Heating and cooling of the atmosphere

Ozone concentration is controlled by photochemical production, ultraviolet destruction, transport, and mixing. Temperature depends not only on where ozone absorbs radiation, but also on radiative emission, vertical motion, and the surrounding heat balance. Because these controlling processes peak at different heights, the ozone maximum and temperature maximum need not coincide. Thus option C is correct; the other choices contradict basic atmospheric physics.

A dry hot surface uses more energy to raise air temperature directly so sensible heat is high. In exams link dry surfaces with higher sensible heat.

Evaporation uses energy for phase change instead of raising temperature. In exams treat latent heat as a temperature regulator.

A high Bowen ratio indicates dry surfaces and greater sensible heat. In exams remember it as a sign of aridity.

The surface cools first and then cools the adjacent air by conduction. In exams consider night cooling as starting in the surface layer.

Cold dense air remains trapped below and the warmer layer above blocks vertical movement. In exams link inversion with stability.

Cold dense air drains from slopes into valleys and clear nights cool the surface further. In exams link valley frost with cold air drainage.

Urban surfaces heat strongly and create rising warm air. In exams also link urban heat island with convection.

Thick clouds reflect and absorb more solar energy reducing energy reaching the surface. In exams consider daytime clouds as lowering maximum temperature.

Clouds do not allow longwave heat to escape freely so the night cools less. In exams treat clouds as a night heat blanket.

Dust can reduce energy reaching the surface while dry surfaces can heat air rapidly. In exams separate the combined effects.

With little water vapour and cloud terrestrial radiation escapes easily. In exams link deserts with strong radiational cooling.

The sea heats and cools slowly and winds moderate temperature. In exams link coasts with maritime influence.

Land changes temperature quickly while sea changes slowly creating local pressure differences. In exams connect breezes with unequal heating.

Latent heat released during condensation gives extra energy to rising air. In exams understand condensation as a heat-release process.

In instability warm air rises easily and clouds may develop. In exams link instability with convection.

In stability an air parcel tends to return downward after being lifted. In exams link stable layers with weak mixing.

Tall buildings reduce sky view and heat is repeatedly reflected. In exams link urban canyons with heat trapping.

Low water vapour traps less longwave energy so night cooling is stronger. In exams link dry clear nights with lower minimum temperature.

After sunrise the surface warms and mixes the cold lower layer. In exams remember inversion breakup through morning heating.

Even after solar altitude begins to fall incoming energy can exceed outgoing energy for some time. In exams link maximum temperature with energy-balance lag.

Until sunrise the surface keeps losing energy and enough solar input has not begun. In exams link minimum temperature with overnight heat loss.

Strong horizontal motion can change temperature quickly by bringing a new air mass. In exams link advection with air-mass arrival.

Horizontal arrival of cold air can bring near-surface temperature close to freezing. In exams link cold advection with temperature fall.

Snow reflects strongly so the surface warms less and gives less heat to air. In exams remember snow by high albedo.