solve only part of the applied problems with qualitative evaluations or approximate
generalized quantitative characteristics.
Referring to the contact zone dynamics, special attention should be paid, besides
lithodynamics, to its second part, the hydrodynamics. This part does not play a great
role in the analysis of hydrogenic processes but it has its own applied significance,
particularly in the coastal dynamics. Elementary and complex hydrodynamic systems can be also distinguished in the hydrodynamics of the contact zone. Finally,
hydrodynamics of the contact zone must result in a complete picture of the whole
spectrum of speeds in the given dynamic setting in the bottom layers. This picture is
necessary for specific reliable computing expressions of the solid load discharge in
hydrogenic lithodynamic systems and for the solution of many other problems,
related to the physics of the ocean bottom contact zone.
As our knowledge of the contact zone lithodynamics increases, the construction
of physical models of increasingly more complex systems becomes possible,
though the transition from the models of the local systems to those of the regional
systems are yet far from being clear. It is quite possible that the solution of many
applied problems of the regional lithodynamics even in the future would require the
use of approximate qualitative evaluations and ideas.
Let us discuss some general features of the ocean lithodynamic systems. Comparison of the ocean hydrogenic systems and similar Earth systems shows that they
have basic differences. In the fluvial flows on the Earth surface, the water, being an
active agent, flows in a restricted channel due to the composite gravity determined
by the flow gradient. Thus, a surface water flow eroding its channel is at the
same time governed by this channel, and the flow speed depends directly on the
properties of this channel. In the hydrogenic ocean flows, the underlying surface
“governs” the flow to the extent, to which it (together with the transported sediment) dissipates the energy of the flow. The source of this energy is outside the
contact zone and does not depend on the character of the surface underlying the
flow. When describing the evolution of the fluvial flows, Velikanov (1948) tried to
use a principle of the system’s striving for the minimum dissipation of the flow
energy, but in the ocean this suggestion is not true, and striving for complete
dissipation of the flow energy with the minimum power of dissipation process is
most likely the general principle of the development of ocean lithodynamic system.
Morphologically this tendency manifests itself in striving for the increase in the
energy dissipation and decrease of the gradient, which can be observed when the
equilibrium profile is worked out in the coastal zone.
7.3 The Basic Properties of the Coastal Zone
Hydrodynamics
Water motion in the coastal zone is determined by external forcing. It is manifested
as tidal currents, swell, and wind waves, various kinds of wave currents generated
in the wind waves breaking zone as storm surges, and tsunami. Recurrence of these
7 Lithodynamics of the Coastal Zone
123
generalized quantitative characteristics.
Referring to the contact zone dynamics, special attention should be paid, besides
lithodynamics, to its second part, the hydrodynamics. This part does not play a great
role in the analysis of hydrogenic processes but it has its own applied significance,
particularly in the coastal dynamics. Elementary and complex hydrodynamic systems can be also distinguished in the hydrodynamics of the contact zone. Finally,
hydrodynamics of the contact zone must result in a complete picture of the whole
spectrum of speeds in the given dynamic setting in the bottom layers. This picture is
necessary for specific reliable computing expressions of the solid load discharge in
hydrogenic lithodynamic systems and for the solution of many other problems,
related to the physics of the ocean bottom contact zone.
As our knowledge of the contact zone lithodynamics increases, the construction
of physical models of increasingly more complex systems becomes possible,
though the transition from the models of the local systems to those of the regional
systems are yet far from being clear. It is quite possible that the solution of many
applied problems of the regional lithodynamics even in the future would require the
use of approximate qualitative evaluations and ideas.
Let us discuss some general features of the ocean lithodynamic systems. Comparison of the ocean hydrogenic systems and similar Earth systems shows that they
have basic differences. In the fluvial flows on the Earth surface, the water, being an
active agent, flows in a restricted channel due to the composite gravity determined
by the flow gradient. Thus, a surface water flow eroding its channel is at the
same time governed by this channel, and the flow speed depends directly on the
properties of this channel. In the hydrogenic ocean flows, the underlying surface
“governs” the flow to the extent, to which it (together with the transported sediment) dissipates the energy of the flow. The source of this energy is outside the
contact zone and does not depend on the character of the surface underlying the
flow. When describing the evolution of the fluvial flows, Velikanov (1948) tried to
use a principle of the system’s striving for the minimum dissipation of the flow
energy, but in the ocean this suggestion is not true, and striving for complete
dissipation of the flow energy with the minimum power of dissipation process is
most likely the general principle of the development of ocean lithodynamic system.
Morphologically this tendency manifests itself in striving for the increase in the
energy dissipation and decrease of the gradient, which can be observed when the
equilibrium profile is worked out in the coastal zone.
7.3 The Basic Properties of the Coastal Zone
Hydrodynamics
Water motion in the coastal zone is determined by external forcing. It is manifested
as tidal currents, swell, and wind waves, various kinds of wave currents generated
in the wind waves breaking zone as storm surges, and tsunami. Recurrence of these
7 Lithodynamics of the Coastal Zone
123