First International Conference on Mars Polar Science 3001.pdf
DYNAMIC/THERMODYNAMIC SIMULATIONS OF THE NORTH POLAR ICE CAP OF MARS. R. Greve, Institut fur¨ Mechanik III, Technische Universitat¨ Darmstadt, D-64289 Darmstadt, Germany, [email protected].
Ice-sheet model SICOPOLIS times mean-density ratio Mars/Earth). The bedrock response
to changing ice loads is modelled by a delayed local isostatic = 3000 The present permanent north polar water ice cap of Mars is in- balance with the time lag V yr. vestigated with the dynamic/thermodynamic ice-sheet model According to the data listed by Budd et al. (1986), the mean
SICOPOLIS (SImulation COde for POLythermal Ice Sheets), T
annual air temperature above the ice, ma , is described by a
~ h
which was originally developped for and applied to terrestrial parameterization depending on elevation, , and co-latitude,
~
=90 ice sheets like Greenland, Antarctica and the glacial northern ( N ,where is the latitude),
hemisphere (Greve, 1997b, c; Calov et al., 1998; Greve et al.,
0
~
T = T + h + c ; 3
ma ma ma 1998). The model is based on the continuum-mechanical the- ma
ory of polythermal ice masses (Hutter, 1982, 1993; Greve,
0
T = 90 = 2:5 ma
1997a), which describes the material ice as a density-preser- with ma C, the mean lapse rate C/km,
c = 1:5 ving, heat-conducting power-law fluid with thermo-mechani- and ma C/ lat. The accumulation of water ice on cal coupling due to the strong temperature dependence of the the surface of the ice cap is assumed to be spatially con-
stant. Since the water vapour density in the Martian atmo-
old ice ice viscosity. It is further distinguished between c with
sphere is approximately 1/1000th the terrestrial value, and
erate a temperature below the pressure melting point and temp
typical accumulation rates for terrestrial ice sheets are about e ic with a temperature at the pressure melting point, the latter being considered as a binary mixture of ice and small amounts 300 mm WE/yr (Greenland), the order of magnitude of the of water. The influence of the considerable dust content of the accumulation rate, S ,canbeestimatedas0.1...1mmWE/yr. ice cap on the mechanical properties of the ice is neglected. Surface melting/evaporation is parameterized by the standard
The model computes three-dimensionally the temporal degree-day method with terrestrial (Greenland) values for the
=3
evolution of ice extent, thickness, temperature, water content snow- and ice-melt factors, snow mm WE/(d C) and
=12
and age as a response to external forcing. The latter must be ice mm WE/(d C), an amplitude of the annual tem-
specified by (i) the mean annual air temperature above the ice, perature signal of 30 C and a standard deviation of additional (ii) the surface mass balance (ice accumulation minus melting temperature variations of 10 C. Further, the simulated ice cap
and evaporation), (iii) the global sea level (not relevant for is restricted to its present extent, and the areothermal heat flux 2 Martian applications) and (iv) the geothermal (areothermal) is set to 33.5 mW/m (Budd et al., 1986). heat flux from below into the ice body. Results Simulation set-up A series of simulations were carried out, where the meas- ured/estimated topography described above is used as initial
The surface topography, h, of the permanent north polar water ice cap of Mars used here is based on the map constructed by condition, and the time-forward integration is conducted until Dzurisin and Blasius (1975), which was slightly filtered and the simulated ice cap is in steady state with the present climate digitized to a 40-km grid for this study, and complemented by forcing defined by the air temperature, the surface mass bal-
the ice margin contour given by Budd et al. (1986). As for the ance and the areothermal heat flux. For the initial ice volume,
6 3 6 3 6 3
V 2 10 3 10 4 10
init , the three values km , km and km
ice thickness, H , a Gaussian distribution
are used, corresponding to maximum initial ice thicknesses of
2 2