390
A. V. Panko et al.
sediments on marine slopes. Such transformations can lead to stress (catastrophic)
processes. The conducted preliminary studies of mineralogical processes in the Earth
crust [4–7] also agree with conclusions from the work [30], and they are important for
the development of similar ideas of physicochemical geomechanics in the theory of
catastrophes. It can be developed with the help of rheological method and phenomena
of elastic–plastic, ultraanomal, and hyperanomal dispersion flow [4–6, 21–28].
4.2 Modeling of Geomechanical Catastrophic Processes
in Sediments on Marine Slopes
Indicated phenomena and processes occur in conditions of accumulating of disperse
turbiditic-pelitic marine sediments [4–6, 21–28, 30]. The conditions of accumulation
are connected in the first place with the geography of sedimentary basin, its distance
from the coast, and where the terrigene material is mixing. It is also connected
with the conditions of water circulation in dependence of wind, thermophilic and
other processes. In dependence of geological factors, the sediments are accumulated on different areas of slopes and marine bottom: shelf (depth up to 200 m),
continental slopes, on the bottom of deep-water channels and basins, abyssal (deepwater) plains with abyssal hills with height from 50 to 500 m, and on the tops of
more high underwater rises (mountains). Overall, with the change of natural and
geological conditions, especially with the change of the character of surface and
underwater thermophilic waves under the influence of wind current forces that can
reach the level of typhoon and tsunami, the sediments are accumulating on the bottom
of deep-water channels, basins, and on abyssal plains. In other cases, the turbiditicpelitic sediments sooner or later will also move to indicated areas of marine bottom.
As a rule, such processes occur for tens of thousands and millions of years. In the
geological epochs according to the laws of colloid chemistry and physicochemical
geomechanics, all of them can compact in conditions of initial coagulation–condensation processes within thousands of years, and in the course of time, they can
compact up to solid rocky state. Thus, the most interesting from the point of view of
formation of catastrophic processes of fast shifts are sediments, which accumulate in
quite huge quantities within thousands of years on continental slopes and on slopes
of underwater mountains of volcanic origin on abyssal plains [31, 32]. The model
scheme of such processes is given in Fig. 6.
The most widespread between sediments, which supply the slopes and marine
bottom, are the pelagic oozes with additives of biogenic (biocolloidal) sediments, and
the turbidity deposits that are forming at intensive turbulent wind-wave circulations,
for example, typhoons. At this, the dispersive action of formed sea waves can reach
on the depth of a few kilometers instead of the usual 500–700 m 500–700 m [31].
Pelagic sediments along with turbidities in most cases were accumulated for the
last 18 millions of years in shelf sea zones during the denudation processes, and on
the slopes of underwater hills and mountains (pelitic deposits) [31, 32]. The character
A. V. Panko et al.
sediments on marine slopes. Such transformations can lead to stress (catastrophic)
processes. The conducted preliminary studies of mineralogical processes in the Earth
crust [4–7] also agree with conclusions from the work [30], and they are important for
the development of similar ideas of physicochemical geomechanics in the theory of
catastrophes. It can be developed with the help of rheological method and phenomena
of elastic–plastic, ultraanomal, and hyperanomal dispersion flow [4–6, 21–28].
4.2 Modeling of Geomechanical Catastrophic Processes
in Sediments on Marine Slopes
Indicated phenomena and processes occur in conditions of accumulating of disperse
turbiditic-pelitic marine sediments [4–6, 21–28, 30]. The conditions of accumulation
are connected in the first place with the geography of sedimentary basin, its distance
from the coast, and where the terrigene material is mixing. It is also connected
with the conditions of water circulation in dependence of wind, thermophilic and
other processes. In dependence of geological factors, the sediments are accumulated on different areas of slopes and marine bottom: shelf (depth up to 200 m),
continental slopes, on the bottom of deep-water channels and basins, abyssal (deepwater) plains with abyssal hills with height from 50 to 500 m, and on the tops of
more high underwater rises (mountains). Overall, with the change of natural and
geological conditions, especially with the change of the character of surface and
underwater thermophilic waves under the influence of wind current forces that can
reach the level of typhoon and tsunami, the sediments are accumulating on the bottom
of deep-water channels, basins, and on abyssal plains. In other cases, the turbiditicpelitic sediments sooner or later will also move to indicated areas of marine bottom.
As a rule, such processes occur for tens of thousands and millions of years. In the
geological epochs according to the laws of colloid chemistry and physicochemical
geomechanics, all of them can compact in conditions of initial coagulation–condensation processes within thousands of years, and in the course of time, they can
compact up to solid rocky state. Thus, the most interesting from the point of view of
formation of catastrophic processes of fast shifts are sediments, which accumulate in
quite huge quantities within thousands of years on continental slopes and on slopes
of underwater mountains of volcanic origin on abyssal plains [31, 32]. The model
scheme of such processes is given in Fig. 6.
The most widespread between sediments, which supply the slopes and marine
bottom, are the pelagic oozes with additives of biogenic (biocolloidal) sediments, and
the turbidity deposits that are forming at intensive turbulent wind-wave circulations,
for example, typhoons. At this, the dispersive action of formed sea waves can reach
on the depth of a few kilometers instead of the usual 500–700 m 500–700 m [31].
Pelagic sediments along with turbidities in most cases were accumulated for the
last 18 millions of years in shelf sea zones during the denudation processes, and on
the slopes of underwater hills and mountains (pelitic deposits) [31, 32]. The character