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ones that experience rapid intensification are traversing regions of high ocean heat content rather than lower values 64 high ocean heat content values can help to offset the oceanic cooling caused by the passage of a tropical cyclone limiting the effect this cooling has on the storm 65 faster moving systems are able to intensify to higher intensities with lower ocean heat content values slower moving systems require higher values of ocean heat content to achieve the same intensity 64 the passage of a tropical cyclone over the ocean causes the upper layers of the ocean to cool substantially a process known as upwelling 66 which can negatively influence subsequent cyclone development this cooling is primarily caused by wind driven mixing of cold water from deeper in the ocean with the warm surface waters this effect results in a negative feedback process that can inhibit further development or lead to weakening additional cooling may come in the form of cold water from falling raindrops this is because the atmosphere is cooler at higher altitudes cloud cover may also play a role in cooling the ocean by shielding the ocean surface from direct sunlight before and slightly after the storm passage all these effects can combine to produce a dramatic drop in sea surface temperature over a large area in just a few days 67 conversely the mixing of the sea can result in heat being inserted in deeper waters with potential effects on global climate 68 vertical wind shear decreases tropical cyclone predicability with storms exhibiting wide range of responses in the presence of shear 69 wind shear often negatively affects tropical cyclone intensification by displacing moisture and heat from a system s center 70 low levels of vertical wind shear are most optimal for strengthening while stronger wind shear induces weakening 71 72 dry air entraining into a tropical cyclone s core has a negative effect on its development and intensity by diminishing atmospheric convection and introducing asymmetries in the storm s structure 73 74 75 symmetric strong outflow leads to a faster rate of intensification than observed in other systems by mitigating local wind shear 76 77 78 weakening outflow is associated with the weakening of rainbands within a tropical cyclone 79 tropical cyclones may still intensify even rapidly in the presence of moderate or strong wind shear depending on the evolution and structure of the storm s convection 80 81 the size of tropical cyclones plays a role in how quickly they intensify smaller tropical cyclones are more prone to rapid intensification than larger ones 82 the fujiwhara effect which involves interaction between two tropical cyclones can weaken and ultimately result in the dissipation of the weaker of two tropical cyclones by reducing the organization of the system s convection and imparting horizontal wind shear 83 tropical cyclones typically weaken while situated over a landmass because conditions are often unfavorable as a result of the lack of oceanic forcing 84 the brown ocean effect can allow a tropical cyclone to maintain or increase its intensity following landfall in cases where there has been copious rainfall through the release of latent heat from the saturated soil 85 orographic lift can cause a significant increase in the intensity of the convection of a tropical cyclone when its eye moves over a mountain breaking the capped boundary layer that had been restraining it 86 jet streams can both enhance and inhibit tropical cyclone intensity by influencing the storm s outflow as well as vertical wind shear 87 88 rapid intensification main article rapid intensification on occasion tropical cyclones may undergo a process known as rapid intensification a period in which the maximum sustained winds of a tropical cyclone increase by 30 kn 56 km h 35 mph or more within 24 hours 89 similarly rapid deepening in tropical cyclones is defined as a minimum sea surface pressure decrease of 1 75 hpa 0 052 inhg per hour or 42 hpa 1 2 inhg within a 24 hour period explosive deepening occurs when the surface pressure decreases by 2 5 hpa 0 074 inhg per hour for at least 12 hours or 5 hpa 0 15 inhg per hour for at least 6 hours 90 for rapid intensification to occur several conditions must be in place water temperatures must be extremely high near or above 30 c 86 f and water of this temperature must be sufficiently deep such that waves do not upwell cooler waters to the surface on the other hand tropical cyclone heat potential is one of such non conventional subsurface oceanographic parameters influencing the cyclone intensity 91 wind shear must be low when wind shear is high the convection and circulation in the cyclone will be disrupted usually an anticyclone in the upper layers of the troposphere above the storm must be present as well for extremely low surface pressures to develop air must be rising very rapidly in the eyewall of the storm and an upper level anticyclone helps channel this air away from the cyclone efficiently 91 however some cyclones such as hurricane epsilon in 2020 have rapidly intensified despite relatively unfavorable conditions 92 93 dissipation hurricane paulette in 2020 is an example of a sheared tropical cyclone with deep convection slightly removed from the center of the system there are a number of ways a tropical cyclone can weaken dissipate or lose its tropical characteristics these include making landfall moving over cooler water encountering dry air or interacting with other weather systems however once a system has dissipated or lost its tropical characteristics its remnants could regenerate a tropical cyclone if environmental conditions become favorable 94 95 a tropical cyclone can dissipate when it moves over waters significantly cooler than 26 5 c 79 7 f this will deprive the storm of such tropical characteristics as a warm core with thunderstorms near the center so that it becomes a remnant low pressure area remnant systems may persist for several days before losing their identity this dissipation mechanism is most common in the eastern north pacific weakening or dissipation can also occur if a storm experiences vertical wind shear which causes the convection and heat engine to move away from the center this normally ceases the development of a tropical cyclone 96 in addition its interaction with the main belt of the westerlies by means of merging with a nearby frontal zone can cause tropical cyclones to evolve into extratropical cyclones this transition can take 1 3 days 97 should a tropical cyclone make landfall or pass over an island its circulation could start to break down especially if it encounters mountainous terrain 98 when a system makes landfall on a large landmass it is cut off from its supply of warm moist maritime air and starts to draw in dry continental air 98 this combined with the increased friction over land areas leads to the weakening and dissipation of the tropical cyclone 98 over a mountainous terrain a system can quickly weaken over flat areas it may endure for two to three days before circulation breaks down and dissipates 98 over the years there have been a number of techniques considered to try to artificially modify tropical cyclones 99 these techniques have included using nuclear weapons cooling the ocean with icebergs blowing the storm away from land with giant fans and seeding selected storms with dry ice or silver iodide 99 these techniques however fail to appreciate the duration intensity power or size of tropical cyclones 99 assessment methods for broader coverage of this topic see dvorak technique and scatterometer a variety of methods or techniques including surface satellite and aerial are used to assess the intensity of a tropical cyclone reconnaissance aircraft fly around and through tropical cyclones outfitted with specialized instruments to collect information that can be used to ascertain the winds and pressure of a system 1 tropical cyclones possess winds of different speeds at different heights winds recorded at flight level can be converted to find the wind speeds at the surface 100 surface observations such as ship reports land stations mesonets coastal stations and buoys can provide information on a tropical cyclone s intensity or the direction it is traveling 1 wind pressure relationships wprs are used as a way to determine the pressure of a storm based on its wind speed several different methods and equations have been proposed to calculate wprs 101 102 tropical cyclones agencies each use their own fixed wpr which can result in inaccuracies between agencies that are issuing estimates on the same system 102 the ascat is a scatterometer used by the metop satellites to map the wind field vectors of tropical cyclones 1 the smap uses an l band radiometer channel to determine the wind speeds of tropical cyclones at the ocean surface and has been shown to be reliable at higher intensities and under heavy rainfall conditions unlike scatterometer based and other radiometer based instruments 103 the dvorak technique plays a large role in both the classification of a tropical cyclone and the determination of its intensity used in warning centers the method was developed by vernon dvorak in the 1970s and uses both visible and infrared satellite imagery in the assessment of tropical cyclone intensity the dvorak technique uses a scale of t numbers scaling in increments of 0 5 from t1 0 to t8 0 each t number has an intensity assigned to it with larger t numbers indicating a stronger system tropical cyclones are assessed by forecasters according to an array of patterns including curved banding features shear central dense overcast and eye to determine the t number and thus assess the intensity of the storm 104 the cooperative institute for meteorological satellite studies works to develop and improve automated satellite methods such as the advanced dvorak technique adt and satcon the adt used by a large number of forecasting centers uses infrared geostationary satellite imagery and an algorithm based upon the dvorak technique to assess the intensity of tropical cyclones the adt has a number of differences from the conventional dvorak technique including changes to intensity constraint rules and the usage of microwave imagery to base a system s intensity upon its internal structure which prevents the intensity from leveling off before an eye emerges in infrared imagery 105 the satcon weights estimates from various satellite based systems and microwave sounders accounting for the strengths and flaws in each individual estimate to produce a consensus estimate of a tropical cyclone s intensity which can be more reliable than the dvorak technique at times 106 107 intensity metrics multiple intensity metrics are used including accumulated cyclone energy ace the hurricane surge index the hurricane severity index the power dissipation index pdi and integrated kinetic energy ike ace is a metric of the total energy a system has exerted over its lifespan ace is calculated by summing the squares of a cyclone s sustained wind speed every six hours as long as the system is at or above tropical storm intensity and either tropical or subtropical 108 the calculation of the pdi is similar in nature to ace with the major difference being that wind speeds are cubed rather than squared 109 the hurricane surge index is a metric of the potential damage a storm may inflict via storm surge it is calculated by squaring the dividend of the storm s wind speed and a climatological value 33 m s or 74 mph and then multiplying that quantity by the dividend of the radius of hurricane force winds and its climatological value 96 6 km or 60 0 mi this can be represented in equation form as v 33 m s 2 r 96 6 k m displaystyle left frac v 33 mathrm m s right 2 times left frac r 96 6 mathrm km right where v textstyle v is the storm s wind speed and r textstyle r is the radius of hurricane force winds 110 the hurricane severity index is a scale that can assign up to 50 points to a system up to 25 points come from intensity while the other 25 come from the size of the storm s wind field 111 the ike model measures the destructive capability of a tropical cyclone via winds waves and surge it is calculated as v o l 1 2 p u 2 d v displaystyle int _ vol frac 1 2 pu 2 d_ v where p textstyle p is the density of air u textstyle u is a sustained surface wind speed value and d v textstyle d_ v is the volume element 111 112 classification and naming terminology for tropical cyclones on a world map classification main article tropical cyclone scales three tropical cyclones of the 2006 pacific typhoon season at different stages of development the weakest left demonstrates only the most basic circular shape a stronger storm top right demonstrates spiral banding and increased centralization while the strongest lower right has developed an eye around the world tropical cyclones are classified in different ways based on the location tropical cyclone basins the structure of the system and its intensity for example within the northern atlantic and eastern pacific basins a tropical cyclone with wind speeds of over 65 kn 120 km h 75 mph is called a hurricane while it is called a typhoon or a severe cyclonic storm within the western pacific or north indian oceans 19 20 21 when a hurricane passes west across the international dateline in the northern hemisphere it becomes known as a typhoon this happened in 2014 for hurricane genevieve which became typhoon genevieve 113 within the southern hemisphere it is either called a hurricane tropical cyclone or a severe tropical cyclone depending on if it is located within the south atlantic south west indian ocean australian region or the south pacific ocean 22 23 the descriptors for tropical cyclones with wind speeds below 65 kn 120 km h 75 mph vary by tropical cyclone basin and may be further subdivided into categories such as tropical storm cyclonic storm tropical depression or deep depression 20 21 19 naming main articles tropical cyclone naming and history of tropical cyclone naming the practice of using given names to identify tropical cyclones dates back to the late 1800s and early 1900s and gradually superseded the existing system simply naming cyclones based on what they hit 114 115 the system currently used provides positive identification of severe weather systems in a brief form that is readily understood and recognized by the public 114 115 the credit for the first usage of personal names for weather systems is generally given to the queensland government meteorologist clement wragge who named systems between 1887 and 1907 114 115 this system of naming weather systems fell into disuse for several years after wragge retired until it was revived in the latter part of world war ii for the western pacific 114 115 formal naming schemes have subsequently been introduced for the north and south atlantic eastern central western and southern pacific basins as...
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