two endmembers of their cloud spectrum, corresponding to dust-like and frozen-in clouds.

Their intermediate case serves as a starting point for our model of condensate mass profiles. Our interpretation of the convective cloud model of Lunine et al. (1989) as applied to the Jovian ammonia cloud is shown in Figure 1. Note that we have refined that model slightly, allowing the atmospheric properties to vary with height above the cloud base, and relaxing their assumption that $q_{\rm c}$ = $q_{\rm t}$. The condensate mass is seen to be significantly enhanced above the cloud base for that model: at the tropopause (where there is no cold-trap in this case) $q_{\rm c}$ is enhanced a thousand-fold over that computed by the Lewis (1969) model. Thus the treatment in which Lunine et al. (1989) assume particle sedimentation to balance turbulent transport results in a cloud not so different from their frozen-in case (as depicted by the curve in Figure 1 labeled $f_{\rm rain} = 0$). Evidently the sedimentation in this convective cloud model is far less effective than that assumed by Lewis (1969). As described below, for our calculations of condensate mass profiles we extend the Lunine et al. (1989) approach by applying 