= Solution
Clouds reflect shortwave sunlight, usually cooling the planet, and absorb and emit thermal infrared radiation, usually warming the surface relative to clear sky. Their net effect depends on altitude, temperature, optical depth, phase and the underlying surface: thick low clouds often have strong shortwave cooling, while cold high clouds can have a comparatively strong longwave warming effect. Surface and top-of-atmosphere budgets must be distinguished; absorbing radiation within a cloud can heat the atmospheric layer while shading the ground.
Condensation and freezing release <latent heat>; evaporation and melting absorb it. These processes change buoyancy, stability and convective transport. Entrainment of dry air can evaporate droplets and cool the cloud edge, while precipitation removes condensate and water.
Microphysics controls the radiative properties. For liquid droplets with a fixed <liquid-water path> W, the <cloud optical depth at fixed liquid-water path> is approximately
$$
\boxed{\tau_{\rm cld}\simeq\frac{3W}{2\rho_w r_{\rm eff}}.}
$$
Thus more numerous smaller droplets at fixed W give a brighter, optically thicker cloud: the <Twomey effect>. Ice habit, phase and particle-size distribution also alter scattering, absorption and precipitation. Cloud-water and lifetime adjustments need not preserve W, so a microphysical perturbation has no universal net radiative sign. <The Earth's Energy Budget, Climate Feedbacks, and Climate Sensitivity by Piers Forster and others>[§7.3.3, aerosol–cloud interactions, liquid-water and cloud adjustments]{ref}
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