Tropical cyclogenesis

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Global tropical cyclone tracks between 1985 and 2005, indicating the areas where tropical cyclones usually develop Global tropical cyclone tracks-edit2.jpg
Global tropical cyclone tracks between 1985 and 2005, indicating the areas where tropical cyclones usually develop

Tropical cyclogenesis is the development and strengthening of a tropical cyclone in the atmosphere. [1] The mechanisms through which tropical cyclogenesis occurs are distinctly different from those through which temperate cyclogenesis occurs. Tropical cyclogenesis involves the development of a warm-core cyclone, due to significant convection in a favorable atmospheric environment. [2]

Tropical cyclone Is a rotating storm system

A tropical cyclone is a rapidly rotating storm system characterized by a low-pressure center, a closed low-level atmospheric circulation, strong winds, and a spiral arrangement of thunderstorms that produce heavy rain. Depending on its location and strength, a tropical cyclone is referred to by different names, including hurricane, typhoon, tropical storm, cyclonic storm, tropical depression, and simply cyclone. A hurricane is a tropical cyclone that occurs in the Atlantic Ocean and northeastern Pacific Ocean, and a typhoon occurs in the northwestern Pacific Ocean; in the south Pacific or Indian Ocean, comparable storms are referred to simply as "tropical cyclones" or "severe cyclonic storms".

Atmosphere The layer of gases surrounding an astronomical body held by gravity

An atmosphere is a layer or a set of layers of gases surrounding a planet or other material body, that is held in place by the gravity of that body. An atmosphere is more likely to be retained if the gravity it is subject to is high and the temperature of the atmosphere is low.

Tropics region of the Earth surrounding the Equator

The tropics are the region of the Earth surrounding the Equator. They are delimited in latitude by The Tropic of Cancer in the Northern Hemisphere at 23°26′12.4″ (or 23.43679°) N and the Tropic of Capricorn in the Southern Hemisphere at 23°26′12.4″ (or 23.43679°) S; these latitudes correspond to the axial tilt of the Earth. The tropics are also referred to as the tropical zone and the torrid zone. The tropics include all the areas on the Earth where the Sun contacts a point directly overhead at least once during the solar year - thus the latitude of the tropics is roughly equal to the angle of the Earth's axial tilt.

Contents

Tropical cyclogenesis requires six main factors: sufficiently warm sea surface temperatures (at least 26.5 °C (79.7 °F)), atmospheric instability, high humidity in the lower to middle levels of the troposphere, enough Coriolis force to develop a low-pressure center, a pre-existing low-level focus or disturbance, and low vertical wind shear. [3]

Humidity amount of water vapor in the humid air

Humidity is the amount of water vapour present in air. Water vapour, the gaseous state of water, is generally invisible to the human eye. Humidity indicates the likelihood for precipitation, dew, or fog to be present. The amount of water vapour needed to achieve saturation increases as the temperature increases. As the temperature of a parcel of air decreases it will eventually reach the saturation point without adding or losing water mass. The amount of water vapour contained within a parcel of air can vary significantly. For example, a parcel of air near saturation may contain 28 grams of water per cubic metre of air at 30 °C, but only 8 grams of water per cubic metre of air at 8 °C.

Troposphere The lowest layer of the atmosphere

The troposphere is the lowest layer of Earth's atmosphere, and is also where nearly all weather conditions take place. It contains approximately 75% of the atmosphere's mass and 99% of the total mass of water vapor and aerosols. The average height of the troposphere is 18 km in the tropics, 17 km in the middle latitudes, and 6 km in the polar regions in winter. The total average height of the troposphere is 13 km.

Coriolis force A force on objects moving within a reference frame that rotates with respect to an inertial frame.

In physics, the Coriolis force is an inertial or fictitious force that seems to act on objects that are in motion within a frame of reference that rotates with respect to an inertial frame. In a reference frame with clockwise rotation, the force acts to the left of the motion of the object. In one with anticlockwise rotation, the force acts to the right. Deflection of an object due to the Coriolis force is called the Coriolis effect. Though recognized previously by others, the mathematical expression for the Coriolis force appeared in an 1835 paper by French scientist Gaspard-Gustave de Coriolis, in connection with the theory of water wheels. Early in the 20th century, the term Coriolis force began to be used in connection with meteorology.

Tropical cyclones tend to develop during the summer, but have been noted in nearly every month in most basins. Climate cycles such as ENSO and the Madden–Julian oscillation modulate the timing and frequency of tropical cyclone development. [4] [5] There is a limit on tropical cyclone intensity which is strongly related to the water temperatures along its path. [6]

Tropical cyclone basins area of tropical cyclone formation

Traditionally, areas of tropical cyclone formation are divided into seven basins. These include the north Atlantic Ocean, the eastern and western parts of the northern Pacific Ocean, the southwestern Pacific, the southwestern and southeastern Indian Oceans, and the northern Indian Ocean. The western Pacific is the most active and the north Indian the least active. An average of 86 tropical cyclones of tropical storm intensity form annually worldwide, with 47 reaching hurricane/typhoon strength, and 20 becoming intense tropical cyclones, super typhoons, or major hurricanes.

Climate Statistics of weather conditions in a given region over long periods

Climate is the statistics of weather over long periods of time. It is measured by assessing the patterns of variation in temperature, humidity, atmospheric pressure, wind, precipitation, atmospheric particle count and other meteorological variables in a given region over long periods of time. Climate differs from weather, in that weather only describes the short-term conditions of these variables in a given region.

Madden–Julian oscillation

The Madden–Julian oscillation (MJO) is the largest element of the intraseasonal variability in the tropical atmosphere. It was discovered in 1971 by Roland Madden and Paul Julian of the American National Center for Atmospheric Research (NCAR). It is a large-scale coupling between atmospheric circulation and tropical deep atmospheric convection. Unlike a standing pattern like the El Niño–Southern Oscillation (ENSO), the Madden–Julian oscillation is a traveling pattern that propagates eastward at approximately 4 to 8 m/s, through the atmosphere above the warm parts of the Indian and Pacific oceans. This overall circulation pattern manifests itself most clearly as anomalous rainfall.

An average of 86 tropical cyclones of tropical storm intensity form annually worldwide. Of those, 47 reach hurricane/typhoon strength, and 20 become intense tropical cyclones (at least Category 3 intensity on the Saffir–Simpson Hurricane Scale). [7]

Requirements for tropical cyclone formation

Depth of 26 degC isotherm on October 1, 2006 Depth26Cisotherm.gif
Depth of 26 °C isotherm on October 1, 2006

There are six main requirements for tropical cyclogenesis: sufficiently warm sea surface temperatures, atmospheric instability, high humidity in the lower to middle levels of the troposphere, enough Coriolis force to sustain a low pressure center, a preexisting low level focus or disturbance, and low vertical wind shear. [3] While these conditions are necessary for tropical cyclone formation, they do not guarantee that a tropical cyclone will form. [3]

Wind shear

Wind shear, sometimes referred to as wind gradient, is a difference in wind speed or direction over a relatively short distance in the atmosphere. Atmospheric wind shear is normally described as either vertical or horizontal wind shear. Vertical wind shear is a change in wind speed or direction with change in altitude. Horizontal wind shear is a change in wind speed with change in lateral position for a given altitude.

Warm waters, instability, and mid-level moisture

Waves in the trade winds in the Atlantic Ocean--areas of converging winds that move slowly along the same track as the prevailing wind--create instabilities in the atmosphere that may lead to the formation of hurricanes. Atlantic hurricane graphic.gif
Waves in the trade winds in the Atlantic Ocean—areas of converging winds that move slowly along the same track as the prevailing wind—create instabilities in the atmosphere that may lead to the formation of hurricanes.

Normally, an ocean temperature of 26.5 °C (79.7 °F) spanning through at least a 50-metre depth is considered the minimum to maintain a tropical cyclone. [3] These warm waters are needed to maintain the warm core that fuels tropical systems. This value is well above 16.1 °C (60.9 °F), the global average surface temperature of the oceans. [8]

Tropical cyclones are known to form even when normal conditions are not met. For example, cooler air temperatures at a higher altitude (e.g., at the 500  hPa level, or 5.9 km) can lead to tropical cyclogenesis at lower water temperatures, as a certain lapse rate is required to force the atmosphere to be unstable enough for convection. In a moist atmosphere, this lapse rate is 6.5 °C/km, while in an atmosphere with less than 100% relative humidity, the required lapse rate is 9.8 °C/km. [9]

At the 500 hPa level, the air temperature averages −7 °C (18 °F) within the tropics, but air in the tropics is normally dry at this level, giving the air room to wet-bulb, or cool as it moistens, to a more favorable temperature that can then support convection. A wetbulb temperature at 500 hPa in a tropical atmosphere of −13.2 °C is required to initiate convection if the water temperature is 26.5 °C, and this temperature requirement increases or decreases proportionally by 1 °C in the sea surface temperature for each 1 °C change at 500 hpa. Under a cold cyclone, 500 hPa temperatures can fall as low as −30 °C, which can initiate convection even in the driest atmospheres. This also explains why moisture in the mid-levels of the troposphere, roughly at the 500 hPa level, is normally a requirement for development. However, when dry air is found at the same height, temperatures at 500 hPa need to be even colder as dry atmospheres require a greater lapse rate for instability than moist atmospheres. [10] [11] At heights near the tropopause, the 30-year average temperature (as measured in the period encompassing 1961 through 1990) was −77 °C (−105 °F). [12] A recent example of a tropical cyclone that maintained itself over cooler waters was Epsilon of the 2005 Atlantic hurricane season. [13]

Role of Maximum Potential Intensity (MPI)

Kerry Emanuel created a mathematical model around 1988 to compute the upper limit of tropical cyclone intensity based on sea surface temperature and atmospheric profiles from the latest global model runs. Emanuel's model is called the maximum potential intensity , or MPI. Maps created from this equation show regions where tropical storm and hurricane formation is possible, based upon the thermodynamics of the atmosphere at the time of the last model run. This does not take into account vertical wind shear. [14]

Schematic representation of flow around a low-pressure area (in this case, Hurricane Isabel) in the Northern hemisphere. The pressure gradient force is represented by blue arrows, the Coriolis acceleration (always perpendicular to the velocity) by red arrows Hurricane isabel and coriolis force.jpg
Schematic representation of flow around a low-pressure area (in this case, Hurricane Isabel) in the Northern hemisphere. The pressure gradient force is represented by blue arrows, the Coriolis acceleration (always perpendicular to the velocity) by red arrows

Coriolis force

A minimum distance of 500 km (310 mi) from the equator (about 4.5 degrees from the equator) is normally needed for tropical cyclogenesis. [3] The Coriolis force imparts rotation on the flow and arises as winds begin to flow in toward the lower pressure created by the pre-existing disturbance. In areas with a very small or non-existent Coriolis force (e.g. near the Equator), the only significant atmospheric forces in play are the pressure gradient force (the pressure difference that causes winds to blow from high to low pressure [15] ) and a smaller friction force; these two alone would not cause the large-scale rotation required for tropical cyclogenesis. The existence of a significant Coriolis force allows the developing vortex to achieve gradient wind balance. [16] This is a balance condition found in mature tropical cyclones that allows latent heat to concentrate near the storm core; this results in the maintenance or intensification of the vortex if other development factors are neutral. [17]

Low level disturbance

Whether it be a depression in the intertropical covergence zone (ITCZ), a tropical wave, a broad surface front, or an outflow boundary, a low level feature with sufficient vorticity and convergence is required to begin tropical cyclogenesis. [3] Even with perfect upper level conditions and the required atmospheric instability, the lack of a surface focus will prevent the development of organized convection and a surface low. [3] Tropical cyclones can form when smaller circulations within the Intertropical Convergence Zone merge. [18]

Weak vertical wind shear

Vertical wind shear of less than 10 m/s (20  kt, 22 mph) between the surface and the tropopause is favored for tropical cyclone development. [3] A weaker vertical shear makes the storm grow faster vertically into the air, which helps the storm develop and become stronger. If the vertical shear is too strong, the storm cannot rise to its full potential and its energy becomes spread out over too large of an area for the storm to strengthen. [19] Strong wind shear can "blow" the tropical cyclone apart, [20] as it displaces the mid-level warm core from the surface circulation and dries out the mid-levels of the troposphere, halting development. In smaller systems, the development of a significant mesoscale convective complex in a sheared environment can send out a large enough outflow boundary to destroy the surface cyclone. Moderate wind shear can lead to the initial development of the convective complex and surface low similar to the mid-latitudes, but it must relax to allow tropical cyclogenesis to continue. [21]

Favorable trough interactions

Limited vertical wind shear can be positive for tropical cyclone formation. When an upper-level trough or upper-level low is roughly the same scale as the tropical disturbance, the system can be steered by the upper level system into an area with better diffluence aloft, which can cause further development. Weaker upper cyclones are better candidates for a favorable interaction. There is evidence that weakly sheared tropical cyclones initially develop more rapidly than non-sheared tropical cyclones, although this comes at the cost of a peak in intensity with much weaker wind speeds and higher minimum pressure. [22] This process is also known as baroclinic initiation of a tropical cyclone. Trailing upper cyclones and upper troughs can cause additional outflow channels and aid in the intensification process. Developing tropical disturbances can help create or deepen upper troughs or upper lows in their wake due to the outflow jet emanating from the developing tropical disturbance/cyclone. [23] [24]

There are cases where large, mid-latitude troughs can help with tropical cyclogenesis when an upper-level jet stream passes to the northwest of the developing system, which will aid divergence aloft and inflow at the surface, spinning up the cyclone. This type of interaction is more often associated with disturbances already in the process of recurvature. [25]

Times of formation

Peaks of activity worldwide WorldwideTCpeaks.gif
Peaks of activity worldwide

Worldwide, tropical cyclone activity peaks in late summer when water temperatures are warmest. Each basin, however, has its own seasonal patterns. On a worldwide scale, May is the least active month, while September is the most active. [26]

In the North Atlantic, a distinct hurricane season occurs from June 1 through November 30, sharply peaking from late August through October. [26] The statistical peak of the North Atlantic hurricane season is September 10. [27] The Northeast Pacific has a broader period of activity, but in a similar time frame to the Atlantic. [26] The Northwest Pacific sees tropical cyclones year-round, with a minimum in February and a peak in early September. [26] In the North Indian basin, storms are most common from April to December, with peaks in May and November. [26]

In the Southern Hemisphere, tropical cyclone activity generally begins in early November and generally ends on April 30. Southern Hemisphere activity peaks in mid-February to early March. [26] Virtually all the Southern Hemisphere activity is seen from the southern African coast eastward, toward South America. Tropical cyclones are rare events across the south Atlantic Ocean and the far southeastern Pacific Ocean. [28]

Season lengths and averages
BasinSeason
start
Season
end
Tropical
cyclones
Refs
North AtlanticJune 1November 3012.1 [29]
Eastern PacificMay 15November 3016.6 [29]
Western PacificJanuary 1December 3126.0 [29]
North IndianJanuary 1December 314.8 [29]
South-West IndianJuly 1June 309.3 [29] [30]
Australian regionNovember 1April 3011.0 [31]
Southern PacificNovember 1April 307.3 [32]
Total:87.1

Unusual areas of formation

Hurricane Chris formed in the temperate subtropics during the 2012 Atlantic season. Hurricane Chris Jun 21 2012 1330Z.jpg
Hurricane Chris formed in the temperate subtropics during the 2012 Atlantic season.

Middle latitudes

Areas farther than 30 degrees from the equator (except in the vicinity of a warm current) are not normally conducive to tropical cyclone formation or strengthening, and areas more than 40 degrees from the equator are often very hostile to such development. The primary limiting factor is water temperatures, although higher shear at increasing latitudes is also a factor. These areas are sometimes frequented by cyclones moving poleward from tropical latitudes. On rare occasions, such as Alex in 2004, [33] Alberto in 1988, [34] and the 1975 Pacific Northwest hurricane, [35] storms may form or strengthen in this region. Typically, tropical cyclones will undergo extratropical transition after recurving polewards, and typically become fully extratropical after reaching 45–50˚ of latitude. The majority of extratropical cyclones tend to restrengthen after completing the transition period. [36]

Near the Equator

Areas within approximately ten degrees latitude of the equator do not experience a significant Coriolis Force, a vital ingredient in tropical cyclone formation. [37] However, a few tropical cyclones have been observed forming within five degrees of the equator. [38]

South Atlantic

A combination of wind shear and a lack of tropical disturbances from the Intertropical Convergence Zone (ITCZ) makes it very difficult for the South Atlantic to support tropical activity. [39] [40] Over four tropical cyclones have been observed here such as— a weak tropical storm in 1991 off the coast of Africa near Angola, Hurricane Catarina, which made landfall in Brazil in 2004 at Category 2 strength, and a smaller storm in January 2004, east of Salvador, Brazil. The January storm is thought to have reached tropical storm intensity based on scatterometer wind measurements. [41]

Mediterranean and Black Seas

Storms that appear similar to tropical cyclones in structure sometimes occur in the Mediterranean basin. Examples of these "Mediterranean tropical cyclones" formed in September 1947, September 1969, September 1973, August 1976, January 1982, September 1983, December 1984, December 1985, October 1994, January 1995, October 1996, September 1997, December 2005, September 2006, November 2011, November 2014, November 2017 and September 2018. However, there is debate on whether these storms were tropical in nature. [42]

The Black Sea has, on occasion, produced or fueled storms that begin cyclonic rotation, and that appear to be similar to tropical-like cyclones observed in the Mediterranean. [43]

Elsewhere

Tropical cyclogenesis is extremely rare in the far southeastern Pacific Ocean, due to the cold sea-surface temperatures generated by the Humboldt Current, and also due to unfavorable wind shear; as such, there are no records of a tropical cyclone impacting western South America. But in mid-2015, a rare subtropical cyclone was identified in early May relatively close to Chile. This system was unofficially dubbed Katie by researchers. [44] Another subtropical cyclone was identified at 77.8 degrees longitude in May 2018, just off the coast of Chile. [45]

Vortices have been reported off the coast of Morocco in the past. However, it is debatable if they are truly tropical in character. [43]

Tropical activity is also extremely rare in the Great Lakes. However, a storm system that appeared similar to a subtropical or tropical cyclone formed in 1996 on Lake Huron. The system developed an eye-like structure in its center, and it may have briefly been a subtropical or tropical cyclone. [46]

Influence of large-scale climate cycles

Influence of ENSO

Loop of sea surface temperature (SST) anomalies in the Tropical Pacific Sstaanim.gif
Loop of sea surface temperature (SST) anomalies in the Tropical Pacific

El Niño (ENSO) shifts the region (warmer water, up and down welling at different locations, due to winds) in the Pacific and Atlantic where more storms form, resulting in nearly constant Accumulated Cyclone Energy (ACE) values in any one basin. The El Niño event typically decreases hurricane formation in the Atlantic, and far western Pacific and Australian regions, but instead increases the odds in the central North and South Pacific and particular in the western North Pacific typhoon region. [47]

Tropical cyclones in the northeastern Pacific and north Atlantic basins are both generated in large part by tropical waves from the same wave train. [48]

In the Northwestern Pacific, El Niño shifts the formation of tropical cyclones eastward. During El Niño episodes, tropical cyclones tend to form in the eastern part of the basin, between 150°E and the International Date Line (IDL). [49] Coupled with an increase in activity in the North-Central Pacific (IDL to 140°W) and the South-Central Pacific (east of 160°E), there is a net increase in tropical cyclone development near the International Date Line on both sides of the equator. [50] While there is no linear relationship between the strength of an El Niño and tropical cyclone formation in the Northwestern Pacific, typhoons forming during El Niño years tend to have a longer duration and higher intensities. [51] Tropical cyclogenesis in the Northwestern Pacific is suppressed west of 150°E in the year following an El Niño event. [49]

Influence of the MJO

5-day running mean of MJO. Note how it moves eastward with time. MJO 5-day running mean through 1 Oct 2006.png
5-day running mean of MJO. Note how it moves eastward with time.

In general, westerly wind increases associated with the Madden–Julian oscillation lead to increased tropical cyclogenesis in all basins. As the oscillation propagates from west to east, it leads to an eastward march in tropical cyclogenesis with time during that hemisphere's summer season. [52] There is an inverse relationship between tropical cyclone activity in the western Pacific basin and the north Atlantic basin, however. When one basin is active, the other is normally quiet, and vice versa. The main cause appears to be the phase of the Madden–Julian oscillation, or MJO, which is normally in opposite modes between the two basins at any given time. [53]

Influence of equatorial Rossby waves

Research has shown that trapped equatorial Rossby wave packets can increase the likelihood of tropical cyclogenesis in the Pacific Ocean, as they increase the low-level westerly winds within that region, which then leads to greater low-level vorticity. The individual waves can move at approximately 1.8  m/s (4 mph) each, though the group tends to remain stationary. [54]

Seasonal forecasts

Since 1984, Colorado State University has been issuing seasonal tropical cyclone forecasts for the north Atlantic basin, with results that are better than climatology. [55] The university has found several statistical relationships for this basin that appear to allow long range prediction of the number of tropical cyclones. Since then, numerous others have followed in the university's steps, with some organizations issuing seasonal forecasts for the northwest Pacific and the Australian region. [56] The predictors are related to regional oscillations in the global climate system: the Walker circulation which is related to the El Niño-Southern Oscillation; the North Atlantic oscillation (NAO); the Arctic oscillation (AO); and the Pacific North American pattern (PNA). [55]

See also

Related Research Articles

Cyclone large scale air mass that rotates around a strong center of low pressure

In meteorology, a cyclone is a large scale air mass that rotates around a strong center of low atmospheric pressure. Cyclones are characterized by inward spiraling winds that rotate about a zone of low pressure. The largest low-pressure systems are polar vortices and extratropical cyclones of the largest scale. Warm-core cyclones such as tropical cyclones and subtropical cyclones also lie within the synoptic scale. Mesocyclones, tornadoes and dust devils lie within smaller mesoscale. Upper level cyclones can exist without the presence of a surface low, and can pinch off from the base of the tropical upper tropospheric trough during the summer months in the Northern Hemisphere. Cyclones have also been seen on extraterrestrial planets, such as Mars and Neptune. Cyclogenesis is the process of cyclone formation and intensification. Extratropical cyclones begin as waves in large regions of enhanced mid-latitude temperature contrasts called baroclinic zones. These zones contract and form weather fronts as the cyclonic circulation closes and intensifies. Later in their life cycle, extratropical cyclones occlude as cold air masses undercut the warmer air and become cold core systems. A cyclone's track is guided over the course of its 2 to 6 day life cycle by the steering flow of the subtropical jet stream.

Subtropical cyclone

A subtropical cyclone is a weather system that has some characteristics of a tropical and an extratropical cyclone.

Low-pressure area region where the atmospheric pressure is lower than that of surrounding locations

A low-pressure area, low, depression or cyclone is a region on the topographic map where the atmospheric pressure is lower than that of surrounding locations. Low-pressure systems form under areas of wind divergence that occur in the upper levels of the troposphere. The formation process of a low-pressure area is known as cyclogenesis. Within the field of meteorology, atmospheric divergence aloft occurs in two areas. The first area is on the east side of upper troughs, which form half of a Rossby wave within the Westerlies. A second area of wind divergence aloft occurs ahead of embedded shortwave troughs, which are of smaller wavelength. Diverging winds aloft ahead of these troughs cause atmospheric lift within the troposphere below, which lowers surface pressures as upward motion partially counteracts the force of gravity.

Tropical wave type of atmospheric trough

Tropical waves, easterly waves, or tropical easterly waves, also known as African easterly waves in the Atlantic region, are a type of atmospheric trough, an elongated area of relatively low air pressure, oriented north to south, which moves from east to west across the tropics, causing areas of cloudiness and thunderstorms. West-moving waves can also form from the tail end of frontal zones in the subtropics and tropics, and may be referred to as easterly waves, but these waves are not properly called tropical waves; they are a form of inverted trough sharing many characteristics with fully tropical waves. All tropical waves form in the easterly flow along the equatorward side of the subtropical ridge or belt of high pressure which lies north and south of the Intertropical Convergence Zone (ITCZ). Tropical waves are generally carried westward by the prevailing easterly winds along the tropics and subtropics near the equator. They can lead to the formation of tropical cyclones in the north Atlantic and northeastern Pacific basins. A tropical wave study is aided by Hovmöller diagrams, a graph of meteorological data.

Pacific hurricane mature tropical cyclone that develops within the eastern and central Pacific Ocean

A Pacific hurricane is a mature tropical cyclone that develops within the eastern and central Pacific Ocean to the east of 180°W, north of the equator. For tropical cyclone warning purposes, the northern Pacific is divided into three regions: the eastern, central, and western, while the southern Pacific is divided into 2 sections, the Australian region and the southern Pacific basin between 160°E and 120°W. Identical phenomena in the western north Pacific are called typhoons. This separation between the two basins has a practical convenience, however, as tropical cyclones rarely form in the central north Pacific due to high vertical wind shear, and few cross the dateline.

Typhoon type of tropical cyclone

A typhoon is a mature tropical cyclone that develops between 180° and 100°E in the Northern Hemisphere. This region is referred to as the Northwestern Pacific Basin, and is the most active tropical cyclone basin on Earth, accounting for almost one-third of the world's annual tropical cyclones. For organizational purposes, the northern Pacific Ocean is divided into three regions: the eastern, central, and western. The Regional Specialized Meteorological Center (RSMC) for tropical cyclone forecasts is in Japan, with other tropical cyclone warning centers for the northwest Pacific in Hawaii, the Philippines and Hong Kong. While the RSMC names each system, the main name list itself is coordinated among 18 countries that have territories threatened by typhoons each year A hurricane is a storm that occurs in the Atlantic Ocean or the northeastern Pacific Ocean, a typhoon occurs in the northwestern Pacific Ocean, and a tropical cyclone occurs in the South Pacific or the Indian Ocean.

Atlantic hurricane tropical cyclone that forms in the North Atlantic Ocean

An Atlantic hurricane or tropical storm is a tropical cyclone that forms in the Atlantic Ocean, usually between the months of June and November. A hurricane differs from a cyclone or typhoon only on the basis of location. A hurricane is a storm that occurs in the Atlantic Ocean and northeastern Pacific Ocean, a typhoon occurs in the northwestern Pacific Ocean, and a cyclone occurs in the south Pacific or Indian Ocean.

Central dense overcast

The central dense overcast, or CDO, of a tropical cyclone or strong subtropical cyclone is the large central area of thunderstorms surrounding its circulation center, caused by the formation of its eyewall. It can be round, angular, oval, or irregular in shape. This feature shows up in tropical cyclones of tropical storm or hurricane strength. How far the center is embedded within the CDO, and the temperature difference between the cloud tops within the CDO and the cyclone's eye, can help determine a tropical cyclone's intensity. Locating the center within the CDO can be a problem for strong tropical storms and with systems of minimal hurricane strength as its location can be obscured by the CDO's high cloud canopy. This center location problem can be resolved through the use of microwave satellite imagery.

Extratropical cyclone type of cyclone

Extratropical cyclones, sometimes called mid-latitude cyclones or wave cyclones, are low-pressure areas which, along with the anticyclones of high-pressure areas, drive the weather over much of the Earth. Extratropical cyclones are capable of producing anything from cloudiness and mild showers to heavy gales, thunderstorms, blizzards, and tornadoes. These types of cyclones are defined as large scale (synoptic) low pressure weather systems that occur in the middle latitudes of the Earth. In contrast with tropical cyclones, extratropical cyclones produce rapid changes in temperature and dew point along broad lines, called weather fronts, about the center of the cyclone.

Tropical cyclone forecasting is the science of forecasting where a tropical cyclone's center, and its effects, are expected to be at some point in the future. There are several elements to tropical cyclone forecasting: track forecasting, intensity forecasting, rainfall forecasting, storm surge, tornado, and seasonal forecasting. While skill is increasing in regard to track forecasting, intensity forecasting skill remains nearly unchanged over the past several years. Seasonal forecasting began in the 1980s in the Atlantic basin and has spread into other basins in the years since.

Cold-core low cyclone aloft which has an associated cold pool of air residing at high altitude within the Earths troposphere

A cold-core low, also known as an upper level low or cold-core cyclone, is a cyclone aloft which has an associated cold pool of air residing at high altitude within the Earth's troposphere. It is a low pressure system that strengthens with height in accordance with the thermal wind relationship. If a weak surface circulation forms in response to such a feature at subtropical latitudes of the eastern north Pacific or north Indian oceans, it is called a subtropical cyclone. Cloud cover and rainfall mainly occurs with these systems during the day. Severe weather, such as tornadoes, can occur near the center of cold-core lows. Cold lows can help spawn cyclones with significant weather impacts, such as polar lows, and Kármán vortices. Cold lows can lead directly to the development of tropical cyclones, owing to their associated cold pool of air aloft or by acting as additional outflow channels to aid in further development.

Glossary of tropical cyclone terms

The following is a glossary of tropical cyclone terms.

References

  1. "Definition for Cyclogenesis". Arctic Climatology and Meteorology. National Snow and Ice Data Center. Archived from the original on August 30, 2006. Retrieved October 20, 2006.
  2. Goldenberg, Stan (August 13, 2004). "What is an extra-tropical cyclone?". Frequently Asked Questions: Hurricanes, Typhoons and Tropical Cyclones. Atlantic Oceanographic and Meteorological Laboratory, Hurricane Research Division. Retrieved August 30, 2008.
  3. 1 2 3 4 5 6 7 8 Landsea, Chris. "How do tropical cyclones form?". Frequently Asked Questions. Atlantic Oceanographic and Meteorological Laboratory, Hurricane Research Division. Retrieved October 9, 2017.
  4. Landsea, Christopher. "AOML Climate Variability of Tropical Cyclones paper". Atlantic Oceanographic and Meteorological Laboratory. Retrieved September 23, 2010.
  5. "Madden-Julian Oscillation". UAE. Retrieved September 23, 2010.
  6. Berg, Robbie. "Tropical cyclone intensity in relation to SST and moisture variability" (PDF). RSMAS (University of Miami. Retrieved September 23, 2010.
  7. Chris Landsea (January 4, 2000). "Climate Variability table — Tropical Cyclones". Atlantic Oceanographic and Meteorological Laboratory, National Oceanic and Atmospheric Administration . Retrieved October 19, 2006.
  8. Matt Menne (March 15, 2000). "Global Long-term Mean Land and Sea Surface Temperatures". National Climatic Data Center. Archived from the original on December 19, 2002. Retrieved October 19, 2006.
  9. Kushnir, Yochanan. "The Climate System". EESC. Retrieved September 24, 2010.
  10. John M. Wallace & Peter V. Hobbs (1977). Atmospheric Science: An Introductory Survey. Academic Press, Inc. pp. 76–77.
  11. Chris Landsea (2000). "Climate Variability of Tropical Cyclones: Past, Present and Future". Storms. Atlantic Oceanographic and Meteorological Laboratory. pp. 220–41. Retrieved October 19, 2006.
  12. Dian J. Gaffen-Seidel, Rebecca J. Ross and James K. Angell (November 2000). "Climatological characteristics of the tropical tropopause as revealed by radiosondes". National Oceanic and Atmospheric Administration Air Resources Laboratory. Archived from the original on May 8, 2006. Retrieved October 19, 2006.
  13. Lixion Avila (December 3, 2005). "Hurricane Epsilon Discussion Eighteen". National Hurricane Center. Retrieved December 14, 2010.
  14. Kerry A. Emanuel (1998). "Maximum Intensity Estimation". Massachusetts Institute of Technology . Retrieved October 20, 2006.
  15. Department of Atmospheric Sciences (October 4, 1999). "Pressure Gradient Force". University of Illinois at Urbana-Champaign . Retrieved October 20, 2006.
  16. G.P. King (November 18, 2004). "Vortex Flows and Gradient Wind Balance" (PDF). University of Warwick. Archived from the original (PDF) on November 29, 2007. Retrieved October 20, 2006.
  17. Kepert, Jeffrey D. (2010). "Tropical Cyclone Structure and Dynamics" (PDF). In Johnny C.L. Chan, Jeffrey D Kepert. Global Perspectives on Tropical Cyclones: From Science to Mitigation. Singapore: World Scientific. ISBN   978-981-4293-47-1. Archived from the original (PDF) on June 29, 2011. Retrieved February 2, 2011.
  18. Kieu, Chanh Q. & Da-Lin Zhang (June 2010). "Genesis of Tropical Storm Eugene (2005) from Merging Vortices Associated with ITCZ Breakdowns. Part III: Sensitivity to Various Genesis Parameters". Journal of the Atmospheric Sciences. 67 (6): 1745. Bibcode:2010JAtS...67.1745K. doi:10.1175/2010JAS3227.1.
  19. "Hurricanes: a tropical cyclone with winds > 64 knots". University of Illinois. 2006. Retrieved 24 March 2014.
  20. Department of Atmospheric Sciences (DAS) (1996). "Hurricanes". University of Illinois at Urbana-Champaign . Retrieved August 9, 2008.
  21. University of Illinois (October 4, 1999). Hurricanes. Retrieved 2008-08-17.
  22. M. E. Nicholls & R. A. Pielke (April 1995). "A Numerical Investigation of the Effect of Vertical Wind Shear on Tropical Cyclone Intensification" (PDF). 21st Conference on Hurricanes and Tropical Meteorology of the American Meteorological Society . Colorado State University. pp. 339–41. Archived from the original (PDF) on September 9, 2006. Retrieved October 20, 2006.
  23. Clark Evans (January 5, 2006). "Favorable trough interactions on tropical cyclones". Flhurricane.com. Retrieved October 20, 2006.
  24. Deborah Hanley; John Molinari & Daniel Keyser (October 2001). "A Composite Study of the Interactions between Tropical Cyclones and Upper-Tropospheric Troughs". Monthly Weather Review . 129 (10): 2570–84. Bibcode:2001MWRv..129.2570H. doi:10.1175/1520-0493(2001)129<2570:ACSOTI>2.0.CO;2. ISSN   1520-0493.
  25. Eric Rappin & Michael C. Morgan. "The Tropical Cyclone — Jet Interaction" (PDF). University of Wisconsin, Madison. Archived from the original (PDF) on September 7, 2006. Retrieved October 20, 2006.
  26. 1 2 3 4 5 6 Atlantic Oceanographic and Meteorological Laboratory, Hurricane Research Division. "Frequently Asked Questions: When is hurricane season?". National Oceanic and Atmospheric Administration. Archived from the original on May 5, 2009. Retrieved July 25, 2006.
  27. Kaye, Ken (September 9, 2010). "Peak of hurricane season". Sun Sentinel. Retrieved 23 September 2010.
  28. Chris Landsea (July 13, 2005). "FAQ: Why doesn't the South Atlantic Ocean experience tropical cyclones?". NOAA. Retrieved May 14, 2009.
  29. 1 2 3 4 5 Hurricane Research Division. "Frequently Asked Questions: What are the average, most, and least tropical cyclones occurring in each basin?". National Oceanic and Atmospheric Administration's Atlantic Oceanographic and Meteorological Laboratory. Retrieved December 5, 2012.
  30. RA I Tropical Cyclone Committee (November 9, 2012). Tropical Cyclone Operational Plan for the South-West Indian Ocean: 2012 (PDF) (Report No. TCP-12). World Meteorological Organization. pp. 11–14. Archived (PDF) from the original on March 29, 2015. Retrieved March 29, 2015.
  31. National Climate Prediction Centre (October 14, 2013). "2013/14 Australian Tropical Cyclone season outlook". Australian Bureau of Meteorology. Retrieved October 14, 2013.
  32. RSMC Nadi — Tropical Cyclone Centre (October 22, 2015). "2015–16 Tropical Cyclone Season Outlook in the Regional Specialised Meteorological Centre Nadi – Tropical Cyclone Centre (RSMC Nadi – TCC) Area of Responsibility (AOR)". Fiji Meteorological Service. Archived from the original (PDF) on October 22, 2015. Retrieved October 22, 2015.
  33. James L. Franklin (October 26, 2004). "Hurricane Alex Tropical Cyclone Report". National Hurricane Center . Retrieved October 24, 2006.
  34. "Alberto "Best-track"". Unysis Corporation. Archived from the original on January 31, 2008. Retrieved March 31, 2006.
  35. "12" "Best-track". Unysis Corporation. Archived from the original on January 31, 2009. Retrieved March 31, 2006.
  36. Evans, Jenni L.; Hart, Robert E. (May 2003). "Objective Indicators of the Life Cycle Evolution of Extratropical Transition for Atlantic Tropical Cyclones". Monthly Weather Review. 131 (5): 911–913. Bibcode:2003MWRv..131..909E. doi:10.1175/1520-0493(2003)131<0909:OIOTLC>2.0.CO;2.
  37. Chang, C.-P.; Liu, C.-H.; Kuo, H.-C. (February 2003). "Typhoon Vamei: An equatorial tropical cyclone formation". Geophysical Research Letters . 30 (3): 1150. Bibcode:2003GeoRL..30.1150C. doi:10.1029/2002GL016365 . Retrieved November 15, 2010.
  38. Staff Writer (October 28, 2010). "Tropical Cyclone Guidance 2010–11" (PDF). Fiji Meteorological Service. Archived from the original (PDF) on November 13, 2010. Retrieved November 13, 2010.
  39. Atlantic Oceanographic and Meteorological Laboratory, Hurricane Research Division. "Frequently Asked Questions: Why doesn't the South Atlantic Ocean experience tropical cyclones?". National Oceanic and Atmospheric Administration . Retrieved July 25, 2006.
  40. Department of Meteorology, e-Education Institute. "Upper-Level Lows". Meteorology 241: Fundamentals of Tropical Forecasting. Pennsylvania State University. Archived from the original on September 7, 2006. Retrieved October 24, 2006.
  41. "Monitoramento – Ciclone tropical na costa gaúcha" (in Portuguese). Brazilian Meteorological Service. March 2010. Archived from the original on March 10, 2010.
  42. Atlantic Oceanographic and Meteorological Laboratory, Hurricane Research Division. "Frequently Asked Questions: What regions around the globe have tropical cyclones and who is responsible for forecasting there?". NOAA . Retrieved July 25, 2006.
  43. 1 2 "Miscellaneous Images". Met Office. Archived from the original on September 29, 2007. Retrieved 21 November 2015.
  44. Diamond, Howard J (August 25, 2015). "Review of the 2014/15 Tropical Cyclone Season in the Southwest Pacific Ocean Basin". Climate Program Office. National Oceanic and Atmospheric Administration. Retrieved October 16, 2017.
  45. Jonathan Belles (May 9, 2018). "Extremely Rare Southeast Pacific Subtropical Cyclone Forms Off the Chilean Coast". The Weather Channel. Retrieved May 10, 2018.
  46. Todd Miner; Peter J. Sousounis; James Wallman & Greg Mann (February 2000). "Hurricane Huron". Bulletin of the American Meteorological Society. 81 (2): 223–36. Bibcode:2000BAMS...81..223M. doi:10.1175/1520-0477(2000)081<0223:HH>2.3.CO;2.
  47. "Climate Change 2007: Working Group I: The Physical Science Basis". IPCC. 2007.
  48. Avila, Lixion A.; Pasch, Richard J. (March 1995). "Atlantic Tropical Systems of 1993". Monthly Weather Review. 123 (3): pg. 893. Bibcode:1995MWRv..123..887A. doi:10.1175/1520-0493(1995)123<0887:ATSO>2.0.CO;2. ISSN   1520-0493.
  49. 1 2 Chan, J. C. L. (April 1985). "Tropical Cyclone Activity in the Northwest Pacific in Relation to the El Niño/Southern Oscillation Phenomenon". Monthly Weather Review . 113 (4): 599–606. Bibcode:1985MWRv..113..599C. doi:10.1175/1520-0493(1985)113<0599:TCAITN>2.0.CO;2. ISSN   1520-0493.
  50. Bureau of Meteorology Research Centre. "ENSO Relationships with Seasonal Tropical Cyclone Activity". Global Guide to Tropical Cyclone Forecasting. Australian Bureau of Meteorology. Archived from the original on November 27, 2012. Retrieved October 20, 2006.
  51. Camargo, Suzana J.; Adam H. Sobel (August 2005). "Western North Pacific Tropical Cyclone Intensity and ENSO". Journal of Climate . 18 (15): 2996. Bibcode:2005JCli...18.2996C. doi:10.1175/JCLI3457.1.
  52. John Molinari & David Vollaro (September 2000). "Planetary- and Synoptic-Scale Influences on Eastern Pacific Tropical Cyclogenesis". Monthly Weather Review . 128 (9): 3296–307. Bibcode:2000MWRv..128.3296M. doi:10.1175/1520-0493(2000)128<3296:PASSIO>2.0.CO;2. ISSN   1520-0493.
  53. Maloney, E. D. & D. L. Hartmann (September 2001). "The Madden–Julian Oscillation, Barotropic Dynamics, and North Pacific Tropical Cyclone Formation. Part I: Observations". Journal of the Atmospheric Sciences . 58 (17): 2545–2558. Bibcode:2001JAtS...58.2545M. CiteSeerX   10.1.1.583.3789 . doi:10.1175/1520-0469(2001)058<2545:TMJOBD>2.0.CO;2. ISSN   1520-0469.
  54. Kelly Lombardo. "Influence of Equatorial Rossby Waves on Tropical Cyclogenesis in the Western Pacific" (PDF). State University of New York at Albany . Retrieved October 20, 2006.
  55. 1 2 Philip J. Klotzbach; Willam Gray & Bill Thornson (October 3, 2006). "Extended Range Forecast of Atlantic Seasonal Hurricane Activity and U.S. Landfall Strike Probability for 2006". Colorado State University . Retrieved October 20, 2006.
  56. Mark Saunders & Peter Yuen. "Tropical Storm Risk Group Seasonal Predictions". Tropical Storm Risk. Archived from the original on May 4, 2006. Retrieved October 20, 2006.