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1.
Characteristics of stationary Rossby-waves are investigated by use of equations expressing conservation of potential vorticity for a quasi-geostrophic two-layer flow of an incompressible inviscid fluid on a beta-plane. A two-dimensional problem is discussed; the basic flow is directing eastward without horizontal shear, and the stationary Rossby-waves are produced by a two-dimensional bump extending in the north-south direction which is located on a sloping bottom with a constant north-south gradient.When the slope is steep, stream-lines are scarcely displaced being influenced by the bump. When the bottom has no north-south inclination, however, there is a case where group velocity of Rossby-waves produced by the bump directs westward and the stream-lines meander sinusoidally at the west of the bump. This phenomenon is called upstream influence. These two special cases have a possibility to explain two different mean paths for the Kuroshio namely, the path along the continental slope and the path with a stationary meander at the west of the Izu-Ogasawara Ridge.  相似文献   

2.
Properties of coastal trapped waves when the pycnocline intersects a sloping bottom are studied using a two-layer model which has slopes in both layers. In this system there is an infinite discrete sequence of modes, and four different sorts of waves exist: the barotropic Kelvin wave, the upper shelf wave, the lower shelf wave and the internal Kelvin-type wave. They all propagate with the coast to their right in the Northern Hemisphere. The upper and lower shelf waves are due to the topographic-effect on the upper-layer and lower-layer slopes, respectively. Their motions are dominant in the respective layers being accompanied by significant interface elevations. The properties of the upper (lower) shelf wave are almost unaffected by the existence of a lower-layer (upper-layer) slope. The motion of the internal Kelvin-type wave is confined to the region around the line where the density interface intersects the bottom slope.The modes, except that with the fastest phase speed (the barotropic Kelvin wave), are assigned mode numbers in order of descending frequency. Characteristics of Mode 1 change with wavenumber; the upper shelf wave for small wavenumbers and the internal Kelvin-type wave for large wavenumbers (high frequencies). The higher modes of Mode 2 and above can be classified into the upper and lower shelf waves.  相似文献   

3.
Numerical solutions are examined for isolated, intense vortices as influenced by western bounding bottom topography through the use of a rigid-lid, two-layer primitive -plane numerical model. Systematic studies are made of the sense of rotation (cyclonic/anticyclonic), the consequence of varying the gradient of bottom slope, and the different vertical shear in a two layer ocean. In the basin with a bottom slope, the nearly barotropic anticyclonic vortex forms a modon-like vortex for S with fixedRo 2<O(1) (where is the ratio between the variation of the Coriolis parameter across the eddy to the Coriolis parameter in the center, S the topographic effect and,Ro 2 the Rossby number in the lower layer) and its generation is due to a compound effect of the planetary beta, topographic beta, avvection, and mirror image. The formation of the modon-like vortex and the propagation of the original vortex onto the bottom slope depends on the strength of slope gradient and the baroclinicity of the vortex. The nearly barotropic anticyclonic vortex evolves into the stronger upper ocean one with increasing S: the gradient of the bottom slope becomes steeper. Then the original vortex lives longer because the barotropic component of the energy is converted to the baroclinic one and it moves toward southeast in forming a modon-like vortex in the lower layer. The evolution of a vortex in the model results are compared to observational results of a Kuroshio warm core ring (KWCR) obtained from hydrographic data (June, 1985) and from NOAA satellite infrared images (April, 1985 to July, 1985). It is shown that a KWCR (June, 1985) is influenced by the western continental slope/shelf of the East Japan.  相似文献   

4.
Branching of the Tsushima Current in the Japan Sea   总被引：4，自引：0，他引：4  
Three branches of the Tsushima Current are reproduced in a numerical model, and their formation mechanisms are studied. Two types of a two-layer, inflow-outflow model with a bottom slope along the Japanese coast are used. One has a bottom slope only in the lower layer (Model A), and the other has bottom slopes in both layers (Model B). Model B represents the typical situation in the Japan Sea, i.e., the main pycnocline intersects the bottom slope. The onshore side of the line where the pycnocline intersects the bottom slope has only one layer in Model B. Seasonal variation of inflow in the upper layer of the western half in the entrance section (the Tsushima Strait) is incorporated into the model.Three branches are formed in Model B and not in Model A. The first branch is the bottom-controlled steady current due to the topographic-effect on the upper-layer slope which exists in the one-layer region along the Japanese coast. The second branch is a temporal current which is formed along the offshore edge of the coastal one-layer region in association with the variation of inflow. The third branch is the steady western boundary current due to the planetary-effect. These results compare favorably with observations in Part I of this study.The mechanism of formation of the second branch is examined in detail. This branch is caused by the propagation of the lowest two modes of the upper shelf wave caused by the topographic-effect on the upper-layer slope which are generated by the significant increase in inflow from June to August.  相似文献   

5.
The formation of the spun up region by the withdrawal of water from a watergate located in the eastern boundary in a homogeneous ocean on a beta-plane at low Rossby number is presented. The spun up region penetrates only westward from the Watergate because of the special character of the generated Rossby waves. The growth rate and the final longitudinal length of the spun up region in the dissipative system is much affected by the watergate scale in the north-south direction.The relation with the experiment ofLong (1952) and the geophysical application are presented.  相似文献   

6.
This paper reports the results of a numerical study on the hydrodynamic instability parameters of a long-shore wave current in a surf zone with convex and concave bottom profiles. The limits of the change of the relative length of a long-shore meander have been derived in the form of 2/66, and structural and dynamic peculiarities of perturbations in a surf zone with various bottom profiles have been demonstrated.Translated by Vladimir A. Puchkin.  相似文献   

7.
The north/south-trending Panama Fracture Zone forms the present eastern boundary of the Cocos Plate, with the interplate motion being right-lateral strike-slip. This fracture zone is composed of at least four linear troughs some hundreds of kilometers in length. Separate active or historic faults undoubtedly coincide with each trough. The greatest sediment fill is found in the easternmost trough. Surface and basement depths of the western trough are generally greater than those of the other three; the western trough contains the least sediment, and is most continually linear. Morphology and sediments suggest that the principal locus of strike-slip movement within the fracture zone probably migrated incrementally westward from one fault-trough to another. From north to south, the fracture zone apparently narrows from the continental intersection to approximately 5°30N, and again widens from about 5°N to at least 3°N. Residual E/W-trending magnetic anomalies are centered between two of the four troughs; sea floor spreading in a north-south direction is interpreted to have occurred between 5°30N and 7°N from 4.5 m.y. ago to 2 m.y. ago, with the symmetric center roughly coinciding with a rift valley at 6°10N, 82°30W.  相似文献   

8.
Freely propagating surface gravity waves are observed to slow down and to stop at a beach when the bottom has a relatively gentle upward slope toward the shore and the frequency range of the waves covers the most energetic wind waves (sea and swell). Essentially no wave reflection can be seen and the measured reflected energy is very small compared to that transmitted shoreward. One consequence of this is that the flux of the wave’s linear momentum decreases in the direction of wave propagation, which is equivalent to a time rate of change of the momentum. It takes a force to cause the time rate of change of the momentum. Therefore, the bottom exerts a force on the waves in order to decrease the momentum flux. By Newton’s third law (action equals reaction) the waves then impart an equal but opposite force to the bottom. In shallow (but finite) water depths the wave force per unit bottom area is calculated, for normal angle of incidence to the beach, to be directly proportional to the square of the wave amplitude and to the bottom slope and inversely proportional to the mean depth; it is independent of the wave frequency. Constants of proportionality are: 1/4, the fluid density and the acceleration of gravity. Swell attenuation near coasts and some characteristics of sand movement in the near-shore region are not inconsistent with the algebraic structure of the wave force formula. Since the force has a depth variation which is significantly faster than that of the dimensions of the particle orbits in the vertical direction, the bottom induces a torque on the fluid particles that decreases the angular momentum flux of the waves. By an extension of Newton’s third law, the waves also exert an equal but opposite torque on the bottom. And because the bottom force on the waves exists over a horizontal distance, it does work on the waves and decreases their energy flux. Thus, theoretically, the fluxes of energy, angular and linear momentum are not conserved for shoaling surface gravity waves. Mass flux, associated with the Stokes drift, is assumed to be conserved, and the wave frequency is constant for a steady medium.  相似文献   

9.
A sequential updating method for assimilating Geosat altimeter data into an eddyresolving, quasi-geostrophic model is examined using simulated data of mesoscale features taken from a control run solution. The upper-layer streamfunction in the model is updated by the altimeter data on satellite tracks (at 110 km intervals) at times of observations (with 17-day cycles). To evaluate data suitability, the correlation between the data and the assimilation solution just before update is compared with the correlation between the two data with a 1-cycle separation: i.e., predictability is compared with persistence. The assimilation method is tested on mesoscale features such as linear Rossby waves, unstable mesoscale meanders in a jet and dipole eddies over realistic deep ocean topography. The assimilation method is successful for reconstructing the mesoscale features that evolve gradually or extend over more than one track. Assimilation is degraded by quick evolution of smaller scale features; i.e the unstable meanders that have short wavelengths and are not well captured by the altimeter with the low cross-track resolution, and the mesoscale features, whose lower layer component receives effects of bottom topography in the data but is underestimated due to inefficient downward transfer of the surface data in the assimilation.  相似文献   

10.
A coastal ocean -coordinate model of Monterey Bay (MOB) with realistic bottom topography and coastlines is developed using the Princeton Ocean Model (POM) and grid generation technique (GGT) to study the horizontal pressure gradient errors associated with the MOB steep topography. The submarine canyon in MOB features some of the steepest topography encountered anywhere in the world oceans. The MOB grids are designed using the EAGEAL View and GENIE++ grid generation systems. A grid package developed by Ly and Luong (1993) is used in this study to couple grids to the model. The MOB model is tested with both orthogonal and curvilinear nearly-orthogonal (CNO) grids. The CNO grid has horizontal resolution which varies from 300 m to 2 km, while the resolution of the orthogonal grid is uniform with x = 1.25 km and y = 1.38 km. These grids cover a domain of 180 × 160 km with the same number of grid points of 131 × 131. Vertical resolutions of 25, 35 and 45 vertical sigma levels are tested. The error in the MOB are evaluated in terms of mean kinetic energy and velocity against various grids, vertical, horizontal resolution and distributions, and bottom topography smoothing. Simulations with various grids show that GGT can be used as another tool in reducing -coordinate errors in coastal ocean modeling besides increasing resolution and smoothing bottom topography. Topographical smoothing not only reduces topographic slope, but changes realistic topography. A CNO grid with a high grid density packed along steep slopes and Monterey Submarine Canyon reduces the errors by 40% compared to a rectangular grid with the same number of grid points. The CNO grid is more efficient than the rectangular grid, since it has most of its grids over water. The simulations show that the presented MOB -coordinate model can be used with a confidence regarding horizontal pressure gradient error.  相似文献   

11.
Time-series measurements of temperature, salinity, suspended matter and beam attenuation coefficient () were measured at four hour intervals for about two days in June/ July 1982 in the middle shelf region and the coastal region of the southeastern Bering Sea. Current meters were also moored at the same locations.Depth-time distributions of indicated that profiles of suspended matter resulted from a combined process of resuspension of underlying sediments and sinking of suspended particles. Average-values for all measurements for particles revealed that the upward transport of particles due to resuspension formed a boundary layer, with a thickness apparently related to scalar speed. The average-profiles of the particle volume concentration were assumed to result from a balance between the sinking and diffusive flux of particles under a steady state, and the upward fluxes were calculated. Within the boundary layer, values of the upward fluxes of particulate organic matter linearly decreased with the logarithm of distance from the bottom. Fluxes of organic carbon at the upper edge of the boundary layer were 0.375 gC·m–2·day–1 in the middle shelf region (18 m above the bottom, bottom depth=78m) and 0.484gC·m–2·day–1 in the coastal region (25 m above the bottom, bottom depth=33m), and fluxes of nitrogen in both regions were 0.067 gN·m–2·day–1. The flux of organic carbon obtained in the middle shelf region (18 m above the bottom) agreed approximately with the flux (0.416 gC·m–2·day–1) calculated by substituting primary production data into the empirical equation of Suess (1980).  相似文献   

12.
The reflection and breaking of internal waves on a sloping beach were studied in a small wavetank filled with water and petroleum. The dependence of the reflection coefficient of the internal waves on wave steepness and on beach slope is found to be very similar to that of surface waves. The reflection coefficient is small for the very gentle slope, increases rapidly as the slope increases, and becomes almost constant for the steep slope. The reflection coefficient decreases with increase of the wave steepness. Also, the transition slope at which the coefficient curve has the maximum gradient increases with increase of the wave steepness. Breaking pattern of the internal waves is classified into four types; breaking, semi-breaking, wrinkle-generating, and non-breaking. Their dependence on beach slope and wave steepness is examined. The regular sequence of the four breaking types from breaking to non-breaking is observed with decrease of wave steepness or with increase of beach slope.  相似文献   

13.
A geological and geophysical survey off Tottori, southern-west of Honshu, Japan, was carried out by the Hydrographic Department of Japan during May and June (26 days) of 1974.In the survey area, there is marginal plateau which lies under the slope of the continental shelf adjacent to the Sanin district. By the closely-spaced surveying the marginal plateau was divided into two different zones based on differences of genesis and structure, which are identified in this paper as marginal plateaus A (west side) and marginal plateau B (east side). The tectonic boundary between marginal plateaus A and B, previously believed to exist near Tottori City, was not confirmed. An erosional plane, beneath the horizontally bedded upper layer was found to be 75 m lower than the submerged surface of marginal plateau A. Marginal plateau B is hypothesized to have been generated by the sliding of the upper layer. This is suggested by the presence of prominent slumping directed toward the bottom of the Oki Trough. This result implies that the submergence of the Oki Trough area and formation of the marginal plateau are closely related.  相似文献   

14.
Geochemical properties of gas hydrate accumulation associated with an active gas vent on the continental slope offshore northeast Sakhalin Island in the Sea of Okhotsk have been investigated. The pore water chemistry data suggest that the gas hydrates (GHs) were formed in an environment of upward-migrating fluid combined with a mechanism of pore water segregation. The upward infiltration of water enriched mainly by Cl– and K+ species appears to occur on the background of earlier diagenesis processes within the gas vent sediments. The GHs were formed from water with chlorinity ranging from 530 to 570 mM. The 18O and D of GH water varied from –1.4 to –1.8 and from –13 to –18, respectively, representing a mix of seawater and infiltrating fluid water. A complex interaction of pore water, water of ascending fluid and segregated pore water during hydrate formation is also supported by water content measurements and observed gas hydrate structure. The direction of segregated water is opposite to upward fluid migration. Decreasing activity of the gas vent is inferred by comparing the present top of the recovered hydrate layer with previous observations.  相似文献   

15.
Resumé Cet article présente des données bathymétriques et magnétiques de la région axiale de la dorsale sud-ouest indienne au voisinage de la zone de fracture majeure Atlantis II. Elles proviennent pricipalement de la campagne MD34 (Marion-Dufresne, 1983).L'axe de la dorsale est défini par la vallée et l'anomalie magnétique qui lui est associée. Le rilief le long de l'axe varie localement très rapidement; A l'ouest de la zone de fracture Atlantis II, le plancher axial présente deux bombements séparés par une dépression importante (4600 m). Cette étude met en évidence la corrélation entre ces hauts bathymétriques, la forme de la vallée et la l'amplitude de l'anomalie magnétique axiale: lorsque la profondeur du plancher axial diminue, la vallée se creuse et son encaissement augmente. On observe ainsi sur les hauts bathymétriques une section d'axe très encaissée, associée à une anomalie magnétique d'amplitude plus importance.L'identification de l'anomalie 5 (10 Ma) sur chaque flanc de la dorsale sud-ouest indienne permet la reconstitution de cette isochrone qui montre clairement une évolution de la géométrie de l'axe: à l'époque de l'anomalie 5, l'axe était composé de segments perpendiculaires à la direction d'expansion, décalés par des failles transformantes, alors qu'il apparait actuellement continu et formé sur les hauts topographiques de courts segments perpendiculaires à la direction d'expansion (et dans les dépressions par des sections d'axe très obliques).La carte bathymétrique met en évidence des lignes de crêtes grossièrement Nord-Sud (007°) dont la direction diffère de la direction d'expansion (357°) déduite des reconstructions, et parallèle à la zone de fracture majeure Atlantis II. Sur les dorsales lentes, les zones de fractures mineures, n'indiqueraient donc pas la véritable direction d'expansion.
The axial region of the Southwest Indian Ridge between 53° E and 59° E: Evolution during the last 10 Ma
An interpretation of bathymetric and magnetic data obtained aboard the R/V Marion Dufresne provides us with new information concerning the evolution of the Southwest Indian Ridge, in the region of the Atlantis II Fracture Zone (57° E), since 10 Ma. On all profiles, the ridge axis and the axial magnetic anomaly have been clearly recognized. Bathymetric data illustrate the rapid variation of depth along the axis. On the western side of the Atlantis II Fracture Zone, the along axis profile is characterized by a succession of two highs, and an important depression between them.Our data show a strong relationship between the regional axial depth, the steep-sidedness of the axial valley and the signature of the central magnetic anomaly. In particular, where the axis is deepest (4500 m), there is a wide, shallow axial valley which is oblique to the spreading direction, and a non-typical central magnetic anomaly signature. In contrast, where the regional axial depth is shallow (3500 m), the axial valley is deep, narrow, perpendicular to the spreading direction, and the central magnetic anomaly is high in amplitude. The ridge axis on the western side of the Atlantis II Fracture Zone appears to consist of short segments located on the axial highs, which are linked by oblique zones. On the eastern side, the ridge axis is continuous, and appears to be oblique to the spreading direction.Clearly lineated magnetic anomalies 3A (5 Ma) and 5 (10 Ma) have been identified and mapped. These magnetic data allow a reconstruction which shows an evolution of the axial geometry since 10 Ma. On the western side of the Atlantis II Fracture Zone, the axis at anomaly 5 time consisted of segments perpendicular to the spreading direction which were offset by transform faults. On the eastern side, the isochron A5 appears to be parallel to the present-day ridge axis. From this plate reconstruction, a spreading direction of 357° was deduced, and appears to be parallel to the Atlantis II Fracture Zone.On each flank of the Suuthwest Indian Ridge, our bathymetric data show elongated ridges, aligned in a north-south direction, which correlate with the axial topographic highs. This direction is not precisely parallel to the spreading direction deduced from plate reconstruction. The differences in these directions suggest that transverse relief on show spreading ridge flanks (which could be interpreted as indicating the location of minor fracture zones) may not be indicative of the seafloor spreading direction.
  相似文献   

16.
Investigated is a possibility of two-dimensional model in the study of the dynamics of the western boundary current by a numerical experiment. Emphasis is laid on the effect of bottom barrier corresponding to the Izu Ridge.The western boundary current in the model is formed by source and sink of the water prescribed at an artificial eastern wall (600 km offshore). The bottom topographyconsists of a continental slope parallel to the straight western coast, and a ridge protruding from the western coast to 500 km offshore (1,500 m deep and 400 km wide). The grid size of 12 km× 25 km (offshore and longshore directions, respectively) resolves both the western boundary current and the bottom topography.The assumption of homogeneity of the water density makes the western boundary current detour along the isobath of the ridge.A steady state solution is obtained under the assumptions that the horizontal velocity does not change direction vertically (equivalent barotropic), and that the geostrophic relationship holds at the bottom. Homogeneity of the water density is not assumed. The solution shows that most of the volume transport of the western boundary current cross the ridge and the current has cyclonic vorticity near the summit of the ridge. It seems to suggest that the investigation by three-dimensional models is neccesary in order to study the complete dynamics of the western boundary current crossing the ridge.  相似文献   

17.
The detailed oceanic structure was observed near the shoal Kokusho-sone (3000N, 12830E), which is located near the axis of the Kuroshio in the East China Sea. The detailed temperature cross-sections along the meridian 12830E, which passes over the shoal, strongly suggest that upwelling is forced along the north slope of the shoal. The behavior of the coastal waters near the Kuroshio front and of the cold water belt along the north-western side of the Kuroshio are also discussed.  相似文献   

18.
The May 2001 Geoacoustic Inversion Techniques Workshop provided synthetic transmission loss (TL) data for four cases with range-dependent shallow-water all-liquid environments. In two of these cases ("0" and "1"), the sea floor has constant slope and the geoacoustic model (GAM) is range independent. Cost functions have been computed using a new adiabatic-mode TL algorithm (which uses an exact velocity boundary condition at the sloping sea floor), as one parameter in the GAM is varied. Two frequencies (80 and 220 Hz) were selected. In case 0, the sea-floor slope is 0.0183 and the GAM comprises an inhomogeneous layer over a basement. The sea-floor sound-speed was selected as the variable parameter. The resulting cost minima at 80 and 220 Hz are displaced from the actual sound speed by 2.3 and 3.4 m/s, respectively. In case 1, the sea-floor slope is 0.012 and the GAM comprises one homogenous layer, five inhomogeneous layers, and a basement. The selected parameter was the sound-speed in the homogeneous layer. The corresponding cost minima are displaced by -1.2 and +1.1 m/s. The relative values of these four errors indicate that mode coupling increases with sea-floor slope and that there may be a dependence on frequency at the greater slope.  相似文献   

19.
Hydrographic data show that the meridional deep current at 47°N is weak and southward in northeastern North Pacific; the strong northward current expected for an upwelling in a flat-bottom ocean is absent. This may imply that the eastward-rising bottom slope in the Northeast Pacific Basin contributes to the overturning circulation. After analysis of observational data, we examine the bottom-slope effect using models in which deep water enters the lower deep layer, upwells to the upper deep layer, and exits laterally. The analytical model is based on geostrophic hydrostatic balance, Sverdrup relation, and vertical advection–diffusion balance of density, and incorporates a small bottom slope and an eastward-increasing upwelling. Due to the sloping bottom, current in the lower deep layer intensifies bottomward, and the intensification is weaker for larger vertical eddy diffusivity (K V), weaker stratification, and smaller eastward increase in upwelling. Varying the value of K V changes the vertical structure and direction of the current; the current is more barotropic and flows further eastward as K V increases. The eastward current is reproduced with the numerical model that incorporates the realistic bottom-slope gradient and includes boundary currents. The interior current flows eastward primarily, runs up the bottom slope, and produces an upwelling. The eastward current has a realistic volume transport that is similar to the net inflow, unlike the large northward current for a flat bottom. The upwelling water in the upper deep layer flows southward and then westward in the southern region, although it may partly upwell further into the intermediate layer.  相似文献   

20.
We have investigated the fundamental processes of deep convection in a lake at high latitudes triggered by wind during spring or autumn and the associated deep water formation, executing vertically two-dimensional numerical experiments with a nonhydrostatic model. The water column in which a relatively cold mixed layer overlies a relatively warm layer becomes unstable, when the Ekman convergence on the shore due to along-shore wind deepens the mixed layer below the compensation depth, where water densities in both layers becomes equal to each other because of the thermobaric effect. At the onset of deep convection, the critical Rayleigh number agrees with that predicted by the linear theory. The onset time of deep convection is inversely proportional to the magnitude of wind stress. On the other hand, the onset time is minimal when water temperature in the mixed layer m is 3.1°C because a change of m has two effects oppositely acting on the stability of the water column. After the first onset, deep convection occurs intermittently for a few days. The sinking of the mixed layer water occurs in a thermal-like shape, and its amount is 4184% of the time-integrated Ekman transport when m 3°C while it decreases to less than 10% for m lower than 1.5°C. The present process can explain 30% of the amount of deep water renewal which is expected from the observation in Lake Baikal.  相似文献   

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