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Dynamic/Thermodynamic Simulations of the North Polar Ice Cap of Mars 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 r =r H =4:26 init 0 km, 6.38 km and 8.51 km, respectively. The H = H e 1 0 accumulation rate is varied such that the initial ice volume is reproduced in the steady state as accurately as possible. is used, where r is the distance from the position of maximum H 87 0 r = 0 ice thickness, 0 ,assumedtobeat N, W, and No. V H S t V H init init ss ss ss 400 km. Based on the horizontal extent and observed surface 1 2.00 4.26 0.04 35 2.01 3.27 H undulations of the ice cap, Budd et al. (1986) argue that 0 3.00 6.38 0.4 4 3.00 4.67 should be about 4 km. From the digitized surface topography 2 3 4.00 8.51 3.0 1 3.97 6.42 and eq. (1), an estimated digitized bedrock topography, b, = h H follows via b . Further, application of a local isostatic able 1: Results of steady-state simulations no. 1-3 with balance between ice load and lithosphere buoyancy yields the T 6 3 varied ice volume. V , V in 10 km , H , H in init ss init ss b relaxed bedrock topography with no ice load, 0 ,as km, S in mm WE/yr, t in Myr quantities are ex- ss plained in the main text. b = b + H; 2 0 a V H S init Table 1 lists init , , , the time required to reach 3 t ss where is the ice density (910 kg/m )and a the mantle the steady state, , and the ice volume and the maximum 3 3 V H ss density, taken as 2350 kg/m (terrestrial value 3300 kg/m ice thickness in the steady state, ss and , for the three First International Conference on Mars Polar Science 3001.pdf SIMULATIONS OF THE NORTH POLAR ICE CAP OF MARS: R. Greve simulations with optimum accumulation rate to reproduce the Press Conference, Spring Meeting of the American Geophys- initial volume (referred to as simulations no. 1, 2, 3, respect- ical Union, Boston, 1998), much like the flowing ice sheets on ively). Evidently, the accumulation rate required to maintain Earth. the initial volume varies by two orders of magnitude for the It is further noticeable that for none of the three simulations three simulations, and it is within the above estimated range the basal temperature reaches the pressure melting point. Fig. 1 of 0.1. 1 mm WE/yr for simulation no. 2, which is therefore depicts the basal temperature (relative to pressure melting) for 29:3 regarded as the most realistic reference simulation. Accord- the reference simulation no. 2, the maximum of C t ingly, ss (which is also a measure for the time necessary to being reached at 85.3 N, 30.3 W. For simulation no. 1, the 46:9 build up the ice cap from ice-free initial conditions) varies by maximum basal temperature is C, for simulation no. 3 4:4 two orders of magnitude, and it is in any case much larger than it is C, already very close to pressure melting. for ice sheets on Earth [ 100 kyr for Greenland, see Greve These results are strongly dependent on the applied areo- (1997b)]. thermal heat flux, which is not very well known. In order to V V ss Even though init and agree very well for the three investigate under which circumstances pressure melting can H simulations, the corresponding maximum thicknesses init be reached at the ice base, the reference simulation no. 2 was H and ss differ by about 25%. The reason for this is that re-run with larger areothermal heat fluxes, namely 40, 50, the ice flow tends to redistribute the initial (measured) surface 60and70mW/m2 . As a consequence, the maximum basal 22:4 12:9 4:6 0 topography with steeper gradients in the interiour and flatter temperatures rise to C, C, Cand C, re- slopes towards the margin to a more parabolic shape with the spectively. Hence, for 70 mW/m2 pressure melting is reached opposite behaviour. A reason for this shortcoming may be the at the ice base, with an area at pressure melting of 4784 km2 tentative use of the terrestrial degree-day parameterization for or 0.34% of the simulated total ice-covered area, and a basal 3 5 :3 10 surface melting/evaporation, which is not likely to describe the melting rate of 3 m WE/yr. surface processes adequately under the very different Martian conditions. References Budd, W. F., D. Jenssen, J. H. I. Leach, I. N. Smith and U. Radok. 1986. The north polar ice cap of Mars as a steady-state system. Polarforschung, 56 (1/2), 43-46. Calov, R., A. Savvin, R. Greve, I. Hansen and K. Hutter. 1998. Simulation of the Antarctic ice sheet with a three- dimensional polythermal ice sheet model, in support of nn. Glaciol. the EPICA project. A , 27 (in press). Dzurisin, D. and K. R. Blasius. 1975. Topography of the polar ophys. Res. layered deposits of Mars. J. Ge , 80 (23), 3286-3306. Greve, R. 1997a. A continuum-mechanical formulation for rans. R. Soc. shallow polythermal ice sheets. Phil. T ond., Ser. A L , 355, 921-974. Greve, R. 1997b. Application of a polythermal three-dimen- sional ice sheet model to the Greenland Ice Sheet: Re- sponse to steady-state and transient climate scenarios.
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