什么是 Saturated adiabatic lapse rate; moist adiabat？

Example 21.20 (The energy in the Norman sounding)

Lift the surface air of Example 21.4. It saturates at $964\,\mathrm{hPa}$, $64\,\mathrm{m}$ up, and follows a moist adiabat. Below $900\,\mathrm{hPa}$ the sounding is itself nearly saturated and the parcel stays a few tenths of a degree colder than its surroundings; then comes the inversion between $908\,\mathrm{hPa}$ and $889\,\mathrm{hPa}$, where the temperature rises by $4.1\,\mathrm{K}$ in $178\,\mathrm{m}$ and the parcel finds itself $5\,\mathrm{K}$ too cold. It becomes warmer than its surroundings only at $732\,\mathrm{hPa}$, $2.4\,\mathrm{km}$ above the ground, its LFC, and stays warmer up to its EL at $236\,\mathrm{hPa}$, $10.9\,\mathrm{km}$ above sea level, just below the tropopause the sounding reports at $235\,\mathrm{hPa}$. On a fine grid of pressures the areas of the skew-T figure are CAPE $= 2100\,\mathrm{J}/\mathrm{kg}$ and CIN $= -200\,\mathrm{J}/\mathrm{kg}$ with the temperature, and $2230\,\mathrm{J}/\mathrm{kg}$ and $-130\,\mathrm{J}/\mathrm{kg}$ with the virtual temperature: the moisture of the parcel adds its own buoyancy. Parcel theory gives $w_{\max} = \sqrt{2 \times 2100} = 65\,\mathrm{m}/\mathrm{s}$.