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There's nothing like a severestorm to bring people together. Watching the hail and laughing hysterically with strangers.

This is the worst storm I've ever seen here in the fraservalley. Probably the scariest commute home through mapleridge too. Be safe out there.

Look at this hail in downtown Maple Ridge right now. Please read our Commenting Policy first. How does a thunderstorm form?

Three basic ingredients are required for a thunderstorm to form: As the air rises, it transfers heat from the surface of the earth to the upper levels of the atmosphere the process of convection.

The water vapor it contains begins to cool, releases the heat, condenses and forms a cloud. The cloud eventually grows upward into areas where the temperature is below freezing.

As a storm rises into freezing air, different types of ice particles can be created from freezing liquid drops. The ice particles can grow by condensing vapor like frost and by collecting smaller liquid drops that haven't frozen yet a state called "supercooled".

When two ice particles collide, they usually bounce off each other, but one particle can rip off a little bit of ice from the other one and grab some electric charge.

Lots of these collisions build up big regions of electric charges to cause a bolt of lightning, which creates the sound waves we hear as thunder.

The Thunderstorm Life Cycle Thunderstorms have three stages in their life cycle: The developing stage, the mature stage, and the dissipating stage.

The developing stage of a thunderstorm is marked by a cumulus cloud that is being pushed upward by a rising column of air updraft.

The cumulus cloud soon looks like a tower called towering cumulus as the updraft continues to develop. There is little to no rain during this stage but occasional lightning.

The thunderstorm enters the mature stage when the updraft continues to feed the storm, but precipitation begins to fall out of the storm, creating a downdraft a column of air pushing downward.

When the downdraft and rain-cooled air spreads out along the ground it forms a gust front, or a line of gusty winds.

In its later stages, the downdraft spreads throughout the cell and diminishes in intensity as precipitation falls from the cloud. Isolated thunderstorms contain one or more convective cells in different stages of evolution.

Frequently, the downdrafts and associated outflows from a storm trigger new convective cells nearby, resulting in the formation of a multiple-cell thunderstorm.

Solar heating is an important factor in triggering local, isolated thunderstorms. Most such storms occur in the late afternoon and early evening, when surface temperatures are highest.

Violent weather at the ground is usually produced by organized multiple-cell storms, squall lines , or a supercell. All of these tend to be associated with a mesoscale disturbance a weather system of intermediate size, that is, 10 to 1, km [6 to miles] in horizontal extent.

Multiple-cell storms have several updrafts and downdrafts in close proximity to one another. They occur in clusters of cells in various stages of development moving together as a group.

Within the cluster one cell dominates for a time before weakening, and then another cell repeats the cycle. Supercell storms have one intense updraft and downdraft; they are discussed in more detail below.

Sometimes the development of a mesoscale weather disturbance causes thunderstorms to develop over a region hundreds of kilometres in diameter.

Examples of such disturbances include frontal wave cyclones low-pressure systems that develop from a wave on a front separating warm and cool air masses and low-pressure troughs at upper levels of the atmosphere.

The resulting pattern of storms is called a mesoscale convective system MCS. Severe multiple-cell thunderstorms and supercell storms are frequently associated with MCSs.

Precipitation produced by these systems typically includes rainfall from convective clouds and from stratiform clouds cloud layers with a large horizontal extent.

Stratiform precipitation is primarily due to the remnants of older cells with a relatively low vertical velocity—that is, with limited convection occurring.

Thunderstorms can be triggered by a cold front that moves into moist, unstable air. Sometimes squall lines develop in the warm air mass tens to hundreds of kilometres ahead of a cold front.

The tendency of prefrontal storms to be more or less aligned parallel to the front indicates that they are initiated by atmospheric disturbances caused by the front.

In the central United States, severe thunderstorms commonly occur in the springtime, when cool westerly winds at middle levels 3, to 10, metres [10, to 33, feet] in altitude move over warm and moist surface air flowing northward from the Gulf of Mexico.

The resulting broad region of instability produces MCSs that persist for many hours or even days.

In the tropics, the northeast trade winds meet the southeast trades near the Equator , and the resulting intertropical convergence zone ITCZ is characterized by air that is both moist and unstable.

Thunderstorms and MCSs appear in great abundance in the ITCZ; they play an important role in the transport of heat to upper levels of the atmosphere and to higher latitudes.

When environmental winds are favourable, the updraft and downdraft of a storm become organized and twist around and reinforce each other.

The result is a long-lived supercell storm. These storms are the most intense type of thunderstorm. In the central United States, supercells typically have a broad, intense updraft that enters from the southeast and brings moist surface air into the storm.

The updraft rises, rotates counterclockwise, and exits to the east, forming an anvil. Updraft speeds in supercell storms can exceed 40 metres feet per second and are capable of suspending hailstones as large as grapefruit.

Supercells can last two to six hours. They are the most likely storm to produce spectacular wind and hail damage as well as powerful tornadoes.

Aircraft and radar measurements show that a single thunderstorm cell extends to an altitude of 8, to 10, metres 26, to 33, feet and lasts about 30 minutes.

An isolated storm usually contains several cells in different stages of evolution and lasts about an hour.

A large storm can be many tens of kilometres in diameter with a top that extends to altitudes above 18 km 10 miles , and its duration can be many hours.

The updrafts and downdrafts in isolated thunderstorms are typically between about 0. The updraft diameter may occasionally exceed 4 km 2. Closer to the ground, drafts tend to have a larger diameter and lower speeds than do drafts higher in the cloud.

Updraft speeds typically peak in the range of 5 to 10 metres 16 to 33 feet per second, and speeds exceeding 20 metres 66 feet per second are common in the upper parts of large storms.

Airplanes flying through large storms at altitudes of about 10, metres 33, feet have measured updrafts exceeding 30 metres 98 feet per second.

The strongest updrafts occur in organized storms that are many tens of kilometres in diameter, and lines or zones of such storms can extend for hundreds of kilometres.

Sometimes thunderstorms will produce intense downdrafts that create damaging winds on the ground. These downdrafts are referred to as macrobursts or microbursts , depending on their size.

A macroburst is more than 4 km 2. A microburst is smaller in dimension but produces winds as high as 75 metres per second, or km per hour feet per second, or miles per hour on the ground.

When the parent storm forms in a wet, humid environment, the microburst will be accompanied by intense rainfall at the ground.

If the storm forms in a dry environment, however, the precipitation may evaporate before it reaches the ground such precipitation is referred to as virga , and the microburst will be dry.

Downbursts are a serious hazard to aircraft, especially during takeoffs and landings, because they produce large and abrupt changes in the wind speed and direction near the ground.

In general, an active cloud will rise until it loses its buoyancy. A loss of buoyancy is caused by precipitation loading when the water content of the cloud becomes heavy enough, or by the entrainment of cool, dry air, or by a combination of these processes.

Growth can also be stopped by a capping inversion, that is, a region of the atmosphere where the air temperature decreases slowly, is constant, or increases with height.

Thunderstorms typically reach altitudes above 10, metres 33, feet and sometimes more than 20, metres 66, feet.

When the instability is high, the atmosphere moist, and winds favourable, thunderstorms can extend to the tropopause, that is, the boundary between the troposphere and the stratosphere.

The tropopause is characterized by air temperatures that are nearly constant or increasing with height, and it is a region of great stability. Occasionally the momentum of an updraft carries it into the stratosphere, but after a short distance the air in the top of the updraft becomes cooler and heavier than the surrounding air, and the overshoot ceases.

The height of the tropopause varies with both latitude and season. It ranges from about 10, to 15, metres 33, to 50, feet and is higher near the Equator.

When a cumulonimbus cloud reaches a capping inversion or the tropopause, it spreads outward and forms the anvil cloud so characteristic of most thunderstorms.

The winds at anvil altitudes typically carry cloud material downwind, and sometimes there are weak cells of convection embedded in the anvil.

An airplane flying through a thunderstorm is commonly buffeted upward and downward and from side to side by turbulent drafts in a storm.

Atmospheric turbulence causes discomfort for the crew and passengers and also subjects the aircraft to undesirable stresses.



Thunderstorm Video

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