Also called a "pulse" thunderstorm, the ordinary cell consists of a one-time updraft and one-time downdraft. In the towering cumulus stage, the rising updraft will suspend growing raindrops until the point where the weight of the water is greater than what can be supported.
At this point, drag between the air and the falling drops begins to diminish the updraft, which allows more raindrops to fall. In effect, the falling rain turns the updraft into a downdraft. With rain falling back into the updraft, the supply of rising moist air is cut-off, and the life of the single cell thunderstorm is short.
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While hail and gusty wind can develop, these occurrences are typically not severe. However, if atmospheric conditions are right and the ordinary cell is strong enough, more than one cell can potentially form and can include microburst winds (usually less than 70 mph/112 km/h) and weak tornadoes.
A thunderstorm may consist of just one ordinary cell that transitions through its life cycle and dissipates without additional new cell formation, but they often form in clusters, with numerous cells in various stages of development merging together.
While each individual thunderstorm cell in a multi-cell cluster behaves as a single cell, the prevailing atmospheric conditions are such that as the first cell matures, it is carried downstream by the upper level winds, with a new cell forming upwind of the previous cell to take its place.
The speed at which the entire cluster of thunderstorms move downstream can make a huge difference in the amount of rain any one place receives. Frequently, as an individual cell moves downstream, additional cells form on the upwind side of the cluster and move directly over the path of the previous cell.
Updrafts, and therefore new cells, continually re-form at the leading edge of the system, with rain and hail following behind. Individual thunderstorm updrafts and downdrafts along the line can become quite strong, resulting in episodes of large hail and strong outflow winds that move rapidly ahead of the system.
While the leading edge of squall lines occasionally form tornadoes, they primarily produce "straight-line" wind damage, a result of the force of the downdraft spreading horizontally as it reaches the Earth's surface.
Often along the leading edge of the squall line is a low hanging arc of cloudiness called the shelf cloud. This results from rain-cooled air spreading out from underneath the squall line like a mini cold front. The cooler, dense air forces the warmer, less dense air up. The rapidly rising air cools and condenses, creating the shelf cloud.
Supercell thunderstorms are a special kind of single cell thunderstorm that can persist for many hours. They are responsible for nearly all of the significant tornadoes produced in the U.S. and for most of the hailstones larger than golf ball size. Supercells are also known to produce extreme winds and flash flooding.
Supercells are highly organized storms characterized by updrafts that can attain speeds of over 100 mph (160 km/h) and are able to produce giant hail with strong or even violent tornadoes. Downdrafts produced by these storms can produce downbursts/outflow winds in excess of 100 mph (160 km/h), posing a high threat to life and property.
The most ideal conditions for supercells to occur are when the winds are veering, or turning clockwise, with height. For example, in a veering wind situation, the winds may be from the south at the surface and from the west at 15,000 feet (4,500 meters). This change in wind speed and direction produces storm-scale rotation, meaning the entire cloud rotates, which may give a striated or corkscrew appearance to the storm's updraft.
Dynamically, all supercells are fundamentally similar. However, they often appear quite visually different from each other, depending on the amount of precipitation accompanying the storm and whether precipitation falls adjacent to, or is removed from, the storm's updraft.
In low precipitation supercells, the updraft is on the rear flank of the storm, creating a barber pole or corkscrew appearance to the cloud. Precipitation is sparse or well removed from the updraft and/or is often transparent.
The majority of supercells fall in the "classic" category. The classic supercell will have a large, flat updraft base with striations or banding seen around the periphery of the updraft. Heavy precipitation falls adjacent to the updraft with large hail likely. These have the potential for strong, long-lived tornadoes.
Beneath the supercell, the rotation of the storm is often visible as well, appearing as a lowered, rotating cloud, called a Wall Cloud, formed below the rain-free base and/or below the main storm tower updraft. Wall clouds are often located on the trailing flank of the precipitation.
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Ideas and explanations found in these posts should be attributed to the ENSO blog team, and not to NOAA (the agency) itself. These are blog posts, not official agency communications; if you quote from these posts or from the comments section, you should attribute the quoted material to the blogger or commenter, not to NOAA, CPC, or Climate.gov.
As Emily wrote two weeks ago, weak La Nia conditions are present and favored to continue through mid-winter of 2017. Even though the La Nia is weak and not expected to last very long, it is only fair here at the ENSO blog to give it and its impacts to the jet stream and to the United States some further elaboration.
Generalized Walker Circulation (December-February) anomaly during La Nia events, overlaid on map of average sea surface temperature anomalies. Anomalous ocean cooling (blue-green) in the central and eastern Pacific Ocean and warming over the western Pacific Ocean enhance the rising branch of the Walker circulation over the Maritime Continent and the sinking branch over the eastern Pacific Ocean. Enhanced rising motion is also observed over northern South America, while anomalous sinking motion is found over eastern Africa. NOAA Climate.gov drawing by Fiona Martin.
Unlike El Nio, which shifts thunderstorm activity from the western Pacific to the central Pacific and changes the Walker Circulation, La Nia simply ramps up the normal Walker Circulation. This means even more rising air and thunderstorms over the Maritime Continent and even less rain over the central Pacific Ocean. As the humid air rises over the Maritime Continent and cools, water vapor condenses releasing energy into the tropical upper atmosphere in the form of heat. This heating helps to rev up the Hadley Circulation, which affects the jet stream that typically resides near Japan and extends across the North Pacific Ocean.
An animated gif of the speed and location of the jet stream winds (at an altitude where the pressure is 300 millibars) in three scenarios: (first frame) an average winter (1981-2010), (second frame) La Nia winters, and (third frame) El Nio winters. La Nia winters favor a more northerly track across the United States, while El Nio winters favor a more southerly track. NOAA Climate.gov image based on data from NOAA's Physical Sciences Lab.
At sea level, the average air pressure is around 1013mb. In general, the higher you go in the atmosphere, the less actual air there is, and the lower the air pressure. The anomalies above are of the height in the atmosphere where the pressure has dropped off to 500mb. Positive anomalies mean that the 500mb pressure level is higher in altitude than normal. Negative anomalies mean the opposite: that the altitude where the pressure has fallen off to 500mb is lower than usual.
Average height anomalies at 500mb for December through February in select strong La Nia years. Positive height anomalies over the eastern Pacific indicate higher pressure than normal in that region during La Nia winters which can impact the flow of storms and cold air into the United States.
Correspondingly, if the atmosphere moved air to create the unusually high heights, it must have removed it from someplace else. And indeed, the addition of positive height anomalies in the North Pacific sets off a ripple effect farther downstream across North America (1). This ripple effect is the final bridge which connects changes in the atmosphere along the equator to changes in the atmosphere over the United States. To the north of the positive height anomalies are negative height anomalies over western Canada, while downstream over the southeastern U.S., positive height anomalies return. 152ee80cbc
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