as time increases; i.e., a top few tens of meters are well mixed in a day. With an initial water temperature above a freezing point, the fresh mixed layer forms in the ice‐covered portion. A wind‐driven ice velocity is oriented to the right from the wind direction. A wind with the ice to the right (left) looking downstream produces upwelling (downwelling) under the ice edge caused by a difference in Ekman transport. An off‐ice (on‐ice) wind advects the ice toward the open water (ice‐covered) area, and makes the ice edge sharper (gentler) owing partially to faster movement in the region with higher ice concentration. In the off‐ice wind case, the mixed layer near the ice edge is shallower under development, so that a melt rate is smaller than that estimated by a prescribed‐depth mixed layer. An inertio‐internal gravity wave is generated by a transient variability in surface stress associated with a moving ice edge, most significantly in the case of the off‐ice wind, and enhances sharpness of the ice edge.
    Materialart: Online-Ressource
    ISSN: 0148-0227
    URL: Article
    DOI: 10.1029/JC094iC07p09699
    Sprache: Englisch
    Verlag: American Geophysical Union (AGU)
    Publikationsdatum: 1989
    ZDB Id: 2033040-6
    ZDB Id: 3094104-0
    ZDB Id: 2130824-X
    ZDB Id: 2016813-5
    ZDB Id: 2016810-X
    ZDB Id: 2403298-0
    ZDB Id: 2016800-7
    ZDB Id: 161666-3
    ZDB Id: 161667-5
    ZDB Id: 2969341-X
    ZDB Id: 161665-1
    ZDB Id: 3094268-8
    ZDB Id: 710256-2
    ZDB Id: 2016804-4
    ZDB Id: 3094181-7
    ZDB Id: 3094219-6
    ZDB Id: 3094167-2
    ZDB Id: 2220777-6
    ZDB Id: 3094197-0
    SSG: 16,13
    Standort Signatur Einschränkungen Verfügbarkeit
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  • 8
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    A coupled ice‐ocean model of a wind‐driven coastal flow
    American Geophysical Union (AGU) ; 1985
    In:  Journal of Geophysical Research: Oceans Vol. 90, No. C5 ( 1985-09-20), p. 9119-9128
    Details
    In: Journal of Geophysical Research: Oceans, American Geophysical Union (AGU), Vol. 90, No. C5 ( 1985-09-20), p. 9119-9128
    Kurzfassung: Ice movement driven by winds along the coast is studied using a two‐dimensional (vertical seaward), ice‐ocean coupled model. Right‐hand alongshore winds are given when internal ice stresses are important to determine the ice movement. These winds induce right‐hand coastal currents and ice movement. A shoreward Ekman flow beneath the ice is a major mechanism to constrain the ice over the shelf, balancing the internal ice pressure gradient. When the wind ceases, the ice decreases its alongshore velocity, and the ice‐covered band becomes wider. The alongshore ice velocity is sensitive to ice shear strength, which determines the shear stress at the coast; i.e., weak (strong) shear strength allows a large (small) ice velocity at the coast, resulting in intense (weak) Ekman flow and downwelling, which induces a fast (slow) coastal current. The alongshore velocity is also sensitive to the relatively small cross‐shore component of the wind; i.e., the seaward (shoreward) component reduces (induces) the shear stress and allows large (small) ice velocity. The results are applied to the ice over the Labrador shelf.
    Materialart: Online-Ressource
    ISSN: 0148-0227
    URL: Article
    DOI: 10.1029/JC090iC05p09119
    Sprache: Englisch
    Verlag: American Geophysical Union (AGU)
    Publikationsdatum: 1985
    ZDB Id: 2033040-6
    ZDB Id: 3094104-0
    ZDB Id: 2130824-X
    ZDB Id: 2016813-5
    ZDB Id: 2016810-X
    ZDB Id: 2403298-0
    ZDB Id: 2016800-7
    ZDB Id: 161666-3
    ZDB Id: 161667-5
    ZDB Id: 2969341-X
    ZDB Id: 161665-1
    ZDB Id: 3094268-8
    ZDB Id: 710256-2
    ZDB Id: 2016804-4
    ZDB Id: 3094181-7
    ZDB Id: 3094219-6
    ZDB Id: 3094167-2
    ZDB Id: 2220777-6
    ZDB Id: 3094197-0
    SSG: 16,13
    Standort Signatur Einschränkungen Verfügbarkeit
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  • 9
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    A three‐dimensional coupled ice‐ocean model of coastal circulation
    American Geophysical Union (AGU) ; 1988
    In:  Journal of Geophysical Research: Oceans Vol. 93, No. C9 ( 1988-09-15), p. 10731-10748
    Details
    In: Journal of Geophysical Research: Oceans, American Geophysical Union (AGU), Vol. 93, No. C9 ( 1988-09-15), p. 10731-10748
    Kurzfassung: A coupled ice‐ocean model is employed to examine roles of ocean circulation on sea ice formation and distribution along the east coasts of North America and Greenland. The model has a flat bottom and a rectangular domain with a coastal boundary to the west, an artificial solid boundary to the north, and open eastern and southern boundaries. The model is driven by idealized alongshore wind stress and atmospheric cooling; the wind stress decays northward and southward with a maximum amplitude at the middle. The open water heat flux is locally specified with both seaward and southward decay, and the heat flux through ice is taken to be inversely proportional to the ice thickness. Ice internal stresses are simplified under the assumption that the major strain is cross‐shore shear deformation. The ocean model has three levels: the surface mixed layer and two levels in the lower ocean. Linear momentum equations are used, and a geostrophic cross‐shore momentum balance is assumed. Vertical viscosity is represented only by the surface and bottom Ekman flow. Equations for temperature and salinity retain advection and diffusion terms in both vertical and horizontal directions. The model reveals the following important roles of the ocean: northerly wind induces shoreward Ekman flow and southward barotropic flow, which develops only to the southern (downstream in the sense of long coastal‐trapped wave propagation) side of wind forcing region and merges westward owing to the β‐effect. Coastal downwelling produces additional baroclinic alongshore flow, intensifying (weakening) the southward flow in the upper (lower) ocean. Cyclonic circulation is generated by differences in Ekman flow between the ice‐covered onshore area and open‐water offshore area. Ice, which occupies the coastal area, is narrowed dynamically by the shoreward Ekman flow and thermodynamically by the warm offshore water in the Ekman flow. Ice is also advected southward by the alongshore current, associated with the coastal flow and the cyclonic circulation, as well as direct wind stress. When a lower ocean is warmer than the freezing point, convective overturning carries heat upward and reduces ice formation. Ice grows faster over downwelled and southward advected cold anomalies in the lower ocean.
    Materialart: Online-Ressource
    ISSN: 0148-0227
    URL: Article
    DOI: 10.1029/JC093iC09p10731
    Sprache: Englisch
    Verlag: American Geophysical Union (AGU)
    Publikationsdatum: 1988
    ZDB Id: 2033040-6
    ZDB Id: 3094104-0
    ZDB Id: 2130824-X
    ZDB Id: 2016813-5
    ZDB Id: 2016810-X
    ZDB Id: 2403298-0
    ZDB Id: 2016800-7
    ZDB Id: 161666-3
    ZDB Id: 161667-5
    ZDB Id: 2969341-X
    ZDB Id: 161665-1
    ZDB Id: 3094268-8
    ZDB Id: 710256-2
    ZDB Id: 2016804-4
    ZDB Id: 3094181-7
    ZDB Id: 3094219-6
    ZDB Id: 3094167-2
    ZDB Id: 2220777-6
    ZDB Id: 3094197-0
    SSG: 16,13
    Standort Signatur Einschränkungen Verfügbarkeit
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  • 10
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    A numerical investigation of the transport process of dense shelf water from a continental shelf to a slope
    American Geophysical Union (AGU) ; 1999
    In:  Journal of Geophysical Research: Oceans Vol. 104, No. C1 ( 1999-01-15), p. 1197-1210
    Details
    In: Journal of Geophysical Research: Oceans, American Geophysical Union (AGU), Vol. 104, No. C1 ( 1999-01-15), p. 1197-1210
    Kurzfassung: We investigate the offshore transport process of dense shelf water, using a three‐dimensional, primitive equation model. We focus on the effects of bottom topography, in particular, inclination of a bottom slope from a continental shelf to a deep basin. For the numerical domain we use an idealized bottom topography in which the bottom deepens gradually from a shallow continental shelf region to a steep slope region. In the continental shelf region we use a salt flux which represents the typical brine rejection in a coastal polynya. Results of the numerical experiments show that dense shelf water is transported offshore by eddy flux and a dense plume. The transport by eddy flux occurs mainly over a continental shelf, while that by the dense plume occurs over a continental slope. A boundary between the regions where the above two processes are dominant corresponds locally to a shelf break. A salinity front is developed in the boundary over the shelf break, separating the dense shelf water from the offshore water. We also investigate the stability of the surface westward current over the shelf break front, using a simple analytical model. The analytical model investigation shows that shelf break topography plays an important role in determining a neutral point of the stability of the shelf break current and preventing dense shelf water from being transported farther offshore by eddy flux. We suggest that eddy activity on a continental shelf contributes not only to the development of the shelf break front but also to the water exchange between a continental shelf and a slope region.
    Materialart: Online-Ressource
    ISSN: 0148-0227
    URL: Article
    DOI: 10.1029/98JC02585
    Sprache: Englisch
    Verlag: American Geophysical Union (AGU)
    Publikationsdatum: 1999
    ZDB Id: 2033040-6
    ZDB Id: 3094104-0
    ZDB Id: 2130824-X
    ZDB Id: 2016813-5
    ZDB Id: 2016810-X
    ZDB Id: 2403298-0
    ZDB Id: 2016800-7
    ZDB Id: 161666-3
    ZDB Id: 161667-5
    ZDB Id: 2969341-X
    ZDB Id: 161665-1
    ZDB Id: 3094268-8
    ZDB Id: 710256-2
    ZDB Id: 2016804-4
    ZDB Id: 3094181-7
    ZDB Id: 3094219-6
    ZDB Id: 3094167-2
    ZDB Id: 2220777-6
    ZDB Id: 3094197-0
    SSG: 16,13
    Standort Signatur Einschränkungen Verfügbarkeit
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