Initiation of convection
On a warm day, convection begins when the air close to the surface warms enough to become buoyant and start rising. This process is called free convection. The temperature at which free convection begins is called the convective temperature. When the convective temperature is reached on a clear, hot, and humid day, the atmosphere becomes widespread and explosive development of thunderstorms begins. The height at which the rising air condenses moisture is called the convective condensation level (CCL).
Air parcels at the surface buoyantly lift and require no other mechanisms to start lifting. There are other ways of getting air parcels at the surface to begin lifting, even if the air near the surface is stable (below convective temperature). There needs to be another lifting mechanism that pushes the air to a height where it becomes buoyant and begins to rise. The height at which moisture in the rising air condenses is now called the lifted condensation level (LCL)
A typical way of forcing air parcels upwards is along a boundary, such as a cold or warm front. A cold front effectively bulldozes the warm air ahead of it, forcing it upwards. The case is reversed along a warm front: the warmer (less dense) air is forced over the wedge of cold air, which is being slowly pushed forward by the warm air (see figures below). The cold front can be a large (synoptic) scale front of the boundary of cool air flowing out of an already existing thunderstorm (outflow boundary).
The cold front pushes forward like a bulldozer or a wedge, forcing the warm, moist air ahead. This upward motion helps initiate convection.
On a warm front, warm air pushes on the colder air ahead of it. As the warm, moist air is more buoyant than cold air, it is pushed up and over the cold air. The cold air forms a wedge, slowly pushed away by the warm air. More often than not, a warm front produces relatively shallow convection and mostly moderate rain showers. In some cases, thunderstorms also form on the warm front.
Warm air is pushed over the cold air, forming a wedge of cold air between the ground and the warm air aloft. The wedge angle is typically very low, and the warm front produces little or no convection. In some cases, on more robust warm fronts, convection does occur and forms rain showers and, more rarely, thunderstorms.
Interesting fact: in Tornado Alley, thunderstorms on warm fronts are prolific producers of tornadoes
There is a third, much more rare type of front, called a dryline. Along with this type of front, air temperature does not change much, but humidity (air moisture content) changes a lot. Drylines form near mountain ranges and, under the right conditions, also initiate convection.
The convergence of surface winds may also lead to the initiation of convection. The air in the convergence zone is forced upwards. The convergence zone also acts as a frontal boundary if two air masses have significantly different temperatures and humidities.
Additionally, convergence zones are typically areas of strong moisture pooling; increased moisture increases convective instability, lowering the lifted condensation level and, consequently, the level of free convection.
Another way of initiating convection is orographic lift: air moves horizontally over flat terrain but is forced upwards when it encounters higher terrain (hills, mountains).
Another mechanism can assist in initiating convection without a convergence of surface winds or orographic lift. Upper-level forcing happens when winds at high altitudes (5-10 km) diverge, i.e. the airflow fans out. This creates an area of low pressure, which encourages vertical motion, which in turn helps moist, warm air rise before reaching convective temperature.
Recap: When warm, moist air near the ground is heated by the Sun, it may become warm enough to start lifting convectively. The temperature at which this process begins is called convective temperature. If this temperature is not reached, convection will not begin.
Other processes may help the air rise and convection begin, even if the convective temperature is not reached. These processes are known as forcing. Forcing mechanisms include fronts (warm front, cold front), outflow boundaries (small-scale cold fronts produced by individual thunderstorms), surface wind convergences, orographic lift, and upper-level forcing.
In one of the future tutorials, we will go into much more detail about the initiation of convection (storm initiation).
Measures of convective instability
There are many different kinds of measures of convective instability. The most common, and you will come across in virtually an in-depth forecast or storm chaser discussions, is CAPE = Convective Available Potential Energy. Chances are you have heard storm chasers and enthusiasts talk about this: “CAPE this, CAPE that…”. CAPE is fuel for convection – and thunderstorms.
CAPE is the energy a parcel of air has for upward motion. The higher the CAPE, the faster and higher the air parcel can rise. CAPE depends on the temperature and amount of moisture (humidity) in the air near the ground and the vertical temperature gradient. The higher the CAPE, the hotter and more humid the air on the ground. Also, the faster the temperature drops with height, the higher the CAPE.
You will likely come across several variations of CAPE: SBCAPE, MUCAPE, and MLCAPE. In one of the future tutorials, we will cover this and other measures of convective instability in detail.
Fun fact(s): Under the right conditions, the rising air goes up really fast! While most thunderstorms form is moderately unstable conditions (CAPE up to ~1000 J/kg), in some cases, there is much more energy available. This is called extreme instability; in such cases, CAPE values can reach 6000 J/kg or more. When thunderstorms form in this type of environment, the upward speed of rising air is extreme, sometimes over 150 m/s! This is enough to keep hailstones 15+ cm in diameter airborne!