condensate mass is seen to be diminished by a factor of $\sim$100 relative to the Lewis (1969) model.

Increasing $f_{\rm s}$ to 1 results in a hundredfold enhancement of $q_{\rm c}$ throughout the cloud compared to the baseline case, as shown in Figure 2*a*. The principle difference between that extreme and the Lewis (1969) condensate model is that for the former there is no regime near the cloud base akin to shallow terrestrial clouds, in which $q_{\rm c}$ increases with altitude. This difference is attributable to a discontinuity of $q_{\rm t}$ in the treatment of Marley et al.: below the cloud base $q_{\rm t}(z) = q_{\rm v}(z-\Delta z)$ as in the Lewis (1969) model, but above the cloud base $q_{\rm t}(z) = (1+f{\rm s}) \: q_{\rm s}(z)$.

For their calculations of cloud particle sizes, which are decoupled from their calculation of condensate mass, Marley et al. (1999) apply the formalism of Rossow (1978) to two atmospheric endmembers: first, a quiescent atmosphere, in which the mean particle size is determined from the condition that the sedimentation rate matches the faster of coagulation and condensation (at an assumed supersaturation of 0.01); and second, a turbulent atmosphere in which mixing is balanced by 