'Tropical cyclogenesis' is the technical term describing 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 mid-
latitude cyclogenesis occurs. Tropical cyclogenesis involves the development of a
warm-core cyclone, due to significant
convection in a favorable atmospheric environment. 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 (at least Category 3 intensity on the
Saffir-Simpson Hurricane Scale).
[2]
Requirements for formation
Depth of 26 °C
isotherm on October 1, 2006
Although the formation of
tropical cyclones is the topic of extensive ongoing research and is still not fully understood, 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 develop a low pressure center, a preexisting low level focus or disturbance, and low vertical
wind shear.
Warm waters, instability, and mid-level moisture
Waves in the trade winds in the Atlantic Ocean—areas of converging winds that move 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 the special
mesocyclone that is the
tropical cyclone. These warm waters are needed to maintain the
warm core that fuels tropical systems. This value is well above the global average surface temperature of the oceans, which is 16.1 °C (60.9 °F).
[3] However, this requirement can be considered only a general baseline because it assumes that the ambient atmospheric environment surrounding an area of disturbed weather presents average conditions.
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.
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
wetbulb, 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, at the air temperatures normally witnessed at 500 hPa does not promote large areas of thunderstorms.
[4] At heights near the
tropopause, the 30-year average temperature (as measured in the period encompassing 1961 through 1990) was -77 °C (-132 °F).
[5] Recent examples of
tropical cyclones that maintained themselves over cooler waters include
Delta,
Epsilon, and
Zeta of the
2005 Atlantic hurricane season.
Role of Maximum Potential Intensity (MPI)
Dr. 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 (either 0000 or 1200
UTC). This does not take into account vertical
wind shear.
[6]
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 (300
miles) from the
equator is normally needed for tropical cyclogenesis. The role of the
Coriolis force is to provide for gradient wind balance by correcting the interaction of the ''pressure gradient force'' (the pressure difference that causes winds to blow from high to low pressure
[7] ) and ''geostrophic winds'' (the force that causes winds to blow parallel to straight
isobars) for
centripetal acceleration (which is introduced by curved
isobars).
[8] Bays and gulfs can enhance local rotation of a storm, and cause formation close to the equator, similar to that witnessed during
Typhoon Vamei's life cycle.
[9]
Low level disturbance
Whether it be the
monsoon trough, 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. 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.
Weak vertical wind shear
Vertical wind shear of less than 10
m/s (22
mph) between the surface and the
tropopause is required for tropical cyclone development. Strong wind shear can "blow" the tropical cyclone apart, 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.
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.
[10] 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. It should be noted that developing tropical disturbances can help create or deepen upper troughs or upper lows in their wake due to the outflow jet eminating from the developing tropical disturbance/cyclone.
[11][12]
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.
[13]
Times of formation
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.
[ Frequently Asked Questions: When is hurricane season? Atlantic Oceanographic and Meteorological Laboratory, Hurricane Research Division ] This can be explained by the greater tropical cyclone activity across the Northern hemisphere than south of the equator.
In the North
Atlantic, a distinct hurricane season occurs from
June 1 through
November 30, sharply peaking from late August through September. The statistical peak of the North Atlantic hurricane season is
September 10. The Northeast Pacific has a broader period of activity, but in a similar time frame to the Atlantic. The Northwest Pacific sees tropical cyclones year-round, with a minimum in February and a peak in early September. In the North Indian basin, storms are most common from April to December, with peaks in May and November.
In the
Southern Hemisphere, tropical cyclone activity begins in late October and ends in May. Southern Hemisphere activity peaks in mid-February to early March.
Virtually all the Southern Hemisphere activity is seen from the southern African coast eastward towards South America. Tropical cyclones are rare events across the south Atlantic ocean.
Unusual areas of formation
Global Tropical Cyclone Tracks between 1985 and 2005, indicating the areas where tropical cyclones usually develop
For areas of unusual
landfall, please see
Unusual Landfalls and
Tropical cyclone landfall.
Subtropics
Areas farther than thirty degrees from the equator are not normally conducive to tropical cyclone formation or strengthening, and areas more than forty degrees from the equator are 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 in
2004,
[14] 1988[ Alberto "Best-track" ] and
1975,
[ "12" "Best-track" ] storms may form or strengthen in this region.
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. In December 2001, however,
Typhoon Vamei formed in the southern South China Sea and made landfall in
Malaysia. It formed from a thunderstorm formation in
Borneo that moved into the South China Sea.
[15]
Southeastern Pacific
Tropical cyclone formation is rare in this region. When tropical cyclones do form, they are frequently linked to El Niño episodes. Most of the tropical cyclones that enter this region formed farther west in the Southwest Pacific. They affect the islands of
Polynesia in rare instances. During the 1982/83 El Niño event, French Polynesia was affected by six tropical cyclones in five months.
[16] There are no records of a tropical cyclone hitting western
South America.
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.
[ Frequently Asked Questions: Why doesn't the South Atlantic Ocean experience tropical cyclones? Atlantic Oceanographic and Meteorological Laboratory, Hurricane Research Division ][17] Three tropical cyclones have been observed here — a weak tropical storm in 1991 off the coast of
Africa near
Angola,
Cyclone Catarina (sometimes also referred to as Aldonça), which made landfall in
Brazil in 2004 at
Category 1 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.
Mediterranean Sea
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, January
1982, September
1983, and January
1995. However, there is debate on whether these storms were tropical in nature.
[ Frequently Asked Questions: What regions around the globe have tropical cyclones and who is responsible for forecasting there? Atlantic Oceanographic and Meteorological Laboratory, Hurricane Research Division ]
Black Sea
The
Black Sea has, on occasion, produced or fueled storms that begin cyclonic rotation, and appear to be similar to cyclones seen in the
Mediterranean.
[18]
Morocco
Vortices have been reported off the coast of
Morocco in the past. However, it is debatable if they are truly tropical in character.
Great Lakes
:''See also: '
1996 Lake Huron cyclone'''
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. It formed an
eye-like structure in its center, and it may have briefly been a subtropical or tropical cyclone.
[19]
Influence of large-scale climate cycles
Loop of SST anomalies in the Tropical Pacific
Influence of ENSO
Warm waters during the
El Niño-Southern Oscillation lower the potential of tropical cyclone formation primarily in the
Atlantic Basin and around Australia, but tend to cause an increase in activity in the North West Pacific Ocean. Because tropical cyclones in the northeastern Pacific and north Atlantic basins are both generated in large part by
tropical waves from the same wave train, decreased tropical cyclone activity in the north Atlantic translates to increased tropical cyclone activity in the Eastern North Pacific. Although El Niño does not impact the number of tropical cyclones in the Western North Pacific, El Niño shifts their formation, as cyclones form farther to the east than normal. Near the
International Date Line on both sides of the equator, there is a net increase in tropical cyclone development during El Niño.
[20]
5-day running mean of MJO. Note how it moves eastward with time.
Influence of the MJO
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.
[21] 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 reason for this 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.
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.
[22]
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. 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.
[23] The predictors are related to regional oscillations in the global
climate system: the
Walker circulation which is related to
ENSO (El Niño and La Niña) and the Southern Oscillation Index; the
North Atlantic oscillation or NAO; the
Arctic oscillation or AO; and, the Pacific North American pattern or PNA.
[24]
See also
★
Rossby wave
★
Tropical cyclone
★
Tropical wave
★
Monsoon trough
References
1. Definition for Cyclogenesis Arctic Climatology and Meteorology
2. Climate Variability table - Tropical Cyclones Chris Landsea
3. Global Long-term Mean Land and Sea Surface Temperatures Matt Menne
4. Climate Variability of Tropical Cyclones: Past, Present and Future Chris Landsea
5. Climatological characteristics of the tropical tropopause as revealed by radiosondes Dian J. Gaffen-Seidel, Rebecca J. Ross and James K. Angell
6. Maximum Intensity Estimation Kerry A. Emanuel
7. Pressure Gradient Force Department of Atmospheric Sciences
8. Vortex Flows and Gradient Wind Balance G.P. King
9. Scientists dissect rare typhoon near Equator
10. A Numerical Investigation of the Effect of Vertical Wind Shear on Tropical Cyclone Intensification M. E. Nicholls and R. A. Pielke
11. Favorable trough interactions on tropical cyclones Clark Evans
12. A Composite Study of the Interactions between Tropical Cyclones and Upper-Tropospheric Troughs, Deborah Hanley, John Molinari, and Daniel Keyser, , , Monthly Weather Review, 2001
13. The Tropical Cyclone - Jet Interaction Eric Rappin and Michael C. Morgan
14. Hurricane Alex Tropical Cyclone Report James L. Franklin
15. Vamei "Best-track"
16. El Niño and Sea Level Changes T. S. Cheng
17. Upper-Level Lows Department of Meteorology, e-Education Institute
18. MetOffice. Miscellaneous Images. Retrieved on 2007-05-11.
19. Hurricane Huron, Todd Miner, Peter J. Sousounis, James Wallman, and Greg Mann, , , Bulletin of the American Meteorological Society, 2000
20. ENSO Relationships with Seasonal Tropical Cyclone Activity Bureau of Meteorology Research Centre
21. Planetary- and Synoptic-Scale Influences on Eastern Pacific Tropical Cyclogenesis, John Molinari and David Vollaro, , , Monthly Weather Review, 2000
22. Influence of Equatorial Rossby Waves on Tropical Cyclogenesis in the Western Pacific Kelly Lombardo
23. Tropical Storm Risk Group Seasonal Predictions Mark Saunders and Peter Yuen
24. Extended Range Forecast of Atlantic Seasonal Hurricane Activity and U.S. Landfall Strike Probability for 2006 Philip J. Klotzbach, Willam Gray, and Bill Thornson
External sites
★
Current AO conditions
★
Current ENSO conditions
★
Current MJO conditions
★
Current NAO conditions
★
Current PNA conditions
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Maximum Potential Intensity
★
Maximum Potential Intensity Maps Worldwide
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Tropical Cyclone Heat Potential
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