vertical eddy diffusion coefficient and $f_{\rm rain}$ is a new parameter that we have introduced, defined as the ratio of the mass-weighted droplet sedimentation velocity to $w_*$, the convective velocity scale. We solve Equation \[K\_pde\] for each condensate independently, and hence ignore any microphysical interactions between clouds. Equation \[K\_pde\] is an extension of Lunine et al.’s convective cloud model, relaxing their implicit assumptions $f_{\rm rain}$ = 1 and $q_{\rm c} = q_{\rm t}$.

The product $f_{\rm rain} w_*$ represents an average sedimentation velocity for the condensate, which offsets turbulent mixing and thereby leads to $q_{\rm t}$ decreasing with altitude. The extreme case with no sedimentation to offset turbulent mixing ($f_{\rm rain}$ = 0) is equivalent the frozen-in endmember of Lunine et al. (1989) and the “dusty” models of the Lyon group (e.g., Chabrier et al. 2000). In this case the solution to Equation \[K\_pde\] is a well-mixed atmosphere ($q_{\rm t}$ independent of altitude), which is seen in Figure 1 to loft even more condensate than the convective cloud of Lunine et al. (1989).

We adopt $f_{\rm rain}$ as an adjustable input parameter, which together with $q_{\rm c}$ constrains the droplet size distributions. First we describe our calculation of $q_{\rm c}$, 