颶風過到澳大利亞英語怎麼說

㈠ 颶風 英語怎麼說

Define 颶風: [ jù fēng ]
1. hurricane
2. cyclone
3. flurry

Relative explainations:
<whirlblast> <wildwind> <tropical hurricane> <tornado>

Examples:
1. 颶風在英國非常罕見。
Hurricanes are uncommon in England.
2. 颶風每小時73英里。
The hurricane has a speed of 73 miles per hour.
3. 外面颶風呼嘯著.
The hurricane screamed outside.
4. 對於這地勢很低的海濱地區，颶風將是一場災難
A hurricane would be a calamity for this low-lying coastal region

㈡ 颶風英語怎麼說

hurricane

英[ˈhʌrɪkən]美[ˈhɜːrəkeɪn]

n. 颶風，暴風

短語

Hurricane Irene艾琳颶風

Hurricane Katrina颶風卡特里娜 ; 卡特里娜颶風 ; 卡特里娜 ; 卡崔娜颶風

Hurricane Sandy颶風桑迪 ; 桑迪颶風 ; 颶風珊迪

Hurricane Ike颶風艾克 ; 颶風埃克

The Hurricane颶風 ; 捍衛正義 ; 黑罪風雲 ; 颶風俠

Hurricane Rita颶風麗塔 ; 莉塔颶風

例句：

1、Sometimes a nor'easter can be worse than a hurricane.

一場東北風暴有時比一次颶風還糟糕。

2、Hurricane Betty is now approaching the coast of Florida.

颶風貝蒂正在逼近佛羅里達海岸。

3、The eye of the hurricane hit Florida just south of Miami.

颶風中心襲擊了邁阿密正南面的佛羅里達州。

4、Hurricane Andrew was last night heading into the Gulf of Mexico.

安德魯颶風昨晚進入墨西哥灣。

5、People were swimming in the ocean despite the hurricane warning.

盡管有颶風警報，人們仍然在大海里游泳。

㈢ 颶風的英文，颶風的翻譯，怎麼用英語翻譯颶風，颶風用

颶風

[詞典]hurricane; typhoon; furacana; furacan(e); furicane; furicano

[例句]

TheHurricane.

颶風中心警告人們，不要對熱帶風暴的危險掉以輕心。

㈣ 颶風用英語怎麼說

颶風
[詞典] hurricane; cyclone; typhoon;
[例句]颶風中心警告人們，不要對熱帶風暴的危險掉以輕心。
The Hurricane Center warns people not to take the threat of tropical storms lightly

㈤ 颶風 英語

"Hurricane" redirects here. For other uses, see Hurricane (disambiguation).

Cyclone Catarina, a rare South Atlantic tropical cyclone, viewed from the International Space Station in March 2004
Tropical cyclones
Formation and naming
Development - Structure
Naming - Seasonal lists - Full list
Effects
Effects
Watches and warnings
Storm surge - Notable storms
Retired names (Atlantic - Eastern Pacific - Western Pacific)

Climatology and tracking
Basins - RSMCs - TCWCs - Scales
Observation - Forecasting
Rainfall forecasting
Rainfall climatology
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Part of the Nature series: Weather

A tropical cyclone is a storm system characterized by a large low pressure center and numerous thunderstorms that proce strong winds and flooding rain. Tropical cyclones feed on heat released when moist air rises, resulting in condensation of water vapor contained in the moist air. They are fueled by a different heat mechanism than other cyclonic windstorms such as nor'easters, European windstorms, and polar lows, leading to their classification as "warm core" storm systems.

The term "tropical" refers to both the geographic origin of these systems, which form almost exclusively in tropical regions of the globe, and their formation in Maritime Tropical air masses. The term "cyclone" refers to such storms' cyclonic nature, with counterclockwise rotation in the Northern Hemisphere and clockwise rotation in the Southern Hemisphere. Depending on its location and strength, a tropical cyclone is referred to by many other names, such as hurricane, typhoon, tropical storm, cyclonic storm, tropical depression, and simply cyclone.

While tropical cyclones can proce extremely powerful winds and torrential rain, they are also able to proce high waves and damaging storm surge as well as spawning tornadoes. They develop over large bodies of warm water, and lose their strength if they move over land. This is the reason coastal regions can receive significant damage from a tropical cyclone, while inland regions are relatively safe from receiving strong winds. Heavy rains, however, can proce significant flooding inland, and storm surges can proce extensive coastal flooding up to 40 kilometres (25 mi) from the coastline. Although their effects on human populations can be devastating, tropical cyclones can also relieve drought conditions. They also carry heat and energy away from the tropics and transport it toward temperate latitudes, which makes them an important part of the global atmospheric circulation mechanism. As a result, tropical cyclones help to maintain equilibrium in the Earth's troposphere, and to maintain a relatively stable and warm temperature worldwide.

Many tropical cyclones develop when the atmospheric conditions around a weak disturbance in the atmosphere are favorable. Others form when other types of cyclones acquire tropical characteristics. Tropical systems are then moved by steering winds in the troposphere; if the conditions remain favorable, the tropical disturbance intensifies, and can even develop an eye. On the other end of the spectrum, if the conditions around the system deteriorate or the tropical cyclone makes landfall, the system weakens and eventually dissipates. It is not possible to artificially ince the dissipation of these systems with current technology.
All tropical cyclones are areas of low atmospheric pressure near the Earth's surface. The pressures recorded at the centers of tropical cyclones are among the lowest that occur on Earth's surface at sea level.[1] Tropical cyclones are characterized and driven by the release of large amounts of latent heat of condensation, which occurs when moist air is carried upwards and its water vapor condenses. This heat is distributed vertically around the center of the storm. Thus, at any given altitude (except close to the surface, where water temperature dictates air temperature) the environment inside the cyclone is warmer than its outer surroundings.[2]

[edit] Eye and center
A strong tropical cyclone will harbor an area of sinking air at the center of circulation. If this area is strong enough, it can develop into an eye. Weather in the eye is normally calm and free of clouds, although the sea may be extremely violent.[3] The eye is normally circular in shape, and may range in size from 3 kilometres (1.9 mi) to 370 kilometres (230 mi) in diameter.[4][5] Intense, mature tropical cyclones can sometimes exhibit an outward curving of the eyewall's top, making it resemble a football stadium; this phenomenon is thus sometimes referred to as the stadium effect.[6]

There are other features that either surround the eye, or cover it. The central dense overcast is the concentrated area of strong thunderstorm activity near the center of a tropical cyclone;[7] in weaker tropical cyclones, the CDO may cover the center completely.[8] The eyewall is a circle of strong thunderstorms that surrounds the eye; here is where the greatest wind speeds are found, where clouds reach the highest, and precipitation is the heaviest. The heaviest wind damage occurs where a tropical cyclone's eyewall passes over land.[3] Eyewall replacement cycles occur naturally in intense tropical cyclones. When cyclones reach peak intensity they usually have an eyewall and radius of maximum winds that contract to a very small size, around 10 kilometres (6.2 mi) to 25 kilometres (16 mi). Outer rainbands can organize into an outer ring of thunderstorms that slowly moves inward and robs the inner eyewall of its needed moisture and angular momentum. When the inner eyewall weakens, the tropical cyclone weakens (in other words, the maximum sustained winds weaken and the central pressure rises.) The outer eyewall replaces the inner one completely at the end of the cycle. The storm can be of the same intensity as it was previously or even stronger after the eyewall replacement cycle finishes. The storm may strengthen again as it builds a new outer ring for the next eyewall replacement.[9]

One measure of the size of a tropical cyclone is determined by measuring the distance from its center of circulation to its outermost closed isobar, also known as its ROCI. If the radius is less than two degrees of latitude or 222 kilometres (138 mi), then the cyclone is "very small" or a "midget". A Radius between 3 and 6 latitude degrees or 333 kilometres (207 mi) to 666 kilometres (414 mi) are considered "average sized". "Very large" tropical cyclones have a radius of greater than 8 degrees or 888 kilometres (552 mi).[10] Use of this measure has objectively determined that tropical cyclones in the northwest Pacific ocean are the largest on earth on average, with Atlantic tropical cyclones roughly half their size.[11] Other methods of determining a tropical cyclone's size include measuring the radius of gale force winds and measuring the radius at which its relative vorticity field decreases to 1×10-5 s-1 from its center.[12][13]

A tropical cyclone's primary energy source is the release of the heat of condensation from water vapor condensing at high altitudes, with solar heating being the initial source for evaporation. Therefore, a tropical cyclone can be visualized as a giant vertical heat engine supported by mechanics driven by physical forces such as the rotation and gravity of the Earth.[15] In another way, tropical cyclones could be viewed as a special type of mesoscale convective complex, which continues to develop over a vast source of relative warmth and moisture. Condensation leads to higher wind speeds, as a tiny fraction of the released energy is converted into mechanical energy;[16] the faster winds and lower pressure associated with them in turn cause increased surface evaporation and thus even more condensation. Much of the released energy drives updrafts that increase the height of the storm clouds, speeding up condensation.[17] This positive feedback loop continues for as long as conditions are favorable for tropical cyclone development. Factors such as a continued lack of equilibrium in air mass distribution would also give supporting energy to the cyclone. The rotation of the Earth causes the system to spin, an effect known as the Coriolis effect,[18] giving it a cyclonic characteristic and affecting the trajectory of the storm.[19]

What primarily distinguishes tropical cyclones from other meteorological phenomena is deep convection as a driving force.[20] Because convection is strongest in a tropical climate, it defines the initial domain of the tropical cyclone. By contrast, mid-latitude cyclones draw their energy mostly from pre-existing horizontal temperature gradients in the atmosphere.[20] To continue to drive its heat engine, a tropical cyclone must remain over warm water, which provides the needed atmospheric moisture to keep the positive feedback loop running. When a tropical cyclone passes over land, it is cut off from its heat source and its strength diminishes rapidly.[21]

Chart displaying the drop in surface temperature in the Gulf of Mexico as Hurricanes Katrina and Rita passed overThe passage of a tropical cyclone over the ocean can cause the upper layers of the ocean to cool substantially, which can influence subsequent cyclone development. Cooling is primarily caused by upwelling of cold water from deeper in the ocean e to the wind. The cooler water causes the storm to weaken. This is a negative feedback process that causes the storms to weaken over sea because of their own effects. 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 proce a dramatic drop in sea surface temperature over a large area in just a few days.[22]

Scientists at the US National Center for Atmospheric Research estimate that a tropical cyclone releases heat energy at the rate of 50 to 200 exajoules (1018 J) per day,[17] equivalent to about 1 PW (1015 watt). This rate of energy release is equivalent to 70 times the world energy consumption of humans and 200 times the worldwide electrical generating capacity,[17] or to exploding a 10-megaton nuclear bomb every 20 minutes.[23]

While the most obvious motion of clouds is toward the center, tropical cyclones also develop an upper-level (high-altitude) outward flow of clouds. These originate from air that has released its moisture and is expelled at high altitude through the "chimney" of the storm engine.[15] This outflow proces high, thin cirrus clouds that spiral away from the center. The clouds are thin enough for the sun to be visible through them. These high cirrus clouds may be the first signs of an approaching tropical cyclone.[24]
There are six Regional Specialized Meteorological Centres (RSMCs) worldwide. These organizations are designated by the World Meteorological Organization and are responsible for tracking and issuing bulletins, warnings, and advisories about tropical cyclones in their designated areas of responsibility. Additionally, there are six Tropical Cyclone Warning Centres (TCWCs) that provide information to smaller regions.[26] The RSMCs and TCWCs are not the only organizations that provide information about tropical cyclones to the public. The Joint Typhoon Warning Center (JTWC) issues advisories in all basins except the Northern Atlantic for the purposes of the United States Government.[27] The Philippine Atmospheric, Geophysical and Astronomical Services Administration (PAGASA) issues advisories and names for tropical cyclones that approach the Philippines in the Northwestern Pacific to protect the life and property of its citizens.[28] The Canadian Hurricane Centre (CHC) issues advisories on hurricanes and their remnants for Canadian citizens when they affect Canada.[29]

On 26 March 2004, Cyclone Catarina became the first recorded South Atlantic cyclone and subsequently struck southern Brazil with winds equivalent to Category 2 on the Saffir-Simpson Hurricane Scale. As the cyclone formed outside the authority of another warning center, Brazilian meteorologists initially treated the system as an extratropical cyclone, although subsequently classified it as tropical.[30]

Worldwide, tropical cyclone activity peaks in late summer, when the difference between temperatures aloft and sea surface temperatures is the greatest. However, each particular basin has its own seasonal patterns. On a worldwide scale, May is the least active month, while September is the most active.[31]

In the Northern Atlantic Ocean, a distinct hurricane season occurs from June 1 to November 30, sharply peaking from late August through September.[31] The statistical peak of the Atlantic hurricane season is 10 September. The Northeast Pacific Ocean has a broader period of activity, but in a similar time frame to the Atlantic.[32] The Northwest Pacific sees tropical cyclones year-round, with a minimum in February and March 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.[31]

In the Southern Hemisphere, tropical cyclone activity begins in late October and ends in May. Southern Hemisphere activity peaks in mid-February to early March.[31]

The formation of tropical cyclones is the topic of extensive ongoing research and is still not fully understood.[34] While six factors appear to be generally necessary, tropical cyclones may occasionally form without meeting all of the following conditions. In most situations, water temperatures of at least 26.5 °C (79.7 °F) are needed down to a depth of at least 50 metres (160 ft);[35] waters of this temperature cause the overlying atmosphere to be unstable enough to sustain convection and thunderstorms.[36] Another factor is rapid cooling with height, which allows the release of the heat of condensation that powers a tropical cyclone.[35] High humidity is needed, especially in the lower-to-mid troposphere; when there is a great deal of moisture in the atmosphere, conditions are more favorable for disturbances to develop.[35] Low amounts of wind shear are needed, as high shear is disruptive to the storm's circulation.[35] Tropical cyclones generally need to form more than 555 kilometres (345 mi) or 5 degrees of latitude away from the equator, allowing the Coriolis effect to deflect winds blowing towards the low pressure center and creating a circulation.[35] Lastly, a formative tropical cyclone needs a pre-existing system of disturbed weather, although without a circulation no cyclonic development will take place.[35]

Most tropical cyclones form in a worldwide band of thunderstorm activity called by several names: the Intertropical Front (ITF),[37] the Intertropical Convergence Zone (ITCZ),[38] or the monsoon trough.[39] Another important source of atmospheric instability is found in tropical waves, which cause about 85% of intense tropical cyclones in the Atlantic ocean,[40] and become most of the tropical cyclones in the Eastern Pacific basin.[41][42]

Tropical cyclones move westward when equatorward of the subtropical ridge, intensifying as they move. Most of these systems form between 10 and 30 degrees away of the equator,[43] and 87% form no farther away than 20 degrees of latitude, north or south.[44] Because the Coriolis effect initiates and maintains tropical cyclone rotation, tropical cyclones rarely form or move within about 5 degrees of the equator, where the Coriolis effect is weakest.[43] However, it is possible for tropical cyclones to form within this boundary as Tropical Storm Vamei did in 2001 and Cyclone Agni in 2004.[45][46]