Because warm air can hold more moisture, the near-surface air becomes warm and moist, but is generally unsaturated (RH less than 100%) The air warmer than it’s surroundings, becomes buoyant and begins to rise. To study this ascent, meteorologists often represent the rising air as an idealized air parcel. The parcel experiences a buoyancy force, B ∝ Tparcel − Tenv so that when Tparcel > Tenv Tparcel>Tenv,​, the buoyancy is positive and the parcel rises. As the parcel rises, pressure decreases with height, causing it to expand and cool adiabatically. Initially, the parcel remains unsaturated, but continued cooling increases its relative humidity. Once the relative humidity reaches 100%, the parcel reaches the Lifting Condensation Level (LCL), where condensation begins, cloud droplets form, and latent heat is released.
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As the rising air cools, its relative humidity increases until it reaches 100%, where condensation begins and the air reaches the Lifting Condensation Level (LCL). Cloud droplets form, and latent heat is released, reducing the rate of cooling. The rising air now follows the Moist Adiabatic Lapse Rate (MALR) instead of the Dry Adiabatic Lapse Rate (DALR). Because the MALR is generally smaller than the Environmental Lapse Rate (ELR), the rising air cools more slowly than its surroundings. Eventually it becomes warmer and less dense than the surrounding atmosphere, producing positive buoyancy: : B = Tparcel − Tenv > 0 The altitude at which this first occurs is called the Level of Free Convection (LFC). Above the LFC, buoyancy alone is sufficient to accelerate the rising air upward without additional external lifting, leading to deep convection.

Above the Level of Free Convection (LFC), positive buoyancy accelerates the rising air, producing strong convective updrafts. These updrafts transport warm, moist air upward, where continued cooling leads to further condensation and vertical cloud growth. As more water vapour condenses, latent heat is released, strengthening the buoyancy and intensifying the updraft. During the cumulus stage, the cloud is dominated by these rising air currents and continues to develop vertically, while precipitation is generally absent or weak because the cloud droplets have not yet grown large enough to fall.

During the mature stage, the cloud reaches its maximum vertical extent and precipitation begins to fall. Strong updrafts continue to transport heat and moisture upward, while falling rain produces downdrafts through evaporative cooling and drag. As a result, both updrafts and downdrafts coexist within the storm, producing the heaviest rainfall and the most intense convective activity.
The rising air eventually reaches the Equilibrium Level (EL), where it is no longer buoyant. It then spreads horizontally near the top of the cloud, forming the characteristic anvil cloud. Within the cloud, condensed droplets continue to grow through microphysical processes until they become large enough to fall as precipitation. In deep convective storms, the EL is often located near the tropopause (10–15 km).

During the dissipating stage, downdrafts become stronger and cut off the supply of warm, moist air feeding the storm. Without a sustained updraft, the cloud loses its source of energy and gradually weakens. Rainfall decreases, leaving only light rain and weak outflow winds for a short time. Eventually, the storm dissipates, often leaving behind a remnant anvil cloud and cooler, more stable air near the surface.