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67-492: Tropical cyclone formation requires several factors, including: high humidity , low wind shear , and sufficiently warm sea surface temperatures . Regions of Earth's oceans with the required conditions are generally found between the latitudes of 8° and 20° from the Equator . An ocean temperature of at least 26.5 °C (79.7 °F) is normally considered the minimum to maintain a tropical cyclone . If water temperatures are lower,

134-419: A 50-metre depth is considered the minimum to maintain a tropical cyclone . 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. 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

201-433: A greater lapse rate for instability than moist atmospheres. At heights near the tropopause , the 30-year average temperature (as measured in the period encompassing 1961 through 1990) was −77 °C (−105 °F). A recent example of a tropical cyclone that maintained itself over cooler waters was Epsilon of the 2005 Atlantic hurricane season . Kerry Emanuel created a mathematical model around 1988 to compute

268-615: 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 generally begins in early November and generally ends on April 30. Southern Hemisphere activity peaks in mid-February to early March. Virtually all the Southern Hemisphere activity

335-506: A pool feels much colder on a windy day), there is a positive feedback on energy input into the system known as the Wind-Induced Surface Heat Exchange (WISHE) feedback. This feedback is offset when frictional dissipation, which increases with the cube of the wind speed, becomes sufficiently large. This upper bound is called the "maximum potential intensity", v p {\displaystyle v_{p}} , and

402-467: A pre-existing low-level focus or disturbance, and low vertical wind shear . 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. The maximum potential intensity is a limit on tropical cyclone intensity which

469-416: A rare subtropical cyclone was identified in early May, slightly near Chile , even further east than the 1983 tropical depression. This system was unofficially dubbed Katie by researchers. Another subtropical cyclone was identified at 77.8 degrees longitude west in May 2018, just off the coast of Chile. This system was unofficially named Lexi by researchers. A subtropical cyclone was spotted just off

536-409: 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. 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

603-576: A subtropical or tropical cyclone. Tropical cyclones typically began to weaken immediately following and sometimes even prior to landfall as they lose the sea fueled heat engine and friction slows the winds. However, under some circumstances, tropical or subtropical cyclones may maintain or even increase their intensity for several hours in what is known as the brown ocean effect . This is most likely to occur with warm moist soils or marshy areas, with warm ground temperatures and flat terrain, and when upper level support remains conducive. El Niño (ENSO) shifts

670-471: A surface focus will prevent the development of organized convection and a surface low. Tropical cyclones can form when smaller circulations within the Intertropical Convergence Zone come together and merge. 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. Weaker vertical shear makes

737-532: A system will most likely weaken. Conversely, higher water temperatures can enable a system to undergo rapid intensification . In the Atlantic, the area between 10°N and 20°N spawns the most hurricanes in a given season because of the warmer temperatures. Hurricanes do not form outside this range because nearer to the equator the Coriolis effect is not strong enough to create the tight circulation needed, and farther north

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804-485: A tropical cyclone impacting western South America. Besides Yaku, there have been several other systems that have been observed developing in the region east of 120°W , which is the official eastern boundary of the South Pacific basin . On May 11, 1983, a tropical depression developed near 110°W , which was thought to be the easternmost forming South Pacific tropical cyclone ever observed in the satellite era. In mid-2015,

871-491: A tropical cyclone is the theoretical limit of the strength of a tropical cyclone . Due to surface friction, the inflow only partially conserves angular momentum. Thus, the sea surface lower boundary acts as both a source (evaporation) and sink (friction) of energy for the system. This fact leads to the existence of a theoretical upper bound on the strongest wind speed that a tropical cyclone can attain. Because evaporation increases linearly with wind speed (just as climbing out of

938-508: A tropical cyclone may be idealized as a Carnot heat engine , the Carnot heat engine efficiency is given by Heat (enthalpy) per unit mass is given by where C p {\displaystyle C_{p}} is the heat capacity of air, T {\displaystyle T} is air temperature, L v {\displaystyle L_{v}} is the latent heat of vaporization, and q {\displaystyle q}

1005-612: A tropical cyclone than regions with relatively cold water. However, this relationship is indirect via the large-scale dynamics of the tropics; the direct influence of the absolute sea surface temperature on v p {\displaystyle v_{p}} is weak in comparison. An empirical limit on tropical cyclone intensity can also be computed using the following formula: V = A + B ⋅ e C ( T − T 0 ) {\displaystyle V=A+B\cdot e^{C(T-T_{0})}} Where V {\displaystyle V}

1072-529: A worldwide scale, May is the least active month, while September is the most active. In the North Atlantic, a distinct hurricane season occurs from June 1 through November 30, sharply peaking from late August through October. 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

1139-413: Is dominant) leads to the solution for v p {\displaystyle v_{p}} given above. This derivation assumes that total energy input and loss within the system can be approximated by their values at the radius of maximum wind. The inclusion of Q i n : f r i c t i o n {\displaystyle Q_{in:friction}} acts to multiply

1206-405: Is due predominantly to the variability in the surface-air enthalpy difference component Δ k {\displaystyle \Delta k} . A tropical cyclone may be viewed as a heat engine that converts input heat energy from the surface into mechanical energy that can be used to do mechanical work against surface friction. At equilibrium, the rate of net energy production in

1273-508: Is given by where T s {\displaystyle T_{s}} is the temperature of the sea surface, T o {\displaystyle T_{o}} is the temperature of the outflow ([K]), Δ k {\displaystyle \Delta k} is the enthalpy difference between the surface and the overlying air ([J/kg]), and C k {\displaystyle C_{k}} and C d {\displaystyle C_{d}} are

1340-430: Is given by where Δ k = k s ∗ − k {\displaystyle \Delta k=k_{s}^{*}-k} represents the enthalpy difference between the ocean surface and the overlying air. The second source is the internal sensible heat generated from frictional dissipation (equal to W o u t {\displaystyle W_{out}} ), which occurs near

1407-428: Is primarily due to variability in the surface enthalpy disequilibrium ( Δ k {\displaystyle \Delta k} ) as well as in the thermodynamic structure of the troposphere, which are controlled by the large-scale dynamics of the tropical climate. These processes are modulated by factors including the sea surface temperature (and underlying ocean dynamics), background near-surface wind speed, and

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1474-407: 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

1541-475: 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. 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

1608-535: Is strongly related to the water temperatures along its path. An average of 86 tropical cyclones of tropical storm intensity form annually worldwide. Of those, 47 reach strength higher than 74 mph (119 km/h), and 20 become intense tropical cyclones (at least Category 3 intensity on the Saffir–Simpson scale ). There are six main requirements for tropical cyclogenesis: sufficiently warm sea surface temperatures, atmospheric instability, high humidity in

1675-494: Is the CAPE of the boundary layer air, and both quantities are calculated at the radius of maximum wind. On Earth, a characteristic temperature for T s {\displaystyle T_{s}} is 300 K and for T o {\displaystyle T_{o}} is 200 K, corresponding to a Carnot efficiency of ϵ = 1 / 3 {\displaystyle \epsilon =1/3} . The ratio of

1742-414: Is the concentration of water vapor. The first component corresponds to sensible heat and the second to latent heat . There are two sources of heat input. The dominant source is the input of heat at the surface, primarily due to evaporation. The bulk aerodynamic formula for the rate of heat input per unit area at the surface, Q i n : k {\displaystyle Q_{in:k}} ,

1809-467: Is the enthalpy of boundary layer air overlying the surface. The maximum potential intensity is predominantly a function of the background environment alone (i.e. without a tropical cyclone), and thus this quantity can be used to determine which regions on Earth can support tropical cyclones of a given intensity, and how these regions may evolve in time. Specifically, the maximum potential intensity has three components, but its variability in space and time

1876-663: Is the maximum potential velocity in meters per second ; T {\displaystyle T} is the sea surface temperature underneath the center of the tropical cyclone, T 0 {\displaystyle T_{0}} is a reference temperature (30 ˚C ) and A {\displaystyle A} , B {\displaystyle B} and C {\displaystyle C} are curve-fit constants. When A = 28.2 {\displaystyle A=28.2} , B = 55.8 {\displaystyle B=55.8} , and C = 0.1813 {\displaystyle C=0.1813} ,

1943-430: Is the near surface wind speed ([m/s]). The rate of energy production per unit surface area, W i n {\displaystyle W_{in}} is given by where ϵ {\displaystyle \epsilon } is the heat engine efficiency and Q i n {\displaystyle Q_{in}} is the total rate of heat input into the system per unit surface area. Given that

2010-601: 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 Pablo in 2019 , Alex in 2004 , Alberto in 1988 , and the 1975 Pacific Northwest hurricane , 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

2077-649: The Mediterranean Sea . Notable examples of these " Mediterranean tropical cyclones " include an unnamed system in September 1969, Leucosia in 1982, Celeno in 1995, Cornelia in 1996, Querida in 2006, Rolf in 2011, Qendresa in 2014, Numa in 2017, Ianos in 2020, and Daniel in 2023. However, there is debate on whether these storms were tropical in nature. 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

Main development region - Misplaced Pages Continue

2144-567: The North American Atlantic coast . During the quiescent periods (3000–1400 BC, and 1000 AD to present), a more northeasterly position of the Azores High would result in more hurricanes being steered towards the Atlantic coast. During the hyperactive period (1400 BC to 1000 AD), more hurricanes were steered towards the Gulf coast as the Azores High was shifted to a more southwesterly position near

2211-550: The equator (about 4.5 degrees from the equator) is normally needed for tropical cyclogenesis. 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 ) and

2278-402: 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,

2345-625: The Azores High hypothesis. A 3,000-year proxy record from a coastal lake in Cape Cod suggests that hurricane activity has increased significantly during the past 500–1,000 years, just as the Gulf coast was amid a quiescent period of the last millennium. Tropical cyclogenesis Tropical cyclogenesis is the development and strengthening of a tropical cyclone in the atmosphere . The mechanisms through which tropical cyclogenesis occur are distinctly different from those through which temperate cyclogenesis occurs. Tropical cyclogenesis involves

2412-626: The Caribbean. Such a displacement of the Azores High is consistent with paleoclimatic evidence that shows an abrupt onset of a drier climate in Haiti around 3200 years ago, and a change towards more humid conditions in the Great Plains during the late- Holocene as more moisture was pumped up the Mississippi Valley through the Gulf coast. Preliminary data from the northern Atlantic coast seem to support

2479-644: The Chilean coast in January 2022, named Humberto by researchers. Vortices have been reported off the coast of Morocco in the past. However, it is debatable if they are truly tropical in character. 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 September 1996 over Lake Huron . The system developed an eye -like structure in its center, and it may have briefly been

2546-623: The Mediterranean. Two of these storms reached tropical storm and subtropical storm intensity in August 2002 and September 2005 respectively. 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, Cyclone Yaku in March 2023 is the only known instance of

2613-720: 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. 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. Tropical cyclogenesis in

2680-513: The Northwestern Pacific is suppressed west of 150°E in the year following an El Niño event. 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. There is an inverse relationship between tropical cyclone activity in

2747-633: 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. Since 1984, Colorado State University has been issuing seasonal tropical cyclone forecasts for the north Atlantic basin, with results that they claim are better than climatology. The university claims to have found several statistical relationships for this basin that appear to allow long range prediction of

Main development region - Misplaced Pages Continue

2814-626: The South Atlantic to support tropical activity. At least six tropical cyclones have been observed here, including a weak tropical storm in 1991 off the coast of Africa near Angola , Hurricane Catarina in March 2004, which made landfall in Brazil at Category 2 strength , Tropical Storm Anita in March 2010, Tropical Storm Iba in March 2019, Tropical Storm 01Q in February 2021, and Tropical Storm Akará in February 2024. Storms that appear similar to tropical cyclones in structure sometimes occur in

2881-496: 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 wet-bulb 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

2948-428: The cost of a peak in intensity with much weaker wind speeds and higher minimum pressure . 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

3015-561: The developing tropical disturbance/cyclone. 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. Worldwide, tropical cyclone activity peaks in late summer when water temperatures are warmest. Each basin, however, has its own seasonal patterns. On

3082-403: The development of a warm-core cyclone, due to significant convection in a favorable atmospheric environment. 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 ,

3149-463: The effect of sea spray on evaporation within the boundary layer. A characteristic value of the maximum potential intensity, v p {\displaystyle v_{p}} , is 80 metres per second (180 mph; 290 km/h). However, this quantity varies significantly across space and time, particularly within the seasonal cycle , spanning a range of 0 to 100 metres per second (0 to 224 mph; 0 to 360 km/h). This variability

3216-403: 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 . While these conditions are necessary for tropical cyclone formation, they do not guarantee that a tropical cyclone will form. Normally, an ocean temperature of 26.5 °C (79.7 °F) spanning through at least

3283-530: The maximum potential intensity, which is mathematically equivalent to the above formulation, is where CAPE stands for the Convective Available Potential Energy , C A P E s ∗ {\displaystyle CAPE_{s}^{*}} is the CAPE of an air parcel lifted from saturation at sea level in reference to the environmental sounding , C A P E b {\displaystyle CAPE_{b}}

3350-563: 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 diminish to allow tropical cyclogenesis to continue. Limited vertical wind shear can be positive for tropical cyclone formation. When an upper-level trough or upper-level low

3417-762: The number of tropical cyclones. Since then, numerous others have issued seasonal forecasts for worldwide basins. 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). Maximum potential intensity The maximum potential intensity of

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3484-485: 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

3551-492: 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

3618-455: The sea the size of the hurricane, which has cooler waters, which can be 5–10 °C (9.0–18.0 °F) lower than before the hurricane. When a new hurricane moves over the cooler waters they have no fuel to continue to thrive, so they weaken or dissipate. According to an Azores High hypothesis of geographer Kam-biu Liu, an anti-phase pattern is expected to exist between the Gulf of Mexico coast and

3685-410: 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. Strong wind shear can "blow" the tropical cyclone apart, as it displaces the mid-level warm core from the surface circulation and dries out

3752-497: The surface exchange coefficients ( dimensionless ) of enthalpy and momentum, respectively. The surface-air enthalpy difference is taken as Δ k = k s ∗ − k {\displaystyle \Delta k=k_{s}^{*}-k} , where k s ∗ {\displaystyle k_{s}^{*}} is the saturation enthalpy of air at sea surface temperature and sea-level pressure and k {\displaystyle k}

3819-501: The surface exchange coefficients, C k / C d {\displaystyle C_{k}/C_{d}} , is typically taken to be 1. However, observations suggest that the drag coefficient C d {\displaystyle C_{d}} varies with wind speed and may decrease at high wind speeds within the boundary layer of a mature hurricane. Additionally, C k {\displaystyle C_{k}} may vary at high wind speeds due to

3886-423: The surface within the tropical cyclone and is recycled to the system. Thus, the total rate of net energy production per unit surface area is given by Setting W i n = W o u t {\displaystyle W_{in}=W_{out}} and taking | u | ≈ v {\displaystyle |\mathbf {u} |\approx v} (i.e. the rotational wind speed

3953-443: The system must equal the rate of energy loss due to frictional dissipation at the surface, i.e. The rate of energy loss per unit surface area from surface friction, W o u t {\displaystyle W_{out}} , is given by where ρ {\displaystyle \rho } is the density of near-surface air ([kg/m ]) and | u | {\displaystyle |\mathbf {u} |}

4020-409: The temperatures are too cool. The waters are only at the necessary temperatures from July until mid-October. In the Atlantic this is the height of the season . Since hurricanes rely on sea surface temperature, sometimes an initially active season becomes quiet later. This is because the hurricanes are so strong that they churn the waters and bring colder waters up from the deep. This creates an area of

4087-403: The total heat input rate by the factor T s T o {\displaystyle {\frac {T_{s}}{T_{o}}}} . Mathematically, this has the effect of replacing T s {\displaystyle T_{s}} with T o {\displaystyle T_{o}} in the denominator of the Carnot efficiency. An alternative definition for

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4154-431: The transition period. Areas within approximately ten degrees latitude of the equator do not experience a significant Coriolis force , a vital ingredient in tropical cyclone formation. However, a few tropical cyclones have been observed forming within five degrees of the equator. A combination of wind shear and a lack of tropical disturbances from the Intertropical Convergence Zone (ITCZ) makes it very difficult for

4221-510: 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 . A minimum distance of 500 km (310 mi) from

4288-407: The vertical structure of atmospheric radiative heating. The nature of this modulation is complex, particularly on climate time-scales (decades or longer). On shorter time-scales, variability in the maximum potential intensity is commonly linked to sea surface temperature perturbations from the tropical mean, as regions with relatively warm water have thermodynamic states much more capable of sustaining

4355-404: The vortex if other development factors are neutral. Whether it be a depression in the Intertropical Convergence 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. Even with perfect upper-level conditions and the required atmospheric instability, the lack of

4422-540: The western North Pacific typhoon region. Tropical cyclones in the northeastern Pacific and north Atlantic basins are both generated in large part by tropical waves from the same wave train. 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). Coupled with an increase in activity in

4489-418: 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. Research has shown that trapped equatorial Rossby wave packets can increase the likelihood of tropical cyclogenesis in

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