Search Results
Abstract
The theory of the evolution of rings under a Cooling atmosphere is extended in two ways. First effects of stratification are studied analytically through the use of a “two and one-half” layer model. Second, model predictions are compared with observations. Qualitative support of the analytical model is also provided by a brief comparison of the analytical predictions with a numerical model.
Ring evolution is computed using the conservation of angular momentum. Idealizations in the analytical model include zero potential vorticity in the upper layer and an infinitely deep and resting third layer. The results from the analytical model witch is based on a crude representation of fluid thermodynamics and a continuously stratified numerical model with an active mixed layer agree qualitatively. Further, both models yield predictions of main thermocline deepening under warm rings which are consistent with field observations. This agreement supports the idea that the response of warm rings to cooling is governed by Rossby adjustmentlike mechanics.
Abstract
The theory of the evolution of rings under a Cooling atmosphere is extended in two ways. First effects of stratification are studied analytically through the use of a “two and one-half” layer model. Second, model predictions are compared with observations. Qualitative support of the analytical model is also provided by a brief comparison of the analytical predictions with a numerical model.
Ring evolution is computed using the conservation of angular momentum. Idealizations in the analytical model include zero potential vorticity in the upper layer and an infinitely deep and resting third layer. The results from the analytical model witch is based on a crude representation of fluid thermodynamics and a continuously stratified numerical model with an active mixed layer agree qualitatively. Further, both models yield predictions of main thermocline deepening under warm rings which are consistent with field observations. This agreement supports the idea that the response of warm rings to cooling is governed by Rossby adjustmentlike mechanics.
Abstract
A two-layer model of the general circulation including wind and thermal forcing is discussed. The flow in each layer is geostrophic, hydrostatic and obeys linear potential vorticity constraints. The equations are developed in spherical coordinates and reduce to a surprisingly simple, coupled, nonlinear set. Analytic solutions of this system are obtained in the quasi-geostrophic limit. The novel feature in this model is a weakly ventilated and weakly dissipative lower layer.
The quasi-geostrophic model predicts homogenized potential vorticity is regions of the lower layer which are not directly ventilated. These are also regions of locally minimum value in potential vorticity. The net balance determining the potential vorticity structure is between the diabatic forcing of the lower layer and eddy-drive mixing. As such, the structure of the solution depends on the sign of the eddy diffusion of potential vorticity (positive) and the sign of the diabatic potential vorticity source (negative). It is therefore argued that these features and not dependent on quasi-geostrophy.
A comparison of model results with data is encouraging. The 26.5 sigma-theta isopycnal is argued to be a density surface to which this theory applies. The potential vorticity structure on this surface obtains a bowl-like shape and agrees well with the model. The subtropical mode water of the North Atlantic (18°C water) is centered on this isopycnal and is identified in the model as the homogenized local potential vorticity minimum. The stability of 18°C water characteristics, documented elsewhere, is explained in terms of a gyre-scale response to variability.
Abstract
A two-layer model of the general circulation including wind and thermal forcing is discussed. The flow in each layer is geostrophic, hydrostatic and obeys linear potential vorticity constraints. The equations are developed in spherical coordinates and reduce to a surprisingly simple, coupled, nonlinear set. Analytic solutions of this system are obtained in the quasi-geostrophic limit. The novel feature in this model is a weakly ventilated and weakly dissipative lower layer.
The quasi-geostrophic model predicts homogenized potential vorticity is regions of the lower layer which are not directly ventilated. These are also regions of locally minimum value in potential vorticity. The net balance determining the potential vorticity structure is between the diabatic forcing of the lower layer and eddy-drive mixing. As such, the structure of the solution depends on the sign of the eddy diffusion of potential vorticity (positive) and the sign of the diabatic potential vorticity source (negative). It is therefore argued that these features and not dependent on quasi-geostrophy.
A comparison of model results with data is encouraging. The 26.5 sigma-theta isopycnal is argued to be a density surface to which this theory applies. The potential vorticity structure on this surface obtains a bowl-like shape and agrees well with the model. The subtropical mode water of the North Atlantic (18°C water) is centered on this isopycnal and is identified in the model as the homogenized local potential vorticity minimum. The stability of 18°C water characteristics, documented elsewhere, is explained in terms of a gyre-scale response to variability.
Abstract
Observations suggest that heat loss to the atmosphere causes an important modification of the density structure of warm core rings. In this study, f-plane models of rings under a cooling atmosphere are examined in order to provide a dynamic framework for the interpretation of ring observations and to assess ring effects on their environment.
Two-layer models with finite upper-layer volumes are examined The idealizations in these models include zero potential vorticity in the ring and an initially motionless lower layer. In the simplest problem, the atmosphere is assumed to completely remove the heat anomaly of the ring through cooling. The results of this calculation place limits on the restructuring of warm rings that can be forced by heat exchange. The time-dependent ventilation problem is also examined by considering the effects of partial heat withdrawals and cold air outbreaks. Estimates of energy release by rings during adjustment are large, suggesting the flux of significant energy into the internal wave bands by a single cooling event.
Abstract
Observations suggest that heat loss to the atmosphere causes an important modification of the density structure of warm core rings. In this study, f-plane models of rings under a cooling atmosphere are examined in order to provide a dynamic framework for the interpretation of ring observations and to assess ring effects on their environment.
Two-layer models with finite upper-layer volumes are examined The idealizations in these models include zero potential vorticity in the ring and an initially motionless lower layer. In the simplest problem, the atmosphere is assumed to completely remove the heat anomaly of the ring through cooling. The results of this calculation place limits on the restructuring of warm rings that can be forced by heat exchange. The time-dependent ventilation problem is also examined by considering the effects of partial heat withdrawals and cold air outbreaks. Estimates of energy release by rings during adjustment are large, suggesting the flux of significant energy into the internal wave bands by a single cooling event.
Abstract
A number of general circulation models have recently been proposed that compute the steady-state structure of the general circulation. Observation of 18°C water formation, on the other hand, suggest the need for a study of the time-dependent large-scale structure of the oceans. In this paper, the planetary geostrophic equations are used to compute the evolution of large thermal anomalies with a view toward understanding the variability in the general circulation caused by water mass formation events.
The evolution of a thermal anomaly is considered in the absence of wind forcing. In this case, the planetary geostrophic equations can be reduced to a first-order equations, the Planetary Geostrophic Wave Equation (PGWE). Arbitrary initial conditions governed by the PGWE tend to steepen and, under an assumed diffusive closure, from shock waves. The evolution of an initially columnar eddy is obtained, and four different phases of shock propagation are identified. The implications for heat transport, potential vorticity transport and thermocline ventilation are discussed.
Abstract
A number of general circulation models have recently been proposed that compute the steady-state structure of the general circulation. Observation of 18°C water formation, on the other hand, suggest the need for a study of the time-dependent large-scale structure of the oceans. In this paper, the planetary geostrophic equations are used to compute the evolution of large thermal anomalies with a view toward understanding the variability in the general circulation caused by water mass formation events.
The evolution of a thermal anomaly is considered in the absence of wind forcing. In this case, the planetary geostrophic equations can be reduced to a first-order equations, the Planetary Geostrophic Wave Equation (PGWE). Arbitrary initial conditions governed by the PGWE tend to steepen and, under an assumed diffusive closure, from shock waves. The evolution of an initially columnar eddy is obtained, and four different phases of shock propagation are identified. The implications for heat transport, potential vorticity transport and thermocline ventilation are discussed.
Abstract
Simple analytical and numerical models of gratified circulation are discussed. The models are driven by buoyancy and mechanical forcing, and buoyancy diffusion is parameterized in term of diapycnal mass fluxes. The interior responds in typical Sverdrup fashion, and the requirements of balanced heat and energy budgets are invoked to calculate the eastern boundary stratification parameters.
This effort differs from past attempts to calculate stratification in that buoyancy flux boundary conditions or explicitly considered in the calculation of diapycnal fluxes. A major feature of the solutions is the interplay of planetary dynamics and buoyancy diffusion. This results in the most important components of the thermocline structure, namely density outcrops and interior “pinchoffs.” These are, in turn, essential to the production of thermodynamically balanced states. Some aspects of the present model resemble features found in previous numerical models.
Abstract
Simple analytical and numerical models of gratified circulation are discussed. The models are driven by buoyancy and mechanical forcing, and buoyancy diffusion is parameterized in term of diapycnal mass fluxes. The interior responds in typical Sverdrup fashion, and the requirements of balanced heat and energy budgets are invoked to calculate the eastern boundary stratification parameters.
This effort differs from past attempts to calculate stratification in that buoyancy flux boundary conditions or explicitly considered in the calculation of diapycnal fluxes. A major feature of the solutions is the interplay of planetary dynamics and buoyancy diffusion. This results in the most important components of the thermocline structure, namely density outcrops and interior “pinchoffs.” These are, in turn, essential to the production of thermodynamically balanced states. Some aspects of the present model resemble features found in previous numerical models.
Abstract
Two models of the oceanic response to cooling are discussed. Both are motivated by a desire to understand the effects of variable diabatic forcing on the general circulation. The first model considers an initial value problem in which an initially resting warm ocean is “slowly”cooled on "broad”scales. The lower layer in this model is fully active and it is further argued that the slow and broad scales are relevant to 1 8°C water formation. The purpose of this model is to illustrate the short term barotropic and baroclinic response to variability in thermal forcing.
The second problem addresses the longer-term evolution of finite amplitude thermocline anomalies (which are assumed to have been formed by diabatic effects). A “one and three-quarter”model is used. i.e., the lower layer is assumed to be deep, but not stagnant, and its evolution is computed.
Based on these models, it is argued that diabatic forcing can result in local modifications of the Sverdrup constraint and that mass transport evolves through at least three distinct phases. The first short-term ocean response to cooling is the radiation of eastward moving barotropic planetary waves, which leaves the Sverdrup transport and the planetary geostrophic wave equation (PGWE) in its wake. Local Sverdrup dynamics and the PGWE dominate the second phase of evolution. The last phase occurs as the fronts obtain deformation radius length scales, and the tendency for the system to produce coherent structures results in persistent, spreading regions of anomalous transport. Global measures of the mass transport, however, are in agreement with the classic Sverdrup constraint. Implications for the generation of barotropic and baroclinic variability are discussed.
Abstract
Two models of the oceanic response to cooling are discussed. Both are motivated by a desire to understand the effects of variable diabatic forcing on the general circulation. The first model considers an initial value problem in which an initially resting warm ocean is “slowly”cooled on "broad”scales. The lower layer in this model is fully active and it is further argued that the slow and broad scales are relevant to 1 8°C water formation. The purpose of this model is to illustrate the short term barotropic and baroclinic response to variability in thermal forcing.
The second problem addresses the longer-term evolution of finite amplitude thermocline anomalies (which are assumed to have been formed by diabatic effects). A “one and three-quarter”model is used. i.e., the lower layer is assumed to be deep, but not stagnant, and its evolution is computed.
Based on these models, it is argued that diabatic forcing can result in local modifications of the Sverdrup constraint and that mass transport evolves through at least three distinct phases. The first short-term ocean response to cooling is the radiation of eastward moving barotropic planetary waves, which leaves the Sverdrup transport and the planetary geostrophic wave equation (PGWE) in its wake. Local Sverdrup dynamics and the PGWE dominate the second phase of evolution. The last phase occurs as the fronts obtain deformation radius length scales, and the tendency for the system to produce coherent structures results in persistent, spreading regions of anomalous transport. Global measures of the mass transport, however, are in agreement with the classic Sverdrup constraint. Implications for the generation of barotropic and baroclinic variability are discussed.
Abstract
Midocean fronts have by now been well documented in the World Ocean. In view of this, a general circulation theory that admits interior fronts is considered in this paper and a new class of frontal solutions is discussed. The present solutions are distinguished by having fronts that originate at locations within the interior of the circulation. The locations of the front origins do not depend upon local effects; rather, they are set by conditions far from the front. Such fronts are thus referred to as “spontaneous shocks.” They occur in adiabatic wind-driven models, and participate in the ventilated thermocline. Indeed, calculating basin conditions that result in spontaneous shocks is a central objective of this paper. Aspects of some observed fronts also have counterparts in the theory, and it is suggested that spontaneous shocks in the ventilated thermocline resemble certain North Pacific observations.
Abstract
Midocean fronts have by now been well documented in the World Ocean. In view of this, a general circulation theory that admits interior fronts is considered in this paper and a new class of frontal solutions is discussed. The present solutions are distinguished by having fronts that originate at locations within the interior of the circulation. The locations of the front origins do not depend upon local effects; rather, they are set by conditions far from the front. Such fronts are thus referred to as “spontaneous shocks.” They occur in adiabatic wind-driven models, and participate in the ventilated thermocline. Indeed, calculating basin conditions that result in spontaneous shocks is a central objective of this paper. Aspects of some observed fronts also have counterparts in the theory, and it is suggested that spontaneous shocks in the ventilated thermocline resemble certain North Pacific observations.
Abstract
Convection in the world's oceans often occurs in small, semienclosed basins where bottom slopes and nearby continental shelf breaks are commonplace. The evolution of convectively generated heat anomalies in such settings is studied using quasigeostrophic finite-difference and point vortex models. The displayed behaviors divide essentially into two categories: whole fluid column convection, in which bottom-slope effects are felt immediately, and partial fluid column convection, in which the topographic effects can be delayed. In both cases, topography significantly modifies the evolution of convective patches from that occurring over flat bottoms. Vertical walls induce strong self-propagation mechanisms that accelerate alongslope heat transport, while the continental shelf slope is repulsive and rejects lower-layer anticyclones. These anomalies are then “stranded,” being too far offshore to interact with the shelf break and having lost their heton partner in the interaction. Weaker deep ocean topographic slopes disrupt heton formation and disperse convective patches by topographic mechanisms. Partial fluid column convection, with stratification under the mixed layer, proceeds through a cascade from small to large length scales. In oceanically relevant regimes, smaller scales are shielded from bottom slopes and can disperse as small hetons. Larger-scale structures are prevented by the topography from forming into hetons and instead evolve as if in a sloping-bottom two-layer system. The small hetons, when encountering shelf breaks, can experience topographic repulsion and stranding. Comparisons with the Mediterranean Sea suggest alternative interpretations for some observations, and several observed Labrador Sea mesoscale convective characteristics can be ascribed to topographic effects.
Abstract
Convection in the world's oceans often occurs in small, semienclosed basins where bottom slopes and nearby continental shelf breaks are commonplace. The evolution of convectively generated heat anomalies in such settings is studied using quasigeostrophic finite-difference and point vortex models. The displayed behaviors divide essentially into two categories: whole fluid column convection, in which bottom-slope effects are felt immediately, and partial fluid column convection, in which the topographic effects can be delayed. In both cases, topography significantly modifies the evolution of convective patches from that occurring over flat bottoms. Vertical walls induce strong self-propagation mechanisms that accelerate alongslope heat transport, while the continental shelf slope is repulsive and rejects lower-layer anticyclones. These anomalies are then “stranded,” being too far offshore to interact with the shelf break and having lost their heton partner in the interaction. Weaker deep ocean topographic slopes disrupt heton formation and disperse convective patches by topographic mechanisms. Partial fluid column convection, with stratification under the mixed layer, proceeds through a cascade from small to large length scales. In oceanically relevant regimes, smaller scales are shielded from bottom slopes and can disperse as small hetons. Larger-scale structures are prevented by the topography from forming into hetons and instead evolve as if in a sloping-bottom two-layer system. The small hetons, when encountering shelf breaks, can experience topographic repulsion and stranding. Comparisons with the Mediterranean Sea suggest alternative interpretations for some observations, and several observed Labrador Sea mesoscale convective characteristics can be ascribed to topographic effects.
Abstract
Point vortex and finite-difference methods are used to study baroclinic eddies advected into weak and strong encounters with topography. It is argued that weak interactions often scatter radially symmetric eddies into generalized hetons. The dipole moments so generated within the eddy result in eddy propagations at various angles to the current. Strong interactions can result in the complete separation of the upper- and lower-layer circulations. Subsequent evolution in this case depends on many factors, although strong topographic obstacles (i.e., seamounts) permit a reorganization of the centers into a coherent structure. Weaker topography, confined to the deep ocean, can disrupt the lower center, although the upper center typically survives. Disassociation of the centers with both retaining their integrity is also possible. Heton generation can occur for eddies with weak lower-layer expressions, demonstrating a potentially strong control of shallow eddy propagation by deep sea bathymetry. Analytical and numerical estimates of the induced propagation speeds are sizable, arguing topographic scattering is a potentially powerful mechanism influencing eddy propagation.
Abstract
Point vortex and finite-difference methods are used to study baroclinic eddies advected into weak and strong encounters with topography. It is argued that weak interactions often scatter radially symmetric eddies into generalized hetons. The dipole moments so generated within the eddy result in eddy propagations at various angles to the current. Strong interactions can result in the complete separation of the upper- and lower-layer circulations. Subsequent evolution in this case depends on many factors, although strong topographic obstacles (i.e., seamounts) permit a reorganization of the centers into a coherent structure. Weaker topography, confined to the deep ocean, can disrupt the lower center, although the upper center typically survives. Disassociation of the centers with both retaining their integrity is also possible. Heton generation can occur for eddies with weak lower-layer expressions, demonstrating a potentially strong control of shallow eddy propagation by deep sea bathymetry. Analytical and numerical estimates of the induced propagation speeds are sizable, arguing topographic scattering is a potentially powerful mechanism influencing eddy propagation.
Abstract
Ocean adjustment on annual to interdecadal scales to variable forcing is considered for a more nonlinear general circulation than has previously been studied. The nature of the response is a strong function of forcing frequency and importantly involves the inertial recirculations rather than linear baroclinic waves. The spatial expression of this variability is concentrated near the separation latitudes of the Gulf Stream extension, a model region corresponding to an area in the real ocean of well-known strong ocean–atmosphere buoyancy exchange. “Turn-on” cases, periodically forced cases, and stochastically forced cases are considered. The first set of experiments clarifies the adjustment timescales and dynamics of a nonlinear circulation. The second set examines modifications to that adjustment rendered by time-dependent forcing. The last set is perhaps the most realistic in terms of the atmospheric forcing of the ocean, because wind spectra are not strongly peaked beyond a few weeks. Multidecadal forcing is argued both to excite a novel, rapid mode of adjustment and to resonate with a considerably slower, nonlinear mode. Stochastic forcing seems clearly to excite the fast mode and to contribute to the slower mode, although the latter also derives considerable variance from intrinsic sources. These conclusions are based on a suite of distinct spatial and temporal characteristics of the dominant ocean variability patterns under various forcing scenarios and comment on the ocean dynamics likely to be important to decadal timescale midlatitude climate variability.
Abstract
Ocean adjustment on annual to interdecadal scales to variable forcing is considered for a more nonlinear general circulation than has previously been studied. The nature of the response is a strong function of forcing frequency and importantly involves the inertial recirculations rather than linear baroclinic waves. The spatial expression of this variability is concentrated near the separation latitudes of the Gulf Stream extension, a model region corresponding to an area in the real ocean of well-known strong ocean–atmosphere buoyancy exchange. “Turn-on” cases, periodically forced cases, and stochastically forced cases are considered. The first set of experiments clarifies the adjustment timescales and dynamics of a nonlinear circulation. The second set examines modifications to that adjustment rendered by time-dependent forcing. The last set is perhaps the most realistic in terms of the atmospheric forcing of the ocean, because wind spectra are not strongly peaked beyond a few weeks. Multidecadal forcing is argued both to excite a novel, rapid mode of adjustment and to resonate with a considerably slower, nonlinear mode. Stochastic forcing seems clearly to excite the fast mode and to contribute to the slower mode, although the latter also derives considerable variance from intrinsic sources. These conclusions are based on a suite of distinct spatial and temporal characteristics of the dominant ocean variability patterns under various forcing scenarios and comment on the ocean dynamics likely to be important to decadal timescale midlatitude climate variability.
