ice model driven by a prescribed atmospheric high-pressure system. They determined that the quasi-steady-state response of ice disk with a diameter of 1000 km is
established within 6 h of the initial air stress application, regardless of the initial
conditions.
Formation of the zones with “solid body” motion is a common property of the
elastic-plastic solutions. In plasticity theory, the motion of a continuum is performed as a combination of motions of solid blocks separated by shear plastic zones
or slip lines (e.g., [10]). Korsnes [4] considered elements of rigid motion of ice floes
using the ERS-1 SAR data. Sharp discontinuities separating the regions of uniform
ice motion in the Arctic drift sea ice were investigated by Kwok [5]. The analysis
was performed using the high-resolution deformation fields of the Arctic ice cover
produced by RADARSAT Geophysical Processor System. Goldstein et al. [3] used
RADARSAT images to record solid body motion of ice bands in Bay of Bothnia.
Marchenko [8] investigated analytically steady-state drift of elastic-plastic ice
forced by the drag of sea current unlimited in the longitudinal direction and
localized in the transversal direction. It was shows that the solution consists of the
elastic kernel moving with constant velocity in the direction of the sea current and
plastic boundary zones located at different sides of the elastic kernel. Ice velocity
inside the plastic zones is parallel to the sea current, it equals to the velocity of the
elastic kernel along the contact lines and tends to zero at the periphery of the plastic
zones. Circular drift of elastic-plastic ice caused by the drag force of wind vortex
was investigated by Marchenko [9] analytically. Circular wind vortex is approximated by the polynomial function of the polar radius. It was shown that the drag
force from cyclonic or anticyclonic wind vortex influences circular drift of ice
consisting of the solid body rotation of the elastic kernel and plastic shear zone in
the form of a ring surrounding the elastic kernel. Outside the plastic ring, the ice is
not moving. Solutions with the elastic kernel and plastic ring exist when the
maximum wind speed is greater than the critical speed. If the wind speed is below
the critical value the ice stresses are in the elastic range. It was found that the width
of the plastic ring decreases as the maximum wind speed becomes close to the
critical value.
The main goal of this contribution consists in the further analysis of the analytical solutions of sea ice dynamics model based on AIDJEX elastic-plastic rheology taking into account sea surface tilt and wind velocity component transversal
to ice drift direction. In the second section, we consider examples of ice drift
features appearing under the influence of wind on the ice near shore line of linear
shape, and under the influence of cyclonic wind on the ice. In the third section, the
model equations are formulated. In the fourth section, the characteristics of plastic
shear zones in drift ice are investigated in the plane and axially symmetric cases. In
the fifth section, zonal wind drift of ice cover near rectilinear shoreline is investigated. In the sixth section, circular wind drift of ice cover is investigated. The main
results of the paper are discussed and conclusions are formulated in the last section.
540
A. Marchenko
established within 6 h of the initial air stress application, regardless of the initial
conditions.
Formation of the zones with “solid body” motion is a common property of the
elastic-plastic solutions. In plasticity theory, the motion of a continuum is performed as a combination of motions of solid blocks separated by shear plastic zones
or slip lines (e.g., [10]). Korsnes [4] considered elements of rigid motion of ice floes
using the ERS-1 SAR data. Sharp discontinuities separating the regions of uniform
ice motion in the Arctic drift sea ice were investigated by Kwok [5]. The analysis
was performed using the high-resolution deformation fields of the Arctic ice cover
produced by RADARSAT Geophysical Processor System. Goldstein et al. [3] used
RADARSAT images to record solid body motion of ice bands in Bay of Bothnia.
Marchenko [8] investigated analytically steady-state drift of elastic-plastic ice
forced by the drag of sea current unlimited in the longitudinal direction and
localized in the transversal direction. It was shows that the solution consists of the
elastic kernel moving with constant velocity in the direction of the sea current and
plastic boundary zones located at different sides of the elastic kernel. Ice velocity
inside the plastic zones is parallel to the sea current, it equals to the velocity of the
elastic kernel along the contact lines and tends to zero at the periphery of the plastic
zones. Circular drift of elastic-plastic ice caused by the drag force of wind vortex
was investigated by Marchenko [9] analytically. Circular wind vortex is approximated by the polynomial function of the polar radius. It was shown that the drag
force from cyclonic or anticyclonic wind vortex influences circular drift of ice
consisting of the solid body rotation of the elastic kernel and plastic shear zone in
the form of a ring surrounding the elastic kernel. Outside the plastic ring, the ice is
not moving. Solutions with the elastic kernel and plastic ring exist when the
maximum wind speed is greater than the critical speed. If the wind speed is below
the critical value the ice stresses are in the elastic range. It was found that the width
of the plastic ring decreases as the maximum wind speed becomes close to the
critical value.
The main goal of this contribution consists in the further analysis of the analytical solutions of sea ice dynamics model based on AIDJEX elastic-plastic rheology taking into account sea surface tilt and wind velocity component transversal
to ice drift direction. In the second section, we consider examples of ice drift
features appearing under the influence of wind on the ice near shore line of linear
shape, and under the influence of cyclonic wind on the ice. In the third section, the
model equations are formulated. In the fourth section, the characteristics of plastic
shear zones in drift ice are investigated in the plane and axially symmetric cases. In
the fifth section, zonal wind drift of ice cover near rectilinear shoreline is investigated. In the sixth section, circular wind drift of ice cover is investigated. The main
results of the paper are discussed and conclusions are formulated in the last section.
540
A. Marchenko