The atmosphere and the weather

Conditions for Cloud Formation

Most clouds form as air rises, expands and cools. But why does the air rise on some occasions and not on others? And why does the size and shape of clouds vary so much when the air does rise? The answer to the latter question is related to the concept of atmospheric stability, which we will discuss in later lectures. We will now discuss some of the mechanisms responsible for getting air to rise in the first place.

Four ways to get air to rise

Surface heating and free convection
Horizontal Convergence of surface air and/or Horizontal Divergence of air near the top of the troposphere
Topography (mountains)
Uplift along weather fronts

1. Surface heating and free convection

[convection] During the daytime, the earth's surface is heated by the sun, which in turn heats the air in contact with the surface. Parcels (or bubbles) of hot air (called thermals) rise upward. As they rise upward, the thermals cool by expansion. These warmed parcels continue to rise as long as they remain warmer than the surrounding environment. Early in the day (morning), the parcels don't rise very high because they quickly become colder than the surrounding air. As the day goes on, a deeper and deeper layer of air near the ground warms up. Parcels get hotter as the ground temperature increases and are able to rise higher and higher. If a thermal is able to rise high enough to cool to its saturation point, then some of the water vapor within the rising parcel condenses and becomes visible as a cloud.

On summer days, the sky is often clear during the morning. But as the day goes on, parcels are able to rise higher and higher, resulting in clouds by the afternoon. When the atmosphere is unstable, thunderstorms may develop in the late afternoon if the parcels are able to rise high enough to reach an unstable region of the atmosphere.

2. Surface Convergence and/or Upper-level Divergence

[convergence] Convergence is an atmospheric condition that exists when there is a horizontal net inflow of air into a region. When air converges along the earth's surface, it is forced to rise since it cannot go downward. Large scale convergence can lift a layer of air hundreds of kilometers across. Surface low pressure regions (marked by L's on surface weather maps), are areas where surface convergence takes place.

Divergence is an atmospheric condition that exists when there is a horizontal net outflow of air from a region. When air diverges just below the top of the troposphere, air from below is forced to rise up and take its place. You can think of the tropopause as a "lid" or boundary that does not allow air to move up or down through it. Weather reporters often use the terms "upper-level disturbance" or "upper-level energy" to indicate regions where the rising air motion is forced by the atmospheric conditions 5-10 km above the Earth's surface. As we will cover later in the semester, upper level divergence is forced in regions just downstream of upper-level troughs, e.g., just downstream of 500 mb troughs. We will discuss this in more detail later in the semester. A conceptual figure for this situation will be drawn in class.

3. Lifting Due To Topography

[orographic lifting] When air is confronted by a mountain, it is lifted up and over the mountain, cooling as it rises. If the air cools to its saturation point, the water vapor condenses and a cloud forms. Heating of the mountain slopes by the Sun also causes air to rise upward. These types of clouds are called "orographic clouds", which develop in response to lifting forced by the topography of the earth.

While air on the windward side of a mountain is forced to rise, often resulting in clouds and precipitation, the air on the leeward side of a mountain is forced to sink. Thus on the leeward side of a mountain, we often see clear skies and warm, dry conditions. The leeward side of a mountain range is often called a "rain shadow" region because clouds and precipitation do not form where air is sinking. The great basin area of the United States is a rain shadow region.

4. Lifting Along Frontal Boundaries

[front]

A front is defined as the transition zone between two air masses of different density. The warmer air mass is less dense than the colder air mass. Fronts extend not only in the horizontal direction, but in the vertical as well. Therefore, when referring to the frontal surface (or frontal zone), we referring to both the horizontal and vertical components of the front. All fronts slope in the vertical so that the warmer (less dense) air mass sits on top of the colder (more dense) air mass. In other words, the warmer air mass is forced to rise over the colder air mass. As air from the warm air mass rises, it cools, leading to the development of clouds and maybe precipitation.

Large areas of clouds and precipitation are common near weather fronts. If the atmosphere is stable, a large area of clouds and steady precipitation is common. But if the atmosphere is unstable, numerous thunderstorms (sometimes severe) are often observed near weather fronts. We will discuss the concept of atmospheric stability soon.