## 4. Physical and numerical parametersThe model nucleus has a uniform temperature of
at the beginning of the simulation so that the
condensed CO remains in solid state as its net sublimation rate at
this temperature is small in a porous matter. The initial composition
has a dust to ice mass ratio of which
corresponds to the lower value evaluated for comet 1P/Halley
(McDonnell et al. 1991). The ice contains condensed CO with a molar
fraction of (free) . An additional amount of
is trapped by the amorphous water ice. The
compact dust density is assumed with . One
single density is chosen for the ice . The
initial total mass density is which is a mean
value of Rickman's density estimation for comet 1P/Halley (Rickman
1986). The porosity is . The material is
supposed to be built by accretion of micrometre-sized aggregates.
Accordingly, we have chosen a characteristic pore size
. The thermal conductivity of compact water ice has been evaluated by Klinger (1980). For crystalline ice he found a dependency by means of laboratory experiments. For amorphous ice Klinger suggested a very low conductivity derived from the classical phonon model for solids. Recently, Kouchi et al. (1992) have measured values several orders of magnitude lower. An explanation of this huge difference might be a weakly connected structure of the condensed sample. Nevertheless, already Klinger's value is so small that the main contribution to the heat transport should come from the gas phase and is not due to heat conduction. In our model we use Klinger's expression as an upper limit of the contribution of the amorphous ice. The conductivity of condensed CO is expected to be small if the molecules are in the amorphous phase. Therefore we use for CO the same conductivity as for amorphous . The bulk conductivity of the dust is adopted from the mean conductivity of terrestrial minerals given by Drury et al. (1984). The specific heat of crystalline water ice has been fitted by Klinger (1980) from measured data given by Giauque & Stout (1936). The same expression is adopted for amorphous ice. For CO we use the upper limit suggested by Tancredi et al. (1994) although small deviation occurs below K: . The specific heat of the dust is supposed to be: This formula fits the specific heat of terrestrial minerals
measured at room temperature (Drury et al. 1984). The specific heat of
water vapour and CO gas is inferred from the ideal gas law
approximation: and .
The latent heat of sublimation of pure is given by Cowan & A'Hearn (1979) from a fit of older data (Washburn 1928). The lower limit of latent heat of sublimation of volatile molecules condensed in a water ice matrix is estimated from the adsorption energy (Schmitt 1991): . The energy balance of the crystallisation process is calculated
using the latent heat of crystallisation of pure amorphous water ice
of (Ghormley 1968). The energy of evaporation
of trapped CO is approximated by its latent heat of sublimation. This
description is consistent with the endothermic process observed during
the crystallisation of water ice being strongly enriched with
(Kouchi 1995). For the chosen parameter the
threshold amount of trapped CO for an endothermic process is
23 % (molar). Other works (Prialnik et al.
1992; Tancredi et al. 1994) consider that the trapped CO behaves as a
gas and the energy reduction during the gas release is therefore much
lower. The sticking (or condensation) coefficient (Eq. 38) for on ice surfaces has been measured by Haynes et al. (1992). is temperature dependent. After fitting the measured data by a linear law we get The saturated vapour pressures are approximated by where , K (Fanale
& Salvail 1984) and ,
K (Fanale & Salvail 1990). More precise
formula of the vapour pressure exist (e.g. Washburn 1928, Kouchi
1987). However, taking into account the uncertainties in the
description of the sublimation process we have chosen Eq. (50) as it
allows more efficient computation. The nucleus surface is supposed to be dark which is the actual
image influenced by the analysis of the optical properties of comet
1P/Halley. It is also consistent with the presence of complex
hydrocarbons suggested by Greenberg (1982). We use an albedo of 0.05
and an infrared emissivity of 0.9. The model nucleus has a spherical shape with a radius of
km (see Meech et al. 1993). The nucleus radius
is discretised by grid points. The first
layers under the surface have a thickness of 0.1 m. The deepest layers
have a thickness of a few hundred metres. Each meridian contains
grid points. The nucleus rotation around its
spin axis is cut into steps leading to a data
matrix with the size of elements per rotation.
To resolve the diurnal heat wave the numerical integration time step has to be sufficiently small. But the smaller the time step the larger the computation time for a given problem size. In order to know how good the diurnal heat wave is resolved we compare a characteristic propagation time with . The characteristic time can be defined as the ratio of the space resolution to the propagation velocity: . The propagation velocity of a diffusion wave is where The integration time step is small compared to the diffusion time
scale. A further necessary condition is on the size of the space
resolution. should be smaller than a
characteristic depth of penetration of the diurnal heat wave. We
consider the damping of a harmonic diffusion wave by a factor For the penetration depth is equal to about m corresponding to 5 layers. One can therefore expect that the diurnal heat wave can be resolved with the chosen time and space resolution. © European Southern Observatory (ESO) 1997 Online publication: July 3, 1998 |