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Fig. llc. Pattern of mass transport based on a 2.3-year numerical integration of a three-dimensional model using ob- served density and mass transport of Figure 118 as initial conditions {from Cox, 1975).

Figure 118 llc. Pattern of mass transport based on a 2.3-year numerical integration of a three-dimensional model using ob- served density and mass transport of Figure 118 as initial conditions {from Cox, 1975).

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venient pair to discuss together. Veronis’s [1966] parallels that of Stommel [1948], with the aneuon of time dependent and inertial terms, while Bryan’s tl 963] model parallels that of Munk [1950]. The rigid lid approximation allows a specification of the motion in terms of a volume transport stream function ¥, where
venient pair to discuss together. Veronis’s [1966] parallels that of Stommel [1948], with the aneuon of time dependent and inertial terms, while Bryan’s tl 963] model parallels that of Munk [1950]. The rigid lid approximation allows a specification of the motion in terms of a volume transport stream function ¥, where
A is the horizontal eddy viscosity, K a bottom friction or drag law coefficient, and 7 the stress at the surface. “Nonslip boundary condition on the east and west walls only. Free slip on the north and south boundaries. TABLE 1. Characteristics of Mechanistic Models of the Wind-Driven Ocean Circulation
A is the horizontal eddy viscosity, K a bottom friction or drag law coefficient, and 7 the stress at the surface. “Nonslip boundary condition on the east and west walls only. Free slip on the north and south boundaries. TABLE 1. Characteristics of Mechanistic Models of the Wind-Driven Ocean Circulation
Fig. 2. Patterns of transport stream function for a homogeneous wind-driven ocean. (a) Bottom friction, free slip at the side walls; (6) lateral friction, free slip at the side walls; (c) lateral friction, no slip at the side walls [from Blandford, 1971].
Fig. 2. Patterns of transport stream function for a homogeneous wind-driven ocean. (a) Bottom friction, free slip at the side walls; (6) lateral friction, free slip at the side walls; (c) lateral friction, no slip at the side walls [from Blandford, 1971].
Fig. 3. A time-dependent solution for a homogeneous, frees .rface model. (a) Elevation of the free surface, (6) isopleths (north-south) of the v component of velocity [from Gates, 1968].
Fig. 3. A time-dependent solution for a homogeneous, frees .rface model. (a) Elevation of the free surface, (6) isopleths (north-south) of the v component of velocity [from Gates, 1968].
baroclinicity can produce transport which is enhanced com- pared with what one gets in the level bottom case. This effect has also been studied by Sarkisyan and Ivanov [1971] and termed the joint effect of baroclinicity and bottom topography. There is a bottom pressure torque term in the vorticity equa- tion which is normally omitted in wind-driven circulation studies by assuming either that the bottom is level or that the flow near the bottom is zero due to baroclinic compensation leading to the Sverdrup equation. This term cannot be handled analytically in the realistic baroclinic case. The bottom pres- sure torque also plays a role in case 2 and is responsible for reducing the total transport. The term involved is the one involving current near the bottom and bottom slopes. A der- ivation of this term may also be found in Fofonoff [1962]. interior corresponding to the disturbances discussed in con- nection with the two-layer model of Holland and Lin [1975]. Most of the energy in the mean is potential energy associated with the density structure. Because of the very small spatial scale and the long time scale, the logistics of getting good observations of these oceanic eddies are extremely difficult. Large efforts have been made by groups from the USSR (the Polygon experiment) and the United States-United Kingdom (the midocean dynamics experiment of Mode). Each has ob- served one eddy fairly well and fringes of others. How preva- lent these eddies are in different geographical areas of the ocean is unknown at present, although there is fragmentary evidence in the variability of historical data. The analogs of these oceanic eddies in the atmosphere are the storm systems in mid-latitudes. On a weather map the storm systems look like a series of large eddies. These ‘eddies’ can be considered to be geostrophic turbulence which behaves like two-dimensional turbulence [Charney, 1971]. The eddies gain energy from the available mean potential energy and transfer kinetic energy and momentum to larger scales and to the mean flow. They are
baroclinicity can produce transport which is enhanced com- pared with what one gets in the level bottom case. This effect has also been studied by Sarkisyan and Ivanov [1971] and termed the joint effect of baroclinicity and bottom topography. There is a bottom pressure torque term in the vorticity equa- tion which is normally omitted in wind-driven circulation studies by assuming either that the bottom is level or that the flow near the bottom is zero due to baroclinic compensation leading to the Sverdrup equation. This term cannot be handled analytically in the realistic baroclinic case. The bottom pres- sure torque also plays a role in case 2 and is responsible for reducing the total transport. The term involved is the one involving current near the bottom and bottom slopes. A der- ivation of this term may also be found in Fofonoff [1962]. interior corresponding to the disturbances discussed in con- nection with the two-layer model of Holland and Lin [1975]. Most of the energy in the mean is potential energy associated with the density structure. Because of the very small spatial scale and the long time scale, the logistics of getting good observations of these oceanic eddies are extremely difficult. Large efforts have been made by groups from the USSR (the Polygon experiment) and the United States-United Kingdom (the midocean dynamics experiment of Mode). Each has ob- served one eddy fairly well and fringes of others. How preva- lent these eddies are in different geographical areas of the ocean is unknown at present, although there is fragmentary evidence in the variability of historical data. The analogs of these oceanic eddies in the atmosphere are the storm systems in mid-latitudes. On a weather map the storm systems look like a series of large eddies. These ‘eddies’ can be considered to be geostrophic turbulence which behaves like two-dimensional turbulence [Charney, 1971]. The eddies gain energy from the available mean potential energy and transfer kinetic energy and momentum to larger scales and to the mean flow. They are
Fig. 5. Patterns of flow in a study of bottom pressure torques. (a) Thermohaline circulation, but uniform depth; (5) uniform density and bottom topography; (c) thermohaline circulation combined with bottom topography [from Holland, 1973]. POND AND BRYAN: NUMERICAL MODELS OF THE OCEAN CIRCUI ATION
Fig. 5. Patterns of flow in a study of bottom pressure torques. (a) Thermohaline circulation, but uniform depth; (5) uniform density and bottom topography; (c) thermohaline circulation combined with bottom topography [from Holland, 1973]. POND AND BRYAN: NUMERICAL MODELS OF THE OCEAN CIRCUI ATION
Fig. 6. (a) Spectra of a two-layer model with open boundaries; k, is the wave number corresponding to the radius of deformation; KE, is the kinetic energy for upper and lower layers, respectively. (b) A time-space plot of the stream func- tion in each layer [from Rhines, 1973a].
Fig. 6. (a) Spectra of a two-layer model with open boundaries; k, is the wave number corresponding to the radius of deformation; KE, is the kinetic energy for upper and lower layers, respectively. (b) A time-space plot of the stream func- tion in each layer [from Rhines, 1973a].
TABLE 2. Description of the Different Parameters for the Four Experiments [Orlanski and Cox, 1973]
TABLE 2. Description of the Different Parameters for the Four Experiments [Orlanski and Cox, 1973]
Fig. 7. Results from a study of unstable waves in the Gulf Stream. (a) Growth of the amplitude of the most unstable wave as a function of time. (6) Development of the spectrum [from Orlanski and Cox, 1973]. POND AND BRYAN: NUMERICAL MODELS OF THE OCEAN CIRCULATION
Fig. 7. Results from a study of unstable waves in the Gulf Stream. (a) Growth of the amplitude of the most unstable wave as a function of time. (6) Development of the spectrum [from Orlanski and Cox, 1973]. POND AND BRYAN: NUMERICAL MODELS OF THE OCEAN CIRCULATION
Fig.8. Transport stream function computed for a wind-driven model of uniform density. (a) The circulation pattern at the western boundary; transport is given in sverdrups (10° m?/s). (6) The pattern over the entire basin [from O’Brien, 1971}.
Fig.8. Transport stream function computed for a wind-driven model of uniform density. (a) The circulation pattern at the western boundary; transport is given in sverdrups (10° m?/s). (6) The pattern over the entire basin [from O’Brien, 1971}.
Fig. 9. Cross sections showing the longshore velocity at the Somali Coast in an Indian Ocean model: (a) during the south- west monsoon, (b) the winter during the northeast monsoon [from Cox, 1970]. POND AND BRYAN: NUMERICAL MODELS OF THE OCEAN CIRCULATION
Fig. 9. Cross sections showing the longshore velocity at the Somali Coast in an Indian Ocean model: (a) during the south- west monsoon, (b) the winter during the northeast monsoon [from Cox, 1970]. POND AND BRYAN: NUMERICAL MODELS OF THE OCEAN CIRCULATION
Fig. 10. Transport stream function patterns based on diagnostic calculations based on the observed density field: (a) the case of uniform density; (b) observed density field, but the ocean is assumed to have a uniform depth of 1273 m; (c) realistic case of observed density field and bottom topography, allowing bottom pressure torques [from Holland and Hirschman. 1972].
Fig. 10. Transport stream function patterns based on diagnostic calculations based on the observed density field: (a) the case of uniform density; (b) observed density field, but the ocean is assumed to have a uniform depth of 1273 m; (c) realistic case of observed density field and bottom topography, allowing bottom pressure torques [from Holland and Hirschman. 1972].
Fig. 11a. Pattern of mass transport stream function for a world ocean of uniform density [from Bryan and Cox, 1972].
Fig. 11a. Pattern of mass transport stream function for a world ocean of uniform density [from Bryan and Cox, 1972].
Fig. 11. Pattern of mass transport for the diagnostic case based on the observed density field [from Cox, 1975]
Fig. 11. Pattern of mass transport for the diagnostic case based on the observed density field [from Cox, 1975]