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Paleotempestology is the study of past tropical cyclone activity by means of geological proxies as well as historical documentary records. The term was coined by Kerry Emanuel.
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".
Kerry Andrew Emanuel is an American professor of meteorology currently working at the Massachusetts Institute of Technology in Cambridge. In particular he has specialized in atmospheric convection and the mechanisms acting to intensify hurricanes. He was named one of the Time 100 influential people of 2006. In 2007, he was elected as a member of the U.S. National Academy of Sciences. He was elected a Member of the American Philosophical Society in 2019.
Paleotempestology usually tries to identify leftover deposits from past storms, such as overwash deposits in waterbodies close to the coast which is the most commonly applied techniques, oxygen isotope ratio variations caused by tropical cyclone rainfall in trees or speleothems and beach ridges kicked up by storm waves. From these deposits one can then infer the occurrence rate of tropical cyclones - typically the stronger events are the most easily recognizable ones - and sometimes also their intensity, by comparing them to deposits left by historical events.
Overwash is the flow of water and sediment over a coastal dune or beach crest during storm events. 'Overwash' may refer only to the landward flux of water due to overtopping of a dune system while 'washover' may refer to the sediment deposited by overwash. A common process on barrier islands, Overwash redistributes sediment and facilitates the migration of barrier islands in response to sea level rise. Overwash can occur as a result of runup, or inundation.
Speleothems, commonly known as cave formations, are secondary mineral deposits formed in a cave. Speleothems typically form in limestone or dolomite solutional caves. The term "speleothem" as first introduced by Moore (1952), is derived from the Greek words spēlaion "cave" + théma "deposit". The definition of "speleothem" in most publications, specifically excludes secondary mineral deposits in mines, tunnels and on man-made structures. Hill and Forti more concisely defined "secondary minerals" which create speleothems in caves as;
A "secondary" mineral is one which is derived by a physicochemical reaction from a primary mineral in bedrock or detritus, and/or deposited because of a unique set of conditions in a cave; i.e., the cave environment has influenced the mineral's deposition.
A beach ridge is a wave-swept or wave-deposited ridge running parallel to a shoreline. It is commonly composed of sand as well as sediment worked from underlying beach material. The movement of sediment by wave action is called littoral transport. Movement of material parallel to the shoreline is called longshore transport. Movement perpendicular to the shore is called on-offshore transport. A beach ridge may be capped by, or associated with, sand dunes. The height of a beach ridge is affected by wave size and energy.
While the findings are prone to confounding factors and only some parts of the world have been investigated, some important findings have been made with the help of paleotempestology. For example, in the Gulf Coast and in Australia the occurrence rate of intense tropical cyclones is about once every few centuries, and there are long-term variations in occurrence which are caused e.g. by shifts in their paths.
Paleotempestology is the estimation of tropical cyclone activity with the help of proxy data. The name was coined by Kerry Emanuel of the Massachusetts Institute of Technology;the field has seen increased activity since the 1990s and studies were first carried out in the United States of America on the East Coast.
In the study of past climates ("paleoclimatology"), climate proxies are preserved physical characteristics of the past that stand in for direct meteorological measurements and enable scientists to reconstruct the climatic conditions over a longer fraction of the Earth's history. Reliable global records of climate only began in the 1880s, and proxies provide the only means for scientists to determine climatic patterns before record-keeping began.
The Massachusetts Institute of Technology (MIT) is a private research university in Cambridge, Massachusetts. Founded in 1861 in response to the increasing industrialization of the United States, MIT adopted a European polytechnic university model and stressed laboratory instruction in applied science and engineering. It has since played a key role in the development of many aspects of modern science, engineering, and mathematics, and is widely known for its innovation and academic strength, making it one of the most prestigious institutions of higher learning in the world. The Institute is a land-grant, sea-grant, and space-grant university, with an urban campus that extends more than a mile alongside the Charles River.
The East Coast of the United States, also known as the Eastern Seaboard, the Atlantic Coast, and the Atlantic Seaboard, is the coastline along which the Eastern United States meets the North Atlantic Ocean. The coastal states that have shoreline on the Atlantic Ocean are, from north to south, Maine, New Hampshire, Massachusetts, Rhode Island, Connecticut, New York, New Jersey, Delaware, Maryland, Virginia, North Carolina, South Carolina, Georgia, and Florida.
Tropical cyclones - known depending on location as cyclones, hurricanes or typhoons- with their precipitation, storm surges and winds are highly destructive and deadly phenomena; the 1900 Galveston hurricane claimed over 8,000 fatalities and was the worst natural disaster in United States history, while Hurricane Katrina in 2005 became the costliest hurricane in United States history with over 80 billion dollars damage and over 1600 fatalities. In other parts of the world, a 1970 cyclone killed 300,000 in Bangladesh; Japan in 2004 was hit by 10 typhoons and in 2005 five separate cyclones hit the Cook Islands in a short timeframe; a year later records were broken by Typhoon Saomai in China and Cyclone Larry in Australia. Finally, in 2013 Typhoon Haiyan became one of the most intense tropical cyclones ever recorded and caused 6,000 fatalities in the Philippines. Further, increased coastal development in general and in the United States rapid population growth along hurricane-prone coasts is creating additional attention to the danger posed by tropical cyclones and the interest in the hazard existing for major cities like Miami and New Orleans. Tropical cyclones can also have positive effects on society, for example by bringing rain to drought-prone regions. Finally, there is increasing evidence that tropical cyclone influence the climate themselves by enhancing poleward heat transport.
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.
A storm surge, storm flood, tidal surge or storm tide is a coastal flood or tsunami-like phenomenon of rising water commonly associated with low pressure weather systems, the severity of which is affected by the shallowness and orientation of the water body relative to storm path, as well as the timing of tides. Most casualties during tropical cyclones occur as the result of storm surges. It is a measure of the rise of water beyond what would be expected by the normal movement related to tides.
Wind is the flow of gases on a large scale. On the surface of the Earth, wind consists of the bulk movement of air. In outer space, solar wind is the movement of gases or charged particles from the Sun through space, while planetary wind is the outgassing of light chemical elements from a planet's atmosphere into space. Winds are commonly classified by their spatial scale, their speed, the types of forces that cause them, the regions in which they occur, and their effect. The strongest observed winds on a planet in the Solar System occur on Neptune and Saturn. Winds have various aspects, an important one being its velocity ; another the density of the gas involved; another its energy content or wind energy. Wind is also a great source of transportation for seeds and small birds; with time things can travel thousands of miles in the wind.
The historical record in many places is too short (one century at most) to properly determine the hazard produced by tropical cyclones, especially the rare very intense oneswhich at times are undersampled by historical records; in the United States for example only about 150 years of record are available and only a small number of hurricanes classified as category 4 or 5 - the most destructive ones in the Saffir-Simpson scale - have come ashore, making it difficult to estimate the hazard level, and elsewhere the record often goes back less than half a century. Such records may also not be representative for future climates. The realization that one cannot rely solely on historical records to infer past storm activity was a major driving force for the development of paleotempestology.
Information about past tropical cyclone occurrences can be used to constrain how their occurrences may change in the future or about how they respond to large-scale climate modes such as sea surface temperature changes.In general, the origin and behaviour of tropical cyclone systems is poorly understood and there is concern that man-made global warming will increase the intensity of tropical cyclones and the frequency of strong events by increasing sea surface temperatures.
In general, paleotempestology is a complex field of science that overlaps with other disciplines like climatology and coastal geomorphology.A number of techniques have been used to estimate the past hazards from tropical cyclones. Many of these techniques have also been applied to studying extratropical storms, although research on this field is less advanced than on tropical cyclones.
Overwash deposits in atolls, coastal lakes, marshes or reef flats are the most important paleoclimatological evidence of tropical cyclone strikes; when storms hit these areas currents and waves can overtop barriers, erode these and other beach structures and lay down deposits in the water bodies behind barriers.Isolated breaches and especially widespread overtopping of coastal barriers during storms can generate fan-like, layered deposits behind the barrier. Individual layers can be correlated to particular storms in favourable circumstances; in addition they are often separated by a clear boundary from earlier sediments. Such deposits have been observed in North Carolina after Hurricane Isabel in 2003, for example.
Several techniques have been applied to separate out storm overwash deposits from other sediments:
The position of the research site vis-a-vis the storm path is an important factor in determining the usefulness of the record,which is also influenced by the geography of the analysis site such as e.g. vegetation cover. Prerequisites for successful correlation of overwash deposits to tropical cyclones are:
Various dating techniques can then be used to produce a chronology of tropical cyclone strikes at a given location and thus a recurrence rate; 54 metres per second (120 mph) -73 metres per second (160 mph).for example, at Lake Shelby in Alabama a return period of once every 318 years was determined for storms with windspeeds of over
The intensityand impacts of the tropical cyclone can also be inferred from overwash deposits by comparing the deposits to these formed by known storms and analyzing their lithology. Additionally, thicker sediment layers usually correspond to stronger storm systems. This procedure is not always clear-cut however.
For dating purposes radiometric dating procedures involving carbon-14, cesium-137 and lead-210 are most commonly used, often in combination,although uranium series dating, optically stimulated luminescence and correlations to humans land use can also be used in some places.
Beach ridges and cheniersform when storm surges, storm waves or tides deposit debris in ridges, with one ridge typically corresponding to one storm. Ridges can be formed by coral rubble where the coast coincides with coral reefs and can contain complicated layer structures, shells, pumice and gravel. A known example is the ridge that Cyclone Bebe generated on Funafuti atoll in 1971.
Beach ridges are common on the deltaic shores of China and are indicative of increased typhoon activity.They have also been found on the Australian coast facing the Great Barrier Reef and are formed from reworked corals. The height of each ridge appears to correlate with the intensity of the storm that produced it and thus the intensity of the forming storm can be inferred by numerical modelling and comparison to known storms and known storm surges. Ridges become older the farther inland they are; they can also be dated through optically stimulated luminescence and radiocarbon dating. In addition, no tsunami-generated beach ridges have been observed, and tsunamis are important confounding factors in paleotempestology.
However, wind-driven erosion or accumulation can alter the elevation of such ridges, and in addition the same ridge can be formed by more than one storm eventas has been observed in Australia. Beach ridges can also shift around through non-storm processes after their formation and finally beach ridges can form through non-tropical cyclone processes. Sedimentary texture can be used to infer the origin of a ridge from storm surges.
Precipitation in tropical cyclones has a characteristic isotope composition with a depletion of heavy oxygen isotopes; carbon and nitrogen isotope data have also been used to infer tropical cyclone activity.Corals can store oxygen isotope ratios which in turn reflect water temperatures, precipitation and evaporation; these in turn can be related to tropical cyclone activity. Fish otoliths and bivalves can also store such records, as can trees where the oxygen isotope ratios of precipitation are reflected in the cellulose of trees, and can be inferred with the help of tree rings. However, confounding factors like physiological isotope variations and soil properties also influence oxygen isotope ratios of tree cellulose, which can thus be only used to infer the frequency of storms and not their intensity.
Speleothems, deposits formed in caves through the dissolution and redeposition of dolomite and limestone, can store isotope signatures associated with tropical cyclones, especially in fast growing speleothems, areas with thin soils and speleothems which have undergone little alteration. Such deposits have a high temporal resolution and are also protected from many confounding factorsalthough the extraction of annual layers has become possible only recently, with a two-week resolution (two separate layers correlated to two hurricanes that struck two weeks apart) achieved in one case. However, the suitability of speleothems depends on the characteristics of the cave they are found in; caves that flood frequently may have their speleothems eroded or otherwise damaged, for example, making them less suitable for paleotempestology research. Finally very old records can be obtained from oxygen isotope ratios in rocks.
Historical documents such as county gazzettes in China, diaries, logbooks of travellers, official histories and old newspapers can contain information on tropical cyclones.In China such records go back over a millennium, while elsewhere it is usually confined to the last 130 years. Such historical records however are often ambiguous or unclear. The frequency of shipwrecks has been used to infer past tropical cyclone occurrence, such as has been done with a database of shipwrecks that the Spaniards suffered in the Caribbean.
Aside from oxygen isotope ratios,tree rings can also record information on storm-caused plant damage or vegetation changes such as thin tree rings due to storm-induced damage to a tree canopy and saltwater intrusion and the resulting slowdown in tree growth ("dendrotempestology" ). Speleothems can also store trace elements which can signal tropical cyclone activity and mud layers formed by storm-induced cave flooding. Droughts on the other hand can cause groundwater levels to drop enough that subsequent storms cannot induce flooding and thus fail to leave a record, as has been noted in Yucatan.
A database going back to 8,000 BP has been compiled for the Atlantic Ocean.In the Gulf of Mexico, paleoproxy records go back five millennia but only a few typhoon records go back 5,000 - 6,000 years. In general, tropical cyclone records do not go farther back than 5,000 - 6,000 years ago when the Holocene sea level rise levelled off; tropical cyclone deposits formed during sea level lowstands likely were reworked during sea level rise. Only tentative evidence exists of deposits from the last interglacial. Tempestite deposits and oxygen isotope ratios in much older rocks have also been used to infer the existence of tropical cyclone activity as far back as the Jurassic.
Paleotempestology is a field of science with important practical and social implications.The insurance industry factors in paleotempestological information in risk prediction analysis and when setting insurance rates, and it also funds paleotempestological research. Archeologists, ecologists, forest and water resource managers could also make use of paleotempestology information.
The recurrence rate is an important metric with which one can estimate tropical cyclone risk, and it can be determined by paleotempestological research. In the Gulf of Mexico, catastrophic hurricane strikes at given locations occur once about every 350 years in the last 3,800 yearsor about 0.48%-0.39% annual frequency at any given site, while category 3 or more storms occur at a rate of 3.9 - 0.1 category 3 or more storms per century in the northern Gulf of Mexico. Elsewhere, tropical cyclones with intensities of category 4 or more occur about every 350 years in the Pearl River Delta (China), 1 storm every 100–150 years at Funafuti and a similar rate in French Polynesia, 1 category 3 or stronger every 471 years in St. Catherines Island (Georgia), 1 storm every 140-180 years in Nicaragua, 1 intense storm every 200–300 years in the Great Barrier Reef - formerly their recurrence rate was estimated to be one strong event every few millennia - and 1 storm of category 2-4 intensity every 190–270 years at Shark Bay on the other side of Australia. Steady rates have been found for the Gulf of Mexico and the Coral Sea for timespans of several millennia.
However, it has also been found that the occurrence rates of tropical cyclone measured with instrumental data over historical time can be significantly different from the actual occurrent rate. In the past, tropical cyclones were far more frequent in the Great Barrier Reefand the northern Gulf of Mexico than today; in Apalachee Bay, strong storms occur every 40 years, not every 400 years as documented historically. and serious storms in New York occurred twice in 300 years not once every millennium or less. In general, the area of Australia appears to be unusually inactive in recent times by the standards of the past 550–1500 years, and that the historical record underestimates the incidence of strong storms in Northeastern Australia.
Long-term variations of tropical cyclone activity have also been found. The Gulf of Mexico saw increased activity between 3,800 - 1,000 years ago with a fivefold increase of category 4-5 hurricane activity,and activity at St. Catherines Island and Wassaw Island was also higher between 2,000 and 1,100 years ago. This appears to be a stage of increased tropical cyclone activity spanning the region from New York to Puerto Rico, followed by an inactive interval since 1,000 years that also affected the Gulf Coast. The US Atlantic coast and the Caribbean saw low activity between 950 AD and 1700 with a sudden increase around 1700. Such fluctuations appear to mainly concern strong tropical cyclone systems, at least in the Atlantic; weaker systems have a more steady pattern of activity. Rapid fluctuations over short timespans have also been observed.
In the Atlantic Ocean, the so-called "Bermuda High" hypothesis stipulates that changes in the position of this anticyclone can cause storm paths to alternate between landfalls on the East Coast and the Gulf Coastbut also Nicaragua. Paleotempestological data support this theory although additional findings on Long Island and Puerto Rico have demonstrated some complexity in the patterns as active periods appear to correlate between the three sites. A southward shift of the High has been inferred to have occurred 3,000 -1,000 years ago; furthermore a tendency to a more northerly storm track may be associated with a strong North Atlantic Oscillation. A north-south anti-correlation has also been found in West Asia between the South China Sea and Japan.
The influence of natural trends on tropical cyclone activity has been recognized in paleotempestology records, such as correlation of Atlantic hurricane tracksand activity with the status of the ITCZ, position of the Loop Current (for Gulf of Mexico hurricanes), North Atlantic Oscillation, sea surface temperatures and the strength of the West African Monsoon, and correlation between Australian cyclone activity and the Pacific Decadal Oscillation. Increased insolation - either from solar activity or from orbital variations - have been found to be detrimental to tropical cyclone activity in some regions. In the early Common Era, warmer sea surface temperatures in the Atlantic as well as more restricted anomalies may be responsible for stronger regional hurricane activity.
Among the known climate modes that influence tropical cyclone activity in paleotempestological records are ENSO phase variations, which influence tropical cyclone activity in Australia and the Atlanticbut also their path as has been noted for typhoons. More general global correlations have been found, such as anticorrelation between tropical cyclone activity in Japan and the North Atlantic and correlation between the Atlantic and Australia on the one hand and between Australia and French Polynesia on the other hand.
The effect of general climate variations have also been found. Hurricaneand typhoon tracks tend to shift north (e.g. Amur Bay) during warm periods and south (e.g. South China) during cold periods, patterns that might be mediated by shifts in the subtropical anticyclones. Such a behaviour (northward shift) has been observed as a consequence of man-made global warming and the end of the Little Ice Age but also after volcanic eruptions (southward shift).
During the last 600 years in the Little Ice Age, there were more but weaker storms in the Gulf of Mexicowhile hurricane activity did not decrease in western Long Island. Increased hurricane activity during the last 300 years in the Caribbean may also correlate to the Little Ice Age.
The response of tropical cyclone to future global warming is of great interest. The Holocene Climatic Optimum did not induce increased tropical cyclone strikes in Queensland and phases of higher hurricane activity on the Gulf Coast are not associated with global warming;however warming has been correlated with typhoon activity in the Gulf of Thailand and marine warming with typhoon activity in the South China Sea, increased hurricane activity in Belize (which increased during the Medieval Warm Period) and during the Mesozoic, when carbon dioxide caused warming episodes.
A correlation between hurricane strikes and subsequent wildfire activityand vegetation changes has been noted in Alabama and Cuba paleotempestological evidence. In St. Catherines Island cultural activity ceased at the time of increased storm activity, and Polynesian expansion across the Pacific may have been aided by decreased tropical cyclone activity. Finally, tropical cyclone induced alteration in oxygen isotope ratios may mask isotope ratio variations caused by other climate phenomena, which may thus be misinterpreted.
On the other hand, the Classic Maya collapse may coincide with, and have been caused by, a decrease in tropical cyclone activity,and tropical cyclones are more important for drought amelioration in the southeastern USA than was appreciated.
Not all of the world has been investigated with paleotempestological methods; among the places thus researched are Belize, the Carolinas of North America, northern coasts of the Gulf of Mexico, the northeastern United States,(in a lesser measure) the Southeastern Pacific islands and tropical Australia. Conversely China, Cuba, Florida, Hispaniola, Honduras, the Lesser Antilles and North America north of Canada are little researched. The frequency of research institutions active in paleotempestology, suitable sites for paleotempestological research and of tropical cyclone landfalls may influence whether a given location is researched or not. In the Atlantic Ocean research has been concentrated on regions where hurricanes are common rather than more marginal areas.
Paleotempestological reconstructions are subject to a number of limitations, including changes in the hydrological properties of the site due to e.g. sea level risewhich increases the sensitivity to weaker storms and "false positives" caused by for example non-tropical cyclone-related floods, sediment winnowing, wind-driven transport, tides, tsunamis, bioturbation and non-tropical storms such as nor'easters or winter storm, the latter of which however usually result in lower surges. In particular, tsunamis are a problem for paleotempestological studies in the Indian and Pacific Ocean; one technique that has been used to differentiate the two is the identification of traces of runoff which occurs during storms but not during tsunamis.
Paleotempestology records mostly record activity during the Holocene as of 2017 [update] there has been little effort in making comprehensive databases of paleotempestological data or in attempting regional reconstructions from local results.and tend to record mainly catastrophic storms as these are the ones most likely to leave evidence. In addition,
Additional problems which have been noted is the fact that paleotempestology records, especially overwash records in marshes, are often short and their geochronology questionable; the often poor documentation of the deposition mechanisms and of which microfossils can be used as proxies for storms.The magnitude of overwash deposits is fundamentally a function of storm surge height, which are not simply a function of storm intensity. Overwash deposits are regulated by the height of the overwashed barrier and there is no expectation that it will remain stable over time; tropical cyclones themselves have been observed eroding such barriers and such barrier height decreases (e.g. through storm erosion or sea level rise) may induce a spurious increase of tropical cyclone deposits over time. Successive overwash deposits can be difficult to distinguish, and they are easily eroded by subsequent storms. Finally, storm deposits can vary strongly even a short distance from the landfall point, and over few tens of metres.
|Place||Country/state||Data sources||Record duration in years before present||Conclusions||Sources||Approximate coordinates|
|Actun Tunichil Muknal||Belize||Oxygen and carbon isotopes in a quickly growing stalagmite||AD 1977 - 2000||Strong correlation of hits by named tropical cyclones with isotope ratio variations|
|Amur Bay||Russia||Sediments from floods||1,800||Low storm activity in the last 500 years, probably correlated to the Little Ice Age but continuing into the 19th and 20th century|
|Ara River||Japan||River terraces formed by typhoon flooding||11,600||Intense flooding during the late glacial to 5,000 - 4,500 years ago indicate increased typhoon activity, followed by a period of less intense activity until about 2,350 years ago|
|Barbuda||Antigua and Barbuda||Sediments in a coastal lagoon||5,000||Inactive period between 2,500 - 1,500 years, preceded and followed by more active periods|
|Belize, central||Belize||Overwash deposits||500||1.2-1 catastrophic storms per century including one very strong storm before 1500AD|
|Belize, south-central||Belize||Sediments||7,000||Several active periods, between 6,900 - 6,700, 6,050 - 5,750, 5,450 - 4,750, 4,200 - 3,200, 2,600 - 1,450 and 600 - c. 200 years ago|
|Big Pine Key||Florida||Tree ring evidence of storm damage||AD 1700–present||Decreased activity correlated to decreased shipwreck rates in the Maunder Minimum|
|Blackwood Sinkhole||Bahamas||Sand deposits in sinkhole||3,000||A stage without intense storms between 2,900 - 2,500 years ago, followed by an active period that lasted until 1,000 years ago. Two intense events about 500 years ago and an increase between 300 – 100 years ago|
|Brigantine, New Jersey||New Jersey||Sediments||1,500||Two strong storms between 600-700 and 700-1,400 AD; nor'easters are also recorded here|
|Cenote Chaltun Ha||Yucatan||Mud layers in speleothems||CE 365 - 2007||Frequent flooding during the 7th, 9th and 19th century with less common flooding during the 13th and 15-17th centuries. Also, evidence of strong tropical cyclone strikes during the Terminal Classic Maya|
|Commerce Bight Lagoon||Belize||Sediment cores||7,000||Active periods between 600 and 200, 1,450 - 2,600, 3,200 - 4,200, 4,750 - 5,450, 5,750 - 6,050 years ago|
|Charlotte Harbor||Florida||Sediments||8,000||Increased activity between 3,000 - 2,000 years ago and also during El Nino-leaning periods|
|Chenier Plain||Louisiana||Sediments in coastal plain||600||7 hurricanes with category 3 or more intensity are known in the last 600 years, giving a frequency of 1.2 storms per century. Among the storms are Hurricane Audrey and Hurricane Rita|
|Chezzetcook Inlet||Nova Scotia||Sediment analysis||1,000||Potential storm deposits at 1200 AD, AD 1831 and AD 1848, the middle of which is correlated to a major storm; also an inactive phase in the 1950s and 1970s|
|Cowley Beach||Queensland||Beach ridges||5,740||Low activity between 1,820 - 850 and 2,580 - 3,230 years ago|
|Croatan National Forest||North Carolina||Tree rings||AD 1771 - 2014||Low activity in 1815-1875|
|Culebrita||Puerto Rico||Sediment deposits||2,200||Several sand layers may correlate to hurricanes, including one perhaps linked to the 1867 San Narciso hurricane|
|Curacoa Island||Queensland||Beach ridges||6,000||22 hits by intense storms in 6,000 years, implying return periods of 280 years|
|Duri Island||South Korea||Shell-gravel deposits||1,300||Storms in 720 ± 60, 880 ± 110, 950 ± 70, 995 ± 120 and 1535 ± 40, the latter occurring during the Little Ice Age and the others during the Medieval Climate Anomaly|
|Eshaness||British Isles||Boulders perched on cliffs||1,400||Probably not tropical cyclones, but intense storm activity occurred since AD 1950, between 1,300-1,900 AD, 700-1,050 AD and 400 - 550 AD|
|Exmouth Gulf||Australia, northwestern||Washover fans||3,000||Tropical cyclone strikes took place 170 - 180 ± 16, 360 ± 30, 850 - 870 ± 60, 1,290 - 1,300 ± 90, 1,950 - 1,960 ± 90, 2,260 - 2,300 ± 120 and 2,830 - 2,850 ± 120 years ago, consistent with expectations based on sea surface temperature variations|
|Bluefields||Nicaragua||Sediment deposits||5,400||Last 800 years have an active climate with a return period of about 140-180 years, while between 800-2,800 the return period was only once between 600-2,100 years and another quiet period between 4,900 - 5,400 years ago; between 2,800-4,900 no records|
|Folly Island||South Carolina||Back-barrier marshes||4,600||The last 4,600 years may have seen 27 storms, as well as 11 major storms in the last 3,300 years|
|Frankland Islands||Queensland||Coastal ridges and coral mortality||510||Active periods are known from 1980-2000, 1940-1960, 1860-1880, 1800-1830, 1760-1780, 1700–1720, 1630-1650, 1570-1590|
|France||France||Tempestites||Kimmeridgian||Intense tropical cyclone activity from storms coming off the Tethys||Inapplicable|
|Gales Point||Belize||Sediment cores||5,500||In the last 5,500 years 16 major hurricanes|
|Grand Case||St. Martin||Sediments||4,280||Active period between 3,700 - 1,800 years ago, while 1,800 –800 years ago was inactive|
|Great Bahama Bank||Bahamas||Coarse sediment deposits||7,000||Active periods occurred within the last 50 years, between 1,200 and 500 years ago, 2,400 - 1,800 years ago and 4,600 - 3,800 years ago, with low activity before 4,400 years|
|Great Blue Hole||Belize||Overwash deposits||1,200||Active periods between 800 and 500, 1,300 - 900 or 650 - 1,200 years ago and coinciding with the Medieval Warm Period|
|Gulf of Carpentaria||Australia||Beach ridges||7,500||Low activity/intensity between 5,500-3,500, 2,700-1,800 and 1,000–500 years ago, the former coinciding with the Neoglacial|
|Gulf of Thailand||Thailand||Beach ridges and a coastal marsh||8,000||18 typhoon strikes in the last 8,000 years, with increased activity in the mid-Holocene until 3,900 years ago (2-5 times more storms) either due to a warmer climate or higher sea level induced better sensitivity to storms|
|Hainan Island||China||Deposits in lakes||350||1-2 typhoons per decade, with higher solar activity, positive Pacific Decadal Oscillation, La Nina and positive North Atlantic Oscillation correlating with decreases|
|High Atlas||Morocco||Tempestite||Toarcian||Increased tropical cyclone activity during the hot Toarcian Oceanic Anoxic Event||Inapplicable|
|Ilan Plain||Taiwan||River erosion sediments in a lake||2,000||Between 500 - 700 and after AD 1400 intense typhoon rainfall|
|Israel||Israel||Oxygen isotope ratios in rocks||Cretaceous-Miocene||Intense tropical cyclone activity in the Tethys until its closure 20 million years ago||Inapplicable|
|Kamikoshiki-jima||Japan||Sediments in coastal lagoons||6,400||Higher typhoon activity at the time of the Kamikaze typhoons, with high activity between 3,600 - 2,500 and between 1,000 – 300 years ago|
|Island Bay||Florida||Overwash deposits||1,000||3-4 storms in the last 500 years, 1-2 in 150 – 500 years before present and 11 storms between 1,000 – 500 years ago, all probably major hurricanes; one of the storms in the last 50 years is Hurricane Donna while the other might either be 1926 Miami hurricane, 1910 Cuba hurricane or the 1873 Central Florida Hurricane|
|Kimberley||Australia||Flood deposits in stalagmites||2,200||Moderate activity between 1,450 - 850 CE and low activity between 500 - 850 and 1,450 - 1,650 CE|
|Lady Elliot Island||Queensland||Beach ridges||3,200||Strong storms (at least Category 4 or Category 5) occur every 253 years|
|Laguna Alejandro||Dominican Republic||Sediment analysis||910||Strikes c. 910, 800, 730, 530, 500, 330, 260, 210, 200 and 170 years ago|
|Laguna Negra||Nicaragua||Deposits in a coastal lake||8,000||One very strong storm ("Hurricane Elisenda") 3,340 ± 50 years ago, at the same time as increased storm activity in Alabama and Florida|
|Laguna Madre||Texas||Storm deposits||5,300 - 900 BP||0.46% probability of landfall any given year|
|Laguna Playa Grande||Puerto Rico||Overwash sediments||5,000||0.48% probability of landfall any given year, but an active period in the last 250 years and previous active periods between 2,500 - 1,000 and 3,600 - 5,400 years ago. El Nino is linked with lower activity, a strong West African Monsoon with higher activity|
|Lake Daija||Japan||Sediments in a coastal lagoon||2,000||Beginning at 250 CE increased activity, while a quiet period has lasted from 1600 CE to today. Typhoon Jean, Typhoon Grace and others have been identified, including two deposits that may correlate to the Kamikaze typhoons which also coincide within an active period. Recorded storms appear to be of category 3 or higher strength|
|Lake Shelby||Alabama||Storm deposits||4,800||11 intense storms between 3,500 and 700 years ago, a quiet period before 3,200 radiocarbon years ago may be either a stage of inactivity or a change in the lake environment. Comparisons to Hurricane Frederic and Hurricane Ivan imply that the intense storms reached category 4 or 5 intensity|
|Lake Tiriara||Cook Islands||Minerals from simultaneous seawater intrusion and island erosion||3,500||Two storms between 3,200 - 2,800 and 200 years ago|
|Lingyang Reef||South China Sea||Storm deposits||3,500||Between 3,100 - 1,800 years ago only weak activity, followed and preceded by strong activity; intense storms about once every ten years in the last 3,500 years and the storm activity correlates to sea surface temperatures|
|Little Lake||Alabama||Overwash deposits||1,200||Seven strikes in 1,200 years, including Hurricane Ivan|
|Little Sippewissett Marsh||Massachusetts||Overwash deposits||400||Annual landfall probability is about 2.3%, 4% in the last 50 years|
|Long Island||New York||Overwash deposits||3,500||Increased activity during the Little Ice Age and an inactive period between 900–250 years ago|
|Lower Mystic Lake||Massachusetts||Varves formed by post-storm sedimentation||1000||Up to eight Category 2-3 hurricanes occurred per century in the 12th to 16th century, while the preceding and the two subsequent ones only saw 2-3 such storms per century|
|Mattapoisett Marsh||Massachusetts||Storm inundation deposits||2,200||Inactive period between 2,200 -1,000 followed by an active period in the last 800 years|
|Miaodao||China||Storm deposits||80,000||Marine isotope stage 5e storm frequency comparable to that of Holocene low-latitude China|
|Mullet Pond||Florida||Sediments in a sinkhole||4,500||Active periods with intense storms 650 – 750 years ago, 925 – 875 years ago, 1,250 - 1,150 years ago, 2,800 - 2,300 years ago, 3,350 - 3,250 years ago, 3,600 - 3,500 years ago and 3,950 - 3,650 years ago; the maximum occurrence rate between 2,300 and 2,800 years ago saw six storms per century while the last 150 years have been fairly inactive. Mullet Pond records also somewhat weaker storms and shows a recurrence rate of 3.9 events per century.|
|Onslow Bay||North Carolina||Backbarrier deposits||1,500||Poor preservation; only 5-8 deposits in 1,500 years|
|Oyster Pond||Massachusetts||Sand layers in organic deposits||1,250||One of the earliest paleotempestological records; nine sand layers were interpreted as evidence for hurricanes|
|Pascagoula Marsh||Louisiana||Sediments||4,500 (radiocarbon years)||Storms occur about all 300 years; hyperactive period between 3,800 and 1,000 years ago|
|Pearl River Marsh||Louisiana||Sediments||4,500 (radiocarbon years)||Storms occur about all 300 years; hyperactive period between 3,800 and 1,000 years ago|
|Princess Charlotte Bay||Queensland, Australia||Beach ridges||3,000||12 hits by intense storms in 6,000 years, implying return periods of 180 years|
|Chillagoe||Queensland||Stalagmites||800||2 strong storms between AD 1400 - 1600 after two centuries without one, seven strong storms between AD 1600 and AD 1800 and only one strong storm after that|
|Robinson Lake||Nova Scotia||Sediments in lake||800||Storms at c. 1475, 1530, 1575, 1670 and Hurricane Juan. The record probably reflects storms of at least category 2|
|Rockingham Bay||Queensland||Sand ridges||5,000||Intense storms occurred between 130 and 1,550 years ago as well as between 3,380 - 5,010 years ago, while the time between 1,550 - 2,280 years ago had very weak storms|
|Salt Pond||Massachusetts||Sediments in a lake||2,000||35 hurricanes with active periods between 150 -1,150 CE and 1,400 - 1,675 CE; one historical hurricane (Hurricane Bob) recorded; some storms are stronger than the most intense hurricane there, the Great Colonial Hurricane of 1635|
|Santiago de Cuba||Cuba||Deposits in a coastal lagoon||4,000||Active periods occurred between 2,600 - 1,800 years ago and between 500–250 years ago|
|Sea Breeze||New Jersey||Sediments||AD 214 - present||Storm deposits were emplaced between AD1875-1925, before AD1827, before AD1665-1696, in the 14th-15th century, before AD950-1040, AD429-966 and before AD260-520|
|Seguine Pond||New York||Overwash deposits||300||Severe storm surges associated with the 1821 Norfolk and Long Island hurricane and Hurricane Sandy|
|Shark Bay||Western Australia||Shell beach ridge||6,000||An inactive period between about 5,400 and 3,700 years ago accompanied by drought. Storm intensity indicated by the ridges is about category 2-4 on the Saffir-Simpson scale, while no case of category 5 is inferred|
|Northeast Shark River Slough||Florida||Sediment cores||4,600||Decrease of storm activity after 2,800 years ago|
|Shinnecock Bay||New York||Sediments||Older than 1938AD||Several historical deposits by the 1938 New England hurricane, Hurricane Carol, either Hurricane Donna or Hurricane Esther and the Ash Wednesday Storm of 1962|
|Singleton Swash||South Carolina||Sediments in tidal deposits||3,500||Historical storms like Hurricane Hazel and Hurricane Hugo are recorded, with more storms until 3,000 BP. Between 3,000 - 5,000 there are no storm deposits, but one deposit 5,700 appears to relate to a very intense event, perhaps due to a warmer climate at that time|
|St. Catherines Island||Georgia||Sediment cores||+3,000||7 storms in 3,300 years, equating a recurrence rate of 1 every 471 years. An active period ended 1,100 years before present|
|Spring Creek Pond||Florida||Storm layers||4,500||An active period between about 600 and 1,700 years ago, but fewer major hurricanes in the last 600 years|
|Succotash Marsh||Rhode Island||Sediment overwash||700 years||Over 6 intense storms in the last 700 years|
|Tahaa||French Polynesia||Overwash deposits||5,000||Increased activity between 5,000 - 3,800 and 2,900 – 500 years ago with relative inactivity since|
|Thatchpoint Bluehole||Bahamas||Sediments||AD 1010–present||Recorded storms include Hurricane Jeanne in 2004; active periods between 1050-1150 AD, a very active period between 1350-1650AD, a reincrease in the late 18th century|
|Tutaga||Tuvalu||Coral blocks moved by storms||1,100||Increased storminess c. 1,100, 750, 600 and 350 years ago; correlated with storminess in French Polynesia and a recurrence rate of about 100–150 years|
|Tzabnah Cave||Yucatan||Oxygen isotope ratios in stalagmites||AD 750 and earlier||Low tropical cyclone activity at the time of the Classical Maya collapse, and more generally coinciding with drought|
|Valdosta State University||Georgia||Oxygen isotope ratios in tree rings||AD 1770 - 1990||Historical storms have been recorded, as well as a trio in 1911-1913 and a strong event in 1780|
|Wallaby Island||Australia||Beach ridges||4,100||Strong storms (category 5) occur every 180 years|
|Walsingham Cavern||Bermuda||Sediments in submarine cave||3,100||Increased storm activity between 3,000 - 1,700 and 600 – 150 years ago; however this record might include extratropical storms|
|Wassaw Island||Georgia||Overwash||1,900||At least eight deposits from strong hurricanes between 1,000 - 2,000 years ago, with a quiet period between 1,100 and 250 years ago|
|Western Lake||Florida, northwestern||Overwash deposits||7,000||Between 3,800 - 1,000 years ago strike probability was about 0.5% per year, followed and preceded by relative inactivity|
|Whale Beach||New Jersey||Sand sheets in marshes||AD 1300–present||Two major hurricanes in 700 years, one between 1278-1438 and the other is the 1821 Norfolk and Long Island hurricane|
|Wonga Beach||Queensland, northern||Beach ridges||4,500||An inactive period between about 3,800 and 2,100 years ago was followed by an active on between 2,100 and 900 years ago|
|Yok Balum Cave||Belize||Oxygen isotope ratios in speleothems||AD 1550 - 1983||After an inactive phase (~1 storm/year) in the middle 16th century, an increase to ~8 storms/year in the 17th century associated with the Little Ice Age. Then a steady decrease until 1870, when occurrence halved and dropped to ~2 storms/year|
|Yongshu Reef||South China Sea||Coral blocks relocated by storms||4,000||Six strikes in 1,000 years, with two during the Little Ice Age and four during the Medieval Climate Anomaly. Also high storm activity around 1200 AD, 400 BC and 1200 BC|
The Holocene is the current geological epoch. It began approximately 11,650 cal years before present, after the last glacial period, which concluded with the Holocene glacial retreat. The Holocene and the preceding Pleistocene together form the Quaternary period. The Holocene has been identified with the current warm period, known as MIS 1. It is considered by some to be an interglacial period within the Pleistocene Epoch.
A subtropical cyclone is a weather system that has some characteristics of a tropical and an extratropical cyclone.
Accumulated cyclone energy (ACE) is a measure used by various agencies including the National Oceanic and Atmospheric Administration (NOAA) and the India Meteorological Department to express the activity of individual tropical cyclones and entire tropical cyclone seasons. It uses an approximation of the wind energy used by a tropical system over its lifetime and is calculated every six hours. The ACE of a season is the sum of the ACEs for each storm and takes into account the number, strength, and duration of all the tropical storms in the season. The highest ACE calculated for a single storm is 82, for Hurricane/Typhoon Ioke in 2006.
Cyclone Mahina was the deadliest cyclone in recorded Australian history, and also likely the most intense tropical cyclone ever recorded in the Southern Hemisphere. Mahina struck Bathurst Bay, Cape York Peninsula, Queensland, on 4 March 1899, and its winds and enormous storm surge combined to kill more than 300 people.
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.
The Atlantic hurricane reanalysis project of the National Oceanic and Atmospheric Administration seeks to correct and add new information about past North Atlantic hurricanes. It was started around 2000 to update HURDAT, the official hurricane database for the Atlantic Basin, which has become outdated since its creation due to various systematic errors introduced into the database over time. This effort has involved reanalyses of ship observations from the International Comprehensive Ocean-Atmosphere Data Set (ICOADS) as well as reanalyses done by other researchers over the years. It has been ongoing as of 2016, and should last another four years.
Tropical cyclogenesis is the development and strengthening of a tropical cyclone in the atmosphere. 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.
Tropical cyclone observation has been carried out over the past couple of centuries in various ways. The passage of typhoons, hurricanes, as well as other tropical cyclones have been detected by word of mouth from sailors recently coming to port or by radio transmissions from ships at sea, from sediment deposits in near shore estuaries, to the wiping out of cities near the coastline. Since World War II, advances in technology have included using planes to survey the ocean basins, satellites to monitor the world's oceans from outer space using a variety of methods, radars to monitor their progress near the coastline, and recently the introduction of unmanned aerial vehicles to penetrate storms. Recent studies have concentrated on studying hurricane impacts lying within rocks or near shore lake sediments, which are branches of a new field known as paleotempestology. This article details the various methods employed in the creation of the hurricane database, as well as reconstructions necessary for reanalysis of past storms used in projects such as the Atlantic hurricane reanalysis.
The main effects of tropical cyclones include heavy rain, strong wind, large storm surges near landfall, and tornadoes. The destruction from a tropical cyclone, such as a hurricane or tropical storm, depends mainly on its intensity, its size, and its location. Tropical cyclones act to remove forest canopy as well as change the landscape near coastal areas, by moving and reshaping sand dunes and causing extensive erosion along the coast. Even well inland, heavy rainfall can lead to mudslides and landslides in mountainous areas. Their effects can be sensed over time by studying the concentration of the Oxygen-18 isotope within caves within the vicinity of cyclones' paths.
Hurricane Alley is an area of warm water in the Atlantic Ocean stretching from the west coast of northern Africa to the east coast of Central America and Gulf Coast of the Southern United States. Many hurricanes form within this area. The sea surface temperature of the Atlantic in Hurricane Alley has grown slightly warmer over the past decades. A particularly warm summer in 2005 led climate scientists to begin studying whether this trend would lead to an increase in hurricane activity. See Effects of Climate Change below.
Mediterranean tropical-like cyclones, often referred to as medicanes but sometimes also as Mediterranean cyclones or as Mediterranean hurricanes, are meteorological phenomena observed over the Mediterranean Sea. On a few rare occasions, some storms have been observed reaching the strength of a Category 1 hurricane. The main societal hazard posed by Medicanes is not usually from destructive winds, but through life-threatening torrential rains and flash floods.
Tropical cyclones and climate change concerns how tropical cyclones have changed, and are expected to further change, under global warming. The topic receives considerable attention from climate scientists who study the connections between storms and climate, and notably since 2005 makes news during active storm seasons.
The African humid period (AHP) is a climate period in Africa during the Holocene during which northern Africa was wetter than today. It was caused by changes in Earth's orbit around the Sun, and involved changes in vegetation and dust in the Sahara that altered the African monsoon, the disappearance of much of the Sahara desert which was replaced by grassy vegetation, trees and lakes and the settlement of the former desert by various animals and humans, who lived as hunter-gatherers. It has had profound effects on present-day Africa such as the birth of the Pharaonic civilization and the pyramids and potentially also the development of widespread Golden Age myths.
The Homeric Minimum is a grand solar minimum that took place between 2,800 and 2,550 years before present. It appears to coincide with, and have been the cause of, a phase of climate change at that time, which involved a wetter western and drier eastern Europe. This had far-reaching effects on human civilization, some of which may be recorded in Greek mythology and the Old Testament.