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Funnel cloud

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"Funnel Cloud" redirects here. For the Hem album, see Funnel Cloud (album).
A needle-like funnel cloud, which may have been a tornadic circulation but was not yet visible as such and which did later develop to become a confirmed tornado, near Elie, Manitoba

A funnel cloud is a funnel-shaped cloud of condensed water droplets, associated with a rotating column of wind and extending from the base of a cloud (usually a cumulonimbus or towering cumulus cloud) but not reaching the ground or a water surface.[1] A funnel cloud is usually visible as a cone-shaped or needle like protuberance from the main cloud base. Funnel clouds form most frequently in association with supercell thunderstorms, and are often, but not always, a visual precursor to tornadoes. Funnel clouds are visual phenomena, these are not the vortex of wind itself.[2]

"Classic" funnel clouds

If a funnel cloud touches the surface the feature is considered a tornado, although ground level circulations begin before the visible condensation cloud appears. Most tornadoes begin as funnel clouds, but some funnel clouds do not make surface contact and these cannot be counted as tornadoes from the perspective of a naked eye observer, even as tornadic circulations of some intensity almost always are detectable when low-level radar observations are available. Also, tornadoes occur with some frequency without an associated condensation funnel. The term condensation funnel may refer to either a tornadic cloud or a funnel cloud aloft, but the term funnel cloud exclusively refers to a rotating condensation funnel not reaching the surface. If strong cyclonic winds are occurring at the surface and are connected to a cloud base, regardless of condensation, then the feature is a tornado.[3]

Debris swirls are usually evident prior to the condensation funnel reaching the surface. Some tornadoes may appear only as a debris swirl, with no obvious funnel cloud extending below the rotating cloud base at any time during the tornadic life cycle. The surface level vortex tends to strengthen over time following initial formation, making the debris swirls and the condensation more apparent.[citation needed]

In cloud nomenclature, any funnel- or inverted-funnel-shaped cloud descending from cumulus or cumulonimbus clouds is technically described as an accessory feature called tuba. The terms tuba and funnel cloud are nearly but not exactly synonymous; a wall cloud, for example, is also a form of tuba. Funnel clouds associated with supercells usually form within and under wall clouds.

Cold-air funnel clouds

Cold-air funnel clouds (vortices) are generally much weaker than the vortices produced by supercells. Although cold-air funnels rarely make ground contact, surface level vortices sometimes become strong enough for condensation cloud to "touch down" briefly, becoming visible as weak tornadoes or waterspouts.

A shear funnel extending from a cumulus humilis cloud, which was observed in northern Texas during the first VORTEX project.

Unlike the related phenomenon associated with severe thunderstorms, cold-air funnels are generally associated with partly cloudy skies in the wake of cold fronts,[4] especially associated with certain low pressure systems, or in association with atmospheric boundaries such as lake[5] and sea breezes or outflow boundaries. The larger scale weather conditions are characterized by particularly cold air aloft over relatively warmer low level air, leading to high lapse rates, and often by high environmental vorticity yet relatively meager vertical wind shear. The funnels develop where atmospheric instability and moisture are sufficient to support towering cumulus clouds but typically limited to no or to little precipitation. Cold-air funnels, although weak, may persist for several minutes, and areas of intermittently forming funnel clouds may occur for tens of minutes.[6]

Multiple such areas of activity may form within the same region during afternoon heating. Cold-air funnels appears to be a diurnal phenomenon, weakening and eventually dissipating with loss of solar heating. When precipitation does develop, the associated downdraft tends to cause rapid demise of the cold-air funnels. The mixing of cooler air in the lower troposphere with air flowing in a different direction in the middle troposphere causes the rotation on a horizontal axis, which, when deflected and tightened vertically by convective updrafts, forms a vertical rotation that can cause condensation to form a funnel cloud.[7]

Cold-air funnel clouds are a common sight along the Pacific Coast of the United States, particularly in the spring or fall.[7]

On July 29, 2013, a cold-core funnel cloud touched down as an EF0 tornado in Ottawa, Ontario, Canada, causing extensive damage in the form of downed trees on a golf course. No advance weather watches or warnings were issued by Environment Canada, and the tornado was spawned from one of the few non-severe storm clouds moving through the area.[8][9]

Other funnel clouds

Other funnel clouds include shear or "high based" funnels, which are ephemeral, small, and weak funnels associated with small cumulus clouds, often even those rooted aloft above the boundary or surface layer, and in "fair weather" conditions.[10] Small funnel clouds, such as some occurring within vicinity of mountains, occur by unknown processes.[11]

Shear funnels might also occur with weak transient circulations at the cloud base of thunderstorms. Mesoanticyclones, which accompany mesocyclones, often exhibit these funnel clouds. Brief funnels also are observed with some rear flank downdrafts (RFDs) (within inflow or outflow areas, and especially within inflow-outflow interchange areas as RFDs interact with mesocyclones or flanking line updrafts) and streamwise vorticity currents (SVCs) feeding into mesocyclones.

Although not considered a separate kind of funnel cloud, some funnel clouds form with mesovortices associated with squall lines, which also can become tornadoes but are often not visible as funnel clouds or tornadoes because they usually occur within obscuring precipitation. Other "fair weather" funnel clouds include horseshoe clouds which are a very transient phenomena associated with extremely weak vortices.

See also

References

  1. ^ Glickman, Todd S. (2000). Glossary of Meteorology (2nd ed.). Boston: American Meteorological Society. ISBN 978-1878220349.
  2. ^ "Funnel cloud". National Weather Service Glossary. NOAA National Weather Service. Retrieved 2019-12-17.
  3. ^ Edwards, Roger (19 April 2018). "What's the difference between a funnel cloud and a tornado? What is a funnel cloud?". The Online Tornado FAQ. NWS Storm Prediction Center. Retrieved 2019-12-17.
  4. ^ Davies, Jonathan M. (2006). "Tornadoes with Cold Core 500-mb Lows". Weather and Forecasting. 21 (6): 1051–1062. Bibcode:2006WtFor..21.1051D. doi:10.1175/WAF967.1.
  5. ^ Cooley, Jack R. (1978). "Cold Air Funnel Clouds". Monthly Weather Review. 106 (9): 1368–1372. Bibcode:1978MWRv..106.1368C. doi:10.1175/1520-0493(1978)106<1368:CAFC>2.0.CO;2. ISSN 1520-0493.
  6. ^ Rauber, Robert M.; R. Scott (2001). "Central Illinois Cold Air Funnel Outbreak". Monthly Weather Review. 129 (11): 2815–2821. Bibcode:2001MWRv..129.2815R. doi:10.1175/1520-0493(2001)129<2815:CICAFO>2.0.CO;2. ISSN 1520-0493.
  7. ^ a b Cooley J. R., and M. E. Soderberg, 1973: Cold air funnel clouds. NOAA Tech. Memo. NWS CR-52, Scientific Services Division, NWS Central Region, Kansas City, MO, 29 pp.
  8. ^ http://www.cbc.ca/news/canada/ottawa/story/2013/07/30/ottawa-funnel-clouds-storm-video.html
  9. ^ Lypny, Natascia (July 30, 2013). "'Cold core funnels' give Ottawa commuters a twister fright". ottawacitizen.com. Archived from the original on August 1, 2013. Retrieved August 2, 2013.
  10. ^ Bluestein, Howard B. (1994). "High-Based Funnel Clouds in the Southern Plains". Monthly Weather Review. 122 (11): 2631–2638. Bibcode:1994MWRv..122.2631B. doi:10.1175/1520-0493(1994)122<2631:hbfcit>2.0.co;2.
  11. ^ Bluestein, Howard B. (2005). "More Observations of Small Funnel Clouds and Other Tubular Clouds". Monthly Weather Review. 133 (12): 3714–3720. Bibcode:2005MWRv..133.3714B. doi:10.1175/MWR3080.1.
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