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Cherry tree moving with wind blowing about 22 m/sec Cherry tree moving in the wind 1.gif
Cherry tree moving with wind blowing about 22 m/sec

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 (wind speed); 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.

Gas One of the four fundamental states of matter

Gas is one of the four fundamental states of matter. A pure gas may be made up of individual atoms, elemental molecules made from one type of atom, or compound molecules made from a variety of atoms. A gas mixture, such as air, contains a variety of pure gases. What distinguishes a gas from liquids and solids is the vast separation of the individual gas particles. This separation usually makes a colorless gas invisible to the human observer. The interaction of gas particles in the presence of electric and gravitational fields are considered negligible, as indicated by the constant velocity vectors in the image.

Outer space Void between celestial bodies

Outer space, or just space, is the expanse that exists beyond the Earth and between celestial bodies. Outer space is not completely empty—it is a hard vacuum containing a low density of particles, predominantly a plasma of hydrogen and helium, as well as electromagnetic radiation, magnetic fields, neutrinos, dust, and cosmic rays. The baseline temperature of outer space, as set by the background radiation from the Big Bang, is 2.7 kelvins. The plasma between galaxies accounts for about half of the baryonic (ordinary) matter in the universe; it has a number density of less than one hydrogen atom per cubic metre and a temperature of millions of kelvins; local concentrations of this plasma have condensed into stars and galaxies. Studies indicate that 90% of the mass in most galaxies is in an unknown form, called dark matter, which interacts with other matter through gravitational but not electromagnetic forces. Observations suggest that the majority of the mass-energy in the observable universe is dark energy, a type of vacuum energy that is poorly understood. Intergalactic space takes up most of the volume of the universe, but even galaxies and star systems consist almost entirely of empty space.

Solar wind

The solar wind is a stream of charged particles released from the upper atmosphere of the Sun, called the corona. This plasma consists of mostly electrons, protons and alpha particles with kinetic energy between 0.5 and 10 keV. Embedded within the solar-wind plasma is the interplanetary magnetic field. The solar wind varies in density, temperature and speed over time and over solar latitude and longitude. Its particles can escape the Sun's gravity because of their high energy resulting from the high temperature of the corona, which in turn is a result of the coronal magnetic field.


In meteorology, winds are often referred to according to their strength, and the direction from which the wind is blowing. Short bursts of high-speed wind are termed gusts. Strong winds of intermediate duration (around one minute) are termed squalls. Long-duration winds have various names associated with their average strength, such as breeze, gale, storm, and hurricane. Wind occurs on a range of scales, from thunderstorm flows lasting tens of minutes, to local breezes generated by heating of land surfaces and lasting a few hours, to global winds resulting from the difference in absorption of solar energy between the climate zones on Earth. The two main causes of large-scale atmospheric circulation are the differential heating between the equator and the poles, and the rotation of the planet (Coriolis effect). Within the tropics, thermal low circulations over terrain and high plateaus can drive monsoon circulations. In coastal areas the sea breeze/land breeze cycle can define local winds; in areas that have variable terrain, mountain and valley breezes can dominate local winds.

Meteorology Interdisciplinary scientific study of the atmosphere focusing on weather forecasting

Meteorology is a branch of the atmospheric sciences which includes atmospheric chemistry and atmospheric physics, with a major focus on weather forecasting. The study of meteorology dates back millennia, though significant progress in meteorology did not occur until the 18th century. The 19th century saw modest progress in the field after weather observation networks were formed across broad regions. Prior attempts at prediction of weather depended on historical data. It was not until after the elucidation of the laws of physics and more particularly, the development of the computer, allowing for the automated solution of a great many equations that model the weather, in the latter half of the 20th century that significant breakthroughs in weather forecasting were achieved. An important domain of weather forecasting is marine weather forecasting as it relates to maritime and coastal safety, in which weather effects also include atmospheric interactions with large bodies of water.

Squall sudden, sharp increase in the sustained winds over a short time interval

A squall is a sudden, sharp increase in wind speed lasting minutes, contrary to a wind gust lasting seconds. They are usually associated with active weather, such as rain showers, thunderstorms, or heavy snow. Squalls refer to the increase to the sustained winds over that time interval, as there may be higher gusts during a squall event. They usually occur in a region of strong sinking air or cooling in the mid-atmosphere. These force strong localized upward motions at the leading edge of the region of cooling, which then enhances local downward motions just in its wake.

Gale strong wind

A gale is a strong wind, typically used as a descriptor in nautical contexts. The U.S. National Weather Service defines a gale as 34–47 knots of sustained surface winds. Forecasters typically issue gale warnings when winds of this strength are expected. In the United States, a gale warning is specifically a maritime warning; the land-based equivalent in National Weather Service warning products is a wind advisory.

In human civilization, the concept of wind has been explored in mythology, influenced the events of history, expanded the range of transport and warfare, and provided a power source for mechanical work, electricity and recreation. Wind powers the voyages of sailing ships across Earth's oceans. Hot air balloons use the wind to take short trips, and powered flight uses it to increase lift and reduce fuel consumption. Areas of wind shear caused by various weather phenomena can lead to dangerous situations for aircraft. When winds become strong, trees and human-made structures are damaged or destroyed.

Wind power The conversion of wind energy into a useful form

Wind power is the use of air flow through wind turbines to provide the mechanical power to turn electric generators and traditionally to do other work, like milling or pumping. Wind power, as an alternative to burning fossil fuels, is plentiful, renewable, widely distributed, clean, produces no greenhouse gas emissions during operation, consumes no water, and uses little land. The net effects on the environment are far less problematic than those of fossil fuel sources.

Sailing ship Large wind-powered water vessel

A sailing ship is a large watercraft that uses sails to harness the power of wind. A "ship-rigged" sailing ship carries three or more masts with square sails on each. Other large sailing vessels, that are not ship-rigged, may be more precisely referred to by their sail rig, such as schooner, barque, brig, barkentine, brigantine or sloop.

Hot air balloon lighter than air aircraft consisting of a bag, called an envelope, which contains heated air

A hot air balloon is a lighter-than-air aircraft consisting of a bag, called an envelope, which contains heated air. Suspended beneath is a gondola or wicker basket, which carries passengers and a source of heat, in most cases an open flame caused by burning liquid propane. The heated air inside the envelope makes it buoyant since it has a lower density than the colder air outside the envelope. As with all aircraft, hot air balloons cannot fly beyond the atmosphere. Unlike gas balloons, the envelope does not have to be sealed at the bottom, since the air near the bottom of the envelope is at the same pressure as the surrounding air. In modern sport balloons the envelope is generally made from nylon fabric and the inlet of the balloon is made from a fire resistant material such as Nomex. Modern balloons have been made in all kinds of shapes, such as rocket ships and the shapes of various commercial products, though the traditional shape is used for most non-commercial, and many commercial, applications.

Winds can shape landforms, via a variety of aeolian processes such as the formation of fertile soils, such as loess, and by erosion. Dust from large deserts can be moved great distances from its source region by the prevailing winds; winds that are accelerated by rough topography and associated with dust outbreaks have been assigned regional names in various parts of the world because of their significant effects on those regions. Wind also affects the spread of wildfires. Winds can disperse seeds from various plants, enabling the survival and dispersal of those plant species, as well as flying insect populations. When combined with cold temperatures, wind has a negative impact on livestock. Wind affects animals' food stores, as well as their hunting and defensive strategies.

Aeolian processes Processes due to wind activity

Aeolian processes, also spelled eolian or æolian, pertain to wind activity in the study of geology and weather and specifically to the wind's ability to shape the surface of the Earth. Winds may erode, transport, and deposit materials and are effective agents in regions with sparse vegetation, a lack of soil moisture and a large supply of unconsolidated sediments. Although water is a much more powerful eroding force than wind, aeolian processes are important in arid environments such as deserts.

Loess A predominantly silt-sized clastic sediment of accumulated wind-blown dust

Loess is a clastic, predominantly silt-sized sediment that is formed by the accumulation of wind-blown dust. Ten percent of the Earth's land area is covered by loess or similar deposits.

Erosion Processes which remove soil and rock from one place on the Earths crust, then transport it to another location where it is deposited

In earth science, erosion is the action of surface processes that removes soil, rock, or dissolved material from one location on the Earth's crust, and then transports it to another location. This natural process is caused by the dynamic activity of erosive agents, that is, water, ice (glaciers), snow, air (wind), plants, animals, and humans. In accordance with these agents, erosion is sometimes divided into water erosion, glacial erosion, snow erosion, wind (aeolic) erosion, zoogenic erosion, and anthropogenic erosion. The particulate breakdown of rock or soil into clastic sediment is referred to as physical or mechanical erosion; this contrasts with chemical erosion, where soil or rock material is removed from an area by its dissolving into a solvent, followed by the flow away of that solution. Eroded sediment or solutes may be transported just a few millimetres, or for thousands of kilometres.


Surface analysis of the Great Blizzard of 1888. Areas with greater isobaric packing indicate higher winds. 10 PM March 12 surface analysis of Great Blizzard of 1888.png
Surface analysis of the Great Blizzard of 1888. Areas with greater isobaric packing indicate higher winds.

Wind is caused by differences in the atmospheric pressure. When a difference in atmospheric pressure exists, air moves from the higher to the lower pressure area, resulting in winds of various speeds. On a rotating planet, air will also be deflected by the Coriolis effect, except exactly on the equator. Globally, the two major driving factors of large-scale wind patterns (the atmospheric circulation) are the differential heating between the equator and the poles (difference in absorption of solar energy leading to buoyancy forces) and the rotation of the planet. Outside the tropics and aloft from frictional effects of the surface, the large-scale winds tend to approach geostrophic balance. Near the Earth's surface, friction causes the wind to be slower than it would be otherwise. Surface friction also causes winds to blow more inward into low-pressure areas. [1] [2]

Atmospheric pressure, sometimes also called barometric pressure, is the pressure within the atmosphere of Earth. The standard atmosphere is a unit of pressure defined as 1013.25 mbar (101325 Pa), equivalent to 760 mm Hg (torr), 29.9212 inches Hg, or 14.696 psi. The atm unit is roughly equivalent to the mean sea-level atmospheric pressure on Earth, that is, the Earth's atmospheric pressure at sea level is approximately 1 atm.

Atmospheric circulation The large-scale movement of air, a process which distributes thermal energy about the Earths surface

Atmospheric circulation is the large-scale movement of air, and together with ocean circulation is the means by which thermal energy is redistributed on the surface of the Earth.

Solar energy energy transmitted from the sun

Solar energy is radiant light and heat from the Sun that is harnessed using a range of ever-evolving technologies such as solar heating, photovoltaics, solar thermal energy, solar architecture, molten salt power plants and artificial photosynthesis.

Winds defined by an equilibrium of physical forces are used in the decomposition and analysis of wind profiles. They are useful for simplifying the atmospheric equations of motion and for making qualitative arguments about the horizontal and vertical distribution of winds. The geostrophic wind component is the result of the balance between Coriolis force and pressure gradient force. It flows parallel to isobars and approximates the flow above the atmospheric boundary layer in the midlatitudes. [3] The thermal wind is the difference in the geostrophic wind between two levels in the atmosphere. It exists only in an atmosphere with horizontal temperature gradients. [4] The ageostrophic wind component is the difference between actual and geostrophic wind, which is responsible for air "filling up" cyclones over time. [5] The gradient wind is similar to the geostrophic wind but also includes centrifugal force (or centripetal acceleration). [6]

In physics, equations of motion are equations that describe the behavior of a physical system in terms of its motion as a function of time. More specifically, the equations of motion describe the behaviour of a physical system as a set of mathematical functions in terms of dynamic variables: normally spatial coordinates and time are used, but others are also possible, such as momentum components and time. The most general choice are generalized coordinates which can be any convenient variables characteristic of the physical system. The functions are defined in a Euclidean space in classical mechanics, but are replaced by curved spaces in relativity. If the dynamics of a system is known, the equations are the solutions for the differential equations describing the motion of the dynamics.

The geostrophic wind is the theoretical wind that would result from an exact balance between the Coriolis force and the pressure gradient force. This condition is called geostrophic balance. The geostrophic wind is directed parallel to isobars. This balance seldom holds exactly in nature. The true wind almost always differs from the geostrophic wind due to other forces such as friction from the ground. Thus, the actual wind would equal the geostrophic wind only if there were no friction and the isobars were perfectly straight. Despite this, much of the atmosphere outside the tropics is close to geostrophic flow much of the time and it is a valuable first approximation. Geostrophic flow in air or water is a zero-frequency inertial wave.

Thermal wind

The thermal wind is the variation in strength of wind with height due to, on one hand, a balance between the Coriolis and pressure-gradient forces in the atmosphere and, on the other hand, horizontal temperature gradients. It is the primary physical mechanism for the jet stream and plays an important role in other large-scale atmospheric phenomena. The thermal wind ensures the jet stream is typically strongest in the upper half of the troposphere, which is the atmospheric layer extending from the surface of the planet up to a height of 12 km to 15 km.


Cup-type anemometer with vertical axis, a sensor on a remote meteorological station Anemometer 2745.JPG
Cup-type anemometer with vertical axis, a sensor on a remote meteorological station
An occluded mesocyclone tornado (Oklahoma, May 1999) Occluded mesocyclone tornado5 - NOAA.jpg
An occluded mesocyclone tornado (Oklahoma, May 1999)

Wind direction is usually expressed in terms of the direction from which it originates. For example, a northerly wind blows from the north to the south. [7] Weather vanes pivot to indicate the direction of the wind. [8] At airports, windsocks indicate wind direction, and can also be used to estimate wind speed by the angle of hang. [9] Wind speed is measured by anemometers, most commonly using rotating cups or propellers. When a high measurement frequency is needed (such as in research applications), wind can be measured by the propagation speed of ultrasound signals or by the effect of ventilation on the resistance of a heated wire. [10] Another type of anemometer uses pitot tubes that take advantage of the pressure differential between an inner tube and an outer tube that is exposed to the wind to determine the dynamic pressure, which is then used to compute the wind speed. [11]

Sustained wind speeds are reported globally at a 10 meters (33 ft) height and are averaged over a 10‑minute time frame. The United States reports winds over a 1‑minute average for tropical cyclones, [12] and a 2‑minute average within weather observations. [13] India typically reports winds over a 3‑minute average. [14] Knowing the wind sampling average is important, as the value of a one-minute sustained wind is typically 14% greater than a ten-minute sustained wind. [15] A short burst of high speed wind is termed a wind gust, one technical definition of a wind gust is: the maxima that exceed the lowest wind speed measured during a ten-minute time interval by 10 knots (19 km/h) for periods of seconds. A squall is an increase of the wind speed above a certain threshold, which lasts for a minute or more.

To determine winds aloft, rawinsondes determine wind speed by GPS, radio navigation, or radar tracking of the probe. [16] Alternatively, movement of the parent weather balloon position can be tracked from the ground visually using theodolites. [17] Remote sensing techniques for wind include SODAR, Doppler lidars and radars, which can measure the Doppler shift of electromagnetic radiation scattered or reflected off suspended aerosols or molecules, and radiometers and radars can be used to measure the surface roughness of the ocean from space or airplanes. Ocean roughness can be used to estimate wind velocity close to the sea surface over oceans. Geostationary satellite imagery can be used to estimate the winds throughout the atmosphere based upon how far clouds move from one image to the next. Wind engineering describes the study of the effects of the wind on the built environment, including buildings, bridges and other man-made objects.

Wind force scale

Historically, the Beaufort wind force scale (created by Beaufort) provides an empirical description of wind speed based on observed sea conditions. Originally it was a 13-level scale, but during the 1940s, the scale was expanded to 17 levels. [18] There are general terms that differentiate winds of different average speeds such as a breeze, a gale, a storm, tornado, or a hurricane. Within the Beaufort scale, gale-force winds lie between 28 knots (52 km/h) and 55 knots (102 km/h) with preceding adjectives such as moderate, fresh, strong, and whole used to differentiate the wind's strength within the gale category. [19] A storm has winds of 56 knots (104 km/h) to 63 knots (117 km/h). [20] The terminology for tropical cyclones differs from one region to another globally. Most ocean basins use the average wind speed to determine the tropical cyclone's category. Below is a summary of the classifications used by Regional Specialized Meteorological Centers worldwide:

General wind classificationsTropical cyclone classifications (all winds are 10-minute averages)
Beaufort scale [18] 10-minute sustained winds (knots)10-minute sustained winds (km/h)General term [21] N Indian Ocean
SW Indian Ocean
Australian region
South Pacific
NW Pacific
NW Pacific
NE Pacific &
N Atlantic
0<1<2CalmLow Pressure AreaTropical disturbanceTropical low
Tropical Depression
Tropical depressionTropical depressionTropical depression
11–32–6Light air
24–67–11Light breeze
37–1013–19Gentle breeze
411–1620–30Moderate breeze
517–2131–39Fresh breezeDepression
622–2741–50Strong breeze
728–2952–54Moderate galeDeep depressionTropical depression
834–4063–74Fresh galeCyclonic stormModerate tropical stormTropical cyclone (1)Tropical stormTropical stormTropical storm
941–4776–87Strong gale
1048–5589–102Whole galeSevere cyclonic stormSevere tropical stormTropical cyclone (2)Severe tropical storm
1264–72119–133HurricaneVery severe cyclonic stormTropical cycloneSevere tropical cyclone (3)TyphoonTyphoonHurricane (1)
1373–85135–157Hurricane (2)
1486–89159–165Severe tropical cyclone (4)Major hurricane (3)
1590–99167–183Intense tropical cyclone
16100–106185–196Major hurricane (4)
17107–114198–211Severe tropical cyclone (5)
115–119213–220Very intense tropical cycloneSuper typhoon
>120>222Super cyclonic stormMajor hurricane (5)

Enhanced Fujita scale

The Enhanced Fujita Scale (EF Scale) rates the strength of tornadoes in the United States based on the damage they cause. Below is the scale.

ScaleWind speedRelative frequencyPotential damage
EF065–85105–13753.5%Minor or no damage.

Peels surface off some roofs; some damage to gutters or siding; branches broken off trees; shallow-rooted trees pushed over.

Confirmed tornadoes with no reported damage (i.e., those that remain in open fields) are always rated EF0.

EF0 damage example EF0 tornado damage example (1).jpg
EF0 damage example
EF186–110138–17831.6%Moderate damage.

Roofs severely stripped; mobile homes overturned or badly damaged; loss of exterior doors; windows and other glass broken.

EF1 damage example EF1 tornado damage example.jpg
EF1 damage example
EF2111–135179–21810.7%Considerable damage.

Roofs torn off well-constructed houses; foundations of frame homes shifted; mobile homes completely destroyed; large trees snapped or uprooted; light-object missiles generated; cars lifted off ground.

EF2 damage example EF2 tornado damage example (1).jpg
EF2 damage example
EF3136–165219–2663.4%Severe damage.

Entire stories of well-constructed houses destroyed; severe damage to large buildings such as shopping malls; trains overturned; trees debarked; heavy cars lifted off the ground and thrown; structures with weak foundations are badly damaged.

EF3 damage example EF3 tornado damage example.jpg
EF3 damage example
EF4166–200267–3220.7%Extreme damage.

Well-constructed and whole frame houses completely leveled; cars and other large objects thrown and small missiles generated.

EF4 damage example EF4 tornado damage example.jpg
EF4 damage example
EF5>200>322<0.1%Total Destruction.

Strong-framed, well-built houses leveled off and foundations swept away; steel-reinforced concrete structures are critically damaged; tall buildings collapse or have severe structural deformations.

EF5 damage example EF5 tornado damage example.jpg
EF5 damage example

Station model

Wind plotting within a station model Wind barbs.gif
Wind plotting within a station model

The station model plotted on surface weather maps uses a wind barb to show both wind direction and speed. The wind barb shows the speed using "flags" on the end.

Winds are depicted as blowing from the direction the barb is facing. Therefore, a northeast wind will be depicted with a line extending from the cloud circle to the northeast, with flags indicating wind speed on the northeast end of this line. [23] Once plotted on a map, an analysis of isotachs (lines of equal wind speeds) can be accomplished. Isotachs are particularly useful in diagnosing the location of the jet stream on upper level constant pressure charts, and are usually located at or above the 300 hPa level. [24]

Wind power

Wind energy is the kinetic energy of the air in motion. The kinetic energy of a packet of air of mass m with velocity v is given by ½ m v2. To find the mass of the packet passing through an area A perpendicular its velocity (which could be the rotor area of a turbine), we multiply its volume after time t has passed with the air density ρ, which gives us m = Avtρ. So, we find that the total wind energy is:

Differentiating with respect to time to find the rate of increase of energy, we find that the total wind power is:

Wind power is thus proportional to the third power of the wind velocity.

Theoretical power captured by a wind turbine

Total wind power could be captured only if the wind velocity is reduced to zero. In a realistic wind turbine this is impossible, as the captured air must also leave the turbine. A relation between the input and output wind velocity must be considered. Using the concept of stream tube, the maximal achievable extraction of wind power by a wind turbine is 16/27 ≈ 59% of the total theoretical wind power [25] (see: Betz' law).

Practical wind turbine power

Further insufficiencies, such as rotor blade friction and drag, gearbox losses, generator and converter losses, reduce the power delivered by a wind turbine. The basic relation that the turbine power is (approximately) proportional to the third power of velocity remains.

Global climatology

The westerlies and trade winds Map prevailing winds on earth.png
The westerlies and trade winds
Winds are part of Earth's atmospheric circulation Earth Global Circulation.jpg
Winds are part of Earth's atmospheric circulation

Easterly winds, on average, dominate the flow pattern across the poles, westerly winds blow across the mid-latitudes of the earth, polewards of the subtropical ridge, while easterlies again dominate the tropics.

Directly under the subtropical ridge are the doldrums, or horse latitudes, where winds are lighter. Many of the Earth's deserts lie near the average latitude of the subtropical ridge, where descent reduces the relative humidity of the air mass. [26] The strongest winds are in the mid-latitudes where cold polar air meets warm air from the tropics.


The trade winds (also called trades) are the prevailing pattern of easterly surface winds found in the tropics towards the Earth's equator. [27] The trade winds blow predominantly from the northeast in the Northern Hemisphere and from the southeast in the Southern Hemisphere. [28] The trade winds act as the steering flow for tropical cyclones that form over the world's oceans. [29] Trade winds also steer African dust westward across the Atlantic Ocean into the Caribbean, as well as portions of southeast North America. [30]

A monsoon is a seasonal prevailing wind that lasts for several months within tropical regions. The term was first used in English in India, Bangladesh, Pakistan, and neighboring countries to refer to the big seasonal winds blowing from the Indian Ocean and Arabian Sea in the southwest bringing heavy rainfall to the area. [31] Its poleward progression is accelerated by the development off a heat low over the Asian, African, and North American continents during May through July, and over Australia in December. [32] [33] [34]

Westerlies and their impact

Benjamin Franklin's map of the Gulf Stream Franklingulfstream.jpg
Benjamin Franklin's map of the Gulf Stream

The Westerlies or the Prevailing Westerlies are the prevailing winds in the middle latitudes between 35 and 65 degrees latitude. These prevailing winds blow from the west to the east, [35] [36] and steer extratropical cyclones in this general manner. The winds are predominantly from the southwest in the Northern Hemisphere and from the northwest in the Southern Hemisphere. [28] They are strongest in the winter when the pressure is lower over the poles, and weakest during the summer and when pressures are higher over the poles. [37]

Together with the trade winds, the westerlies enabled a round-trip trade route for sailing ships crossing the Atlantic and Pacific Oceans, as the westerlies lead to the development of strong ocean currents on the western sides of oceans in both hemispheres through the process of western intensification. [38] These western ocean currents transport warm, sub tropical water polewards toward the polar regions. The westerlies can be particularly strong, especially in the southern hemisphere, where there is less land in the middle latitudes to cause the flow pattern to amplify, which slows the winds down. The strongest westerly winds in the middle latitudes are within a band known as the Roaring Forties, between 40 and 50 degrees latitude south of the equator. [39] The Westerlies play an important role in carrying the warm, equatorial waters and winds to the western coasts of continents, [40] [41] especially in the southern hemisphere because of its vast oceanic expanse.

Polar easterlies

The polar easterlies, also known as Polar Hadley cells, are dry, cold prevailing winds that blow from the high-pressure areas of the polar highs at the north and south poles towards the low-pressure areas within the Westerlies at high latitudes. Unlike the Westerlies, these prevailing winds blow from the east to the west, and are often weak and irregular. [42] Because of the low sun angle, cold air builds up and subsides at the pole creating surface high-pressure areas, forcing an equatorward outflow of air; [43] that outflow is deflected westward by the Coriolis effect.

Local considerations

Local winds around the world. These winds are formed through the heating of land (from mountains or flat terrain) Map local winds.png
Local winds around the world. These winds are formed through the heating of land (from mountains or flat terrain)

Sea and land breezes

A: Sea breeze (occurs at daytime), B: Land breeze (occurs at night) Diagrama de formacion de la brisa-breeze.svg
A: Sea breeze (occurs at daytime), B: Land breeze (occurs at night)

In coastal regions, sea breezes and land breezes can be important factors in a location's prevailing winds. The sea is warmed by the sun more slowly because of water's greater specific heat compared to land. [44] As the temperature of the surface of the land rises, the land heats the air above it by conduction. The warm air is less dense than the surrounding environment and so it rises. This causes a pressure gradient of about 2 millibars from the ocean to the land. The cooler air above the sea, now with higher sea level pressure, flows inland into the lower pressure, creating a cooler breeze near the coast. When large-scale winds are calm, the strength of the sea breeze is directly proportional to the temperature difference between the land mass and the sea. If an offshore wind of 8 knots (15 km/h) exists, the sea breeze is not likely to develop.

At night, the land cools off more quickly than the ocean because of differences in their specific heat values. This temperature change causes the daytime sea breeze to dissipate. When the temperature onshore cools below the temperature offshore, the pressure over the water will be lower than that of the land, establishing a land breeze, as long as an onshore wind is not strong enough to oppose it. [45]

Near mountains

Mountain wave schematic. The wind flows towards a mountain and produces a first oscillation (A). A second wave occurs further away and higher. The lenticular clouds form at the peak of the waves (B). Vol d'onde.svg
Mountain wave schematic. The wind flows towards a mountain and produces a first oscillation (A). A second wave occurs further away and higher. The lenticular clouds form at the peak of the waves (B).

Over elevated surfaces, heating of the ground exceeds the heating of the surrounding air at the same altitude above sea level, creating an associated thermal low over the terrain and enhancing any thermal lows that would have otherwise existed, [46] [47] and changing the wind circulation of the region. In areas where there is rugged topography that significantly interrupts the environmental wind flow, the wind circulation between mountains and valleys is the most important contributor to the prevailing winds. Hills and valleys substantially distort the airflow by increasing friction between the atmosphere and landmass by acting as a physical block to the flow, deflecting the wind parallel to the range just upstream of the topography, which is known as a barrier jet. This barrier jet can increase the low level wind by 45%. [48] Wind direction also changes because of the contour of the land. [49]

If there is a pass in the mountain range, winds will rush through the pass with considerable speed because of the Bernoulli principle that describes an inverse relationship between speed and pressure. The airflow can remain turbulent and erratic for some distance downwind into the flatter countryside. These conditions are dangerous to ascending and descending airplanes. [49] Cool winds accelerating through mountain gaps have been given regional names. In Central America, examples include the Papagayo wind, the Panama wind, and the Tehuano wind. In Europe, similar winds are known as the Bora, Tramontane, and Mistral. When these winds blow over open waters, they increase mixing of the upper layers of the ocean that elevates cool, nutrient rich waters to the surface, which leads to increased marine life. [50]

In mountainous areas, local distortion of the airflow becomes severe. Jagged terrain combines to produce unpredictable flow patterns and turbulence, such as rotors, which can be topped by lenticular clouds. Strong updrafts, downdrafts and eddies develop as the air flows over hills and down valleys. Orographic precipitation occurs on the windward side of mountains and is caused by the rising air motion of a large-scale flow of moist air across the mountain ridge, also known as upslope flow, resulting in adiabatic cooling and condensation. In mountainous parts of the world subjected to relatively consistent winds (for example, the trade winds), a more moist climate usually prevails on the windward side of a mountain than on the leeward or downwind side. Moisture is removed by orographic lift, leaving drier air on the descending and generally warming, leeward side where a rain shadow is observed. [51] Winds that flow over mountains down into lower elevations are known as downslope winds. These winds are warm and dry. In Europe downwind of the Alps, they are known as foehn. In Poland, an example is the halny wiatr. In Argentina, the local name for downsloped winds is zonda. In Java, the local name for such winds is koembang. In New Zealand, they are known as the Nor'west arch, and are accompanied by the cloud formation they are named after that has inspired artwork over the years. [52] In the Great Plains of the United States, these winds are known as a chinook. Downslope winds also occur in the foothills of the Appalachian mountains of the United States, [53] and they can be as strong as other downslope winds [54] and unusual compared to other foehn winds in that the relative humidity typically changes little due to the increased moisture in the source air mass. [55] In California, downslope winds are funneled through mountain passes, which intensify their effect, and examples include the Santa Ana and sundowner winds. Wind speeds during downslope wind effect can exceed 160 kilometers per hour (99 mph). [56]

Average wind speeds

As described earlier, prevailing and local winds are not spread evenly across the earth, which means that wind speeds also differ by region. In addition, the wind speed also increases with the altitude.

Wind power density

Nowadays, a yardstick used to determine the best locations for wind energy development is referred to as wind power density (WPD). It is a calculation relating to the effective force of the wind at a particular location, frequently expressed in terms of the elevation above ground level over a period of time. It takes into account wind velocity and mass. Color coded maps are prepared for a particular area are described as, for example, "mean annual power density at 50 meters". The results of the above calculation are included in an index developed by the National Renewable Energy Lab and referred to as "NREL CLASS". The larger the WPD calculation, the higher it is rated by class. [57] At the end of 2008, worldwide nameplate capacity of wind-powered generators was 120.8  gigawatts. [58] Although wind produced only about 1.5% of worldwide electricity use in 2009, [58] it is growing rapidly, having doubled in the three years between 2005 and 2008. In several countries it has achieved relatively high levels of penetration, accounting for approximately 19% of electricity production in Denmark, 10% in Spain and Portugal, and 7% in Germany and the Republic of Ireland in 2008. One study indicates that an entirely renewable energy supply based on 70% wind is attainable at today's power prices by linking wind farms with an HVDC supergrid. [59] Wind power has expanded quickly, its share of worldwide electricity usage at the end of 2014 was 3.1%. [60] In 2011 wind energy was also used to power the longest journey in a wind powered car which travelled a distance of 5,000 km (3,100 miles) from Perth to Melbourne in Australia. [61]


Hodograph plot of wind vectors at various heights in the troposphere, which is used to diagnose vertical wind shear Hodographe NOAA.PNG
Hodograph plot of wind vectors at various heights in the troposphere, which is used to diagnose vertical wind shear

Wind shear, sometimes referred to as wind gradient, is a difference in wind speed and direction over a relatively short distance in the Earth's atmosphere. [62] Wind shear can be broken down into vertical and horizontal components, with horizontal wind shear seen across weather fronts and near the coast, [63] and vertical shear typically near the surface, [64] though also at higher levels in the atmosphere near upper level jets and frontal zones aloft. [65]

Wind shear itself is a microscale meteorological phenomenon occurring over a very small distance, but it can be associated with mesoscale or synoptic scale weather features such as squall lines and cold fronts. It is commonly observed near microbursts and downbursts caused by thunderstorms, [66] weather fronts, areas of locally higher low level winds referred to as low level jets, near mountains, [67] radiation inversions that occur because of clear skies and calm winds, buildings, [68] wind turbines, [69] and sailboats. [70] Wind shear has a significant effect on the control of aircraft during take-off and landing, [71] and was a significant cause of aircraft accidents involving large loss of life within the United States. [66]

Sound movement through the atmosphere is affected by wind shear, which can bend the wave front, causing sounds to be heard where they normally would not, or vice versa. [72] Strong vertical wind shear within the troposphere also inhibits tropical cyclone development, [73] but helps to organize individual thunderstorms into living longer life cycles that can then produce severe weather. [74] The thermal wind concept explains how differences in wind speed with height are dependent on horizontal temperature differences, and explains the existence of the jet stream. [75]



Winds according to Aristotle. AristotelesCompass.PNG
Winds according to Aristotle.

As a natural force, the wind was often personified as one or more wind gods or as an expression of the supernatural in many cultures. Vayu is the Hindu God of Wind. [76] [77] The Greek wind gods include Boreas, Notus, Eurus, and Zephyrus. [77] Aeolus, in varying interpretations the ruler or keeper of the four winds, has also been described as Astraeus, the god of dusk who fathered the four winds with Eos, goddess of dawn. The ancient Greeks also observed the seasonal change of the winds, as evidenced by the Tower of the Winds in Athens. [77] Venti are the Roman gods of the winds. [78] Fūjin is the Japanese wind god and is one of the eldest Shinto gods. According to legend, he was present at the creation of the world and first let the winds out of his bag to clear the world of mist. [79] In Norse mythology, Njörðr is the god of the wind. [77] There are also four dvärgar (Norse dwarves), named Norðri, Suðri, Austri and Vestri, and probably the four stags of Yggdrasil, personify the four winds, and parallel the four Greek wind gods. [80] Stribog is the name of the Slavic god of winds, sky and air. He is said to be the ancestor (grandfather) of the winds of the eight directions. [77]

Kamikaze (神風) is a Japanese word, usually translated as divine wind, believed to be a gift from the gods. The term is first known to have been used as the name of a pair or series of typhoons that are said to have saved Japan from two Mongol fleets under Kublai Khan that attacked Japan in 1274 and again in 1281. [81] Protestant Wind is a name for the storm that deterred the Spanish Armada from an invasion of England in 1588 where the wind played a pivotal role, [82] or the favorable winds that enabled William of Orange to invade England in 1688. [83] During Napoleon's Egyptian Campaign, the French soldiers had a hard time with the khamsin wind: when the storm appeared "as a blood-stint in the distant sky", the natives went to take cover, while the French "did not react until it was too late, then choked and fainted in the blinding, suffocating walls of dust". [84] During the North African Campaign of the World War II, "allied and German troops were several times forced to halt in mid-battle because of sandstorms caused by khamsin ... Grains of sand whirled by the wind blinded the soldiers and created electrical disturbances that rendered compasses useless." [85]


RAF Exeter airfield on 20 May 1944, showing the layout of the runways that allow aircraft to take off and land into the wind Exeter-20may44.jpg
RAF Exeter airfield on 20 May 1944, showing the layout of the runways that allow aircraft to take off and land into the wind

There are many different forms of sailing ships, but they all have certain basic things in common. Except for rotor ships using the Magnus effect, every sailing ship has a hull, rigging and at least one mast to hold up the sails that use the wind to power the ship. [86] Ocean journeys by sailing ship can take many months, [87] and a common hazard is becoming becalmed because of lack of wind, [88] or being blown off course by severe storms or winds that do not allow progress in the desired direction. [89] A severe storm could lead to shipwreck, and the loss of all hands. [90] Sailing ships can only carry a certain quantity of supplies in their hold, so they have to plan long voyages carefully to include appropriate provisions, including fresh water. [91]

For aerodynamic aircraft which operate relative to the air, winds affect groundspeed, [92] and in the case of lighter-than-air vehicles, wind may play a significant or solitary role in their movement and ground track. [93] The velocity of surface wind is generally the primary factor governing the direction of flight operations at an airport, and airfield runways are aligned to account for the common wind direction(s) of the local area. While taking off with a tailwind may be necessary under certain circumstances, a headwind is generally desirable. A tailwind increases takeoff distance required and decreases the climb gradient. [94]

Power source

This wind turbine generates electricity from wind power. Windenergy.jpg
This wind turbine generates electricity from wind power.

Historically, the ancient Sinhalese of Anuradhapura and in other cities around Sri Lanka used the monsoon winds to power furnaces as early as 300 BCE. [95] The furnaces were constructed on the path of the monsoon winds to exploit the wind power, to bring the temperatures inside up to 1,200 °C (2,190 °F). A rudimentary windmill was used to power an organ in the first century CE. [96] The first practical windmills were later built in Sistan, Afghanistan, from the 7th century CE. These were vertical-axle windmills, which had long vertical driveshafts with rectangle shaped blades. [97] Made of six to twelve sails covered in reed matting or cloth material, these windmills were used to grind corn and draw up water, and were used in the gristmilling and sugarcane industries. [98] Horizontal-axle windmills were later used extensively in Northwestern Europe to grind flour beginning in the 1180s, and many Dutch windmills still exist. High altitude wind power is the focus of over 30 companies worldwide using tethered technology rather than ground-hugging compressive-towers. [99] Oil is being saved by using wind for powering cargo ships by use of the mechanical energy converted from the wind's kinetic energy using very large kites. [100]


Otto Lilienthal in flight Lilienthal in flight.jpg
Otto Lilienthal in flight

Wind figures prominently in several popular sports, including recreational hang gliding, hot air ballooning, kite flying, snowkiting, kite landboarding, kite surfing, paragliding, sailing, and windsurfing. In gliding, wind gradients just above the surface affect the takeoff and landing phases of flight of a glider. Wind gradient can have a noticeable effect on ground launches, also known as winch launches or wire launches. If the wind gradient is significant or sudden, or both, and the pilot maintains the same pitch attitude, the indicated airspeed will increase, possibly exceeding the maximum ground launch tow speed. The pilot must adjust the airspeed to deal with the effect of the gradient. [101] When landing, wind shear is also a hazard, particularly when the winds are strong. As the glider descends through the wind gradient on final approach to landing, airspeed decreases while sink rate increases, and there is insufficient time to accelerate prior to ground contact. The pilot must anticipate the wind gradient and use a higher approach speed to compensate for it. [102]

Role in the natural world

In arid climates, the main source of erosion is wind. [103] The general wind circulation moves small particulates such as dust across wide oceans thousands of kilometers downwind of their point of origin, [104] which is known as deflation. Westerly winds in the mid-latitudes of the planet drive the movement of ocean currents from west to east across the world's oceans. Wind has a very important role in aiding plants and other immobile organisms in dispersal of seeds, spores, pollen, etc. Although wind is not the primary form of seed dispersal in plants, it provides dispersal for a large percentage of the biomass of land plants.


A rock formation in the Altiplano, Bolivia, sculpted by wind erosion Im Salar de Uyuni.jpg
A rock formation in the Altiplano, Bolivia, sculpted by wind erosion

Erosion can be the result of material movement by the wind. There are two main effects. First, wind causes small particles to be lifted and therefore moved to another region. This is called deflation. Second, these suspended particles may impact on solid objects causing erosion by abrasion (ecological succession). Wind erosion generally occurs in areas with little or no vegetation, often in areas where there is insufficient rainfall to support vegetation. An example is the formation of sand dunes, on a beach or in a desert. [105] Loess is a homogeneous, typically nonstratified, porous, friable, slightly coherent, often calcareous, fine-grained, silty, pale yellow or buff, windblown (Aeolian) sediment. [106] It generally occurs as a widespread blanket deposit that covers areas of hundreds of square kilometers and tens of meters thick. Loess often stands in either steep or vertical faces. [107] Loess tends to develop into highly rich soils. Under appropriate climatic conditions, areas with loess are among the most agriculturally productive in the world. [108] Loess deposits are geologically unstable by nature, and will erode very readily. Therefore, windbreaks (such as big trees and bushes) are often planted by farmers to reduce the wind erosion of loess. [103]

Desert dust migration

During mid-summer (July in the northern hemisphere), the westward-moving trade winds south of the northward-moving subtropical ridge expand northwestward from the Caribbean into southeastern North America. When dust from the Sahara moving around the southern periphery of the ridge within the belt of trade winds moves over land, rainfall is suppressed and the sky changes from a blue to a white appearance, which leads to an increase in red sunsets. Its presence negatively impacts air quality by adding to the count of airborne particulates. [109] Over 50% of the African dust that reaches the United States affects Florida. [110] Since 1970, dust outbreaks have worsened because of periods of drought in Africa. There is a large variability in the dust transport to the Caribbean and Florida from year to year. [111] Dust events have been linked to a decline in the health of coral reefs across the Caribbean and Florida, primarily since the 1970s. [112] Similar dust plumes originate in the Gobi Desert, which combined with pollutants, spread large distances downwind, or eastward, into North America. [104]

There are local names for winds associated with sand and dust storms. The Calima carries dust on southeast winds into the Canary islands. [113] The Harmattan carries dust during the winter into the Gulf of Guinea. [114] The Sirocco brings dust from north Africa into southern Europe because of the movement of extratropical cyclones through the Mediterranean. [115] Spring storm systems moving across the eastern Mediterranean Sea cause dust to carry across Egypt and the Arabian peninsula, which are locally known as Khamsin. [116] The Shamal is caused by cold fronts lifting dust into the atmosphere for days at a time across the Persian Gulf states. [117]

Effect on plants

Tumbleweed blown against a fence Salsola tragus tumbleweed.jpg
Tumbleweed blown against a fence
In the montane forest of Olympic National Park, windthrow opens the canopy and increases light intensity on the understory. Coarse woody debris 6407.JPG
In the montane forest of Olympic National Park, windthrow opens the canopy and increases light intensity on the understory.

Wind dispersal of seeds, or anemochory, is one of the more primitive means of dispersal. Wind dispersal can take on one of two primary forms: seeds can float on the breeze or alternatively, they can flutter to the ground. [118] The classic examples of these dispersal mechanisms include dandelions ( Taraxacum spp., Asteraceae), which have a feathery pappus attached to their seeds and can be dispersed long distances, and maples ( Acer (genus) spp., Sapindaceae), which have winged seeds and flutter to the ground. An important constraint on wind dispersal is the need for abundant seed production to maximize the likelihood of a seed landing in a site suitable for germination. There are also strong evolutionary constraints on this dispersal mechanism. For instance, species in the Asteraceae on islands tended to have reduced dispersal capabilities (i.e., larger seed mass and smaller pappus) relative to the same species on the mainland. [119] Reliance upon wind dispersal is common among many weedy or ruderal species. Unusual mechanisms of wind dispersal include tumbleweeds. A related process to anemochory is anemophily, which is the process where pollen is distributed by wind. Large families of plants are pollinated in this manner, which is favored when individuals of the dominant plant species are spaced closely together. [120]

Wind also limits tree growth. On coasts and isolated mountains, the tree line is often much lower than in corresponding altitudes inland and in larger, more complex mountain systems, because strong winds reduce tree growth. High winds scour away thin soils through erosion, [121] as well as damage limbs and twigs. When high winds knock down or uproot trees, the process is known as windthrow. This is most likely on windward slopes of mountains, with severe cases generally occurring to tree stands that are 75 years or older. [122] Plant varieties near the coast, such as the Sitka spruce and sea grape, [123] are pruned back by wind and salt spray near the coastline. [124]

Wind can also cause plants damage through sand abrasion. Strong winds will pick up loose sand and topsoil and hurl it through the air at speeds ranging from 25 miles per hour (40 km/h) to 40 miles per hour (64 km/h). Such windblown sand causes extensive damage to plant seedlings because it ruptures plant cells, making them vulnerable to evaporation and drought. Using a mechanical sandblaster in a laboratory setting, scientists affiliated with the Agricultural Research Service studied the effects of windblown sand abrasion on cotton seedlings. The study showed that the seedlings responded to the damage created by the windblown sand abrasion by shifting energy from stem and root growth to the growth and repair of the damaged stems. [125] After a period of four weeks the growth of the seedling once again became uniform throughout the plant, as it was before the windblown sand abrasion occurred. [126]

Effect on animals

Cattle and sheep are prone to wind chill caused by a combination of wind and cold temperatures, when winds exceed 40 kilometers per hour (25 mph), rendering their hair and wool coverings ineffective. [127] Although penguins use both a layer of fat and feathers to help guard against coldness in both water and air, their flippers and feet are less immune to the cold. In the coldest climates such as Antarctica, emperor penguins use huddling behavior to survive the wind and cold, continuously alternating the members on the outside of the assembled group, which reduces heat loss by 50%. [128] Flying insects, a subset of arthropods, are swept along by the prevailing winds, [129] while birds follow their own course taking advantage of wind conditions, in order to either fly or glide. [130] As such, fine line patterns within weather radar imagery, associated with converging winds, are dominated by insect returns. [131] Bird migration, which tends to occur overnight within the lowest 7,000 feet (2,100 m) of the Earth's atmosphere, contaminates wind profiles gathered by weather radar, particularly the WSR-88D, by increasing the environmental wind returns by 15 knots (28 km/h) to 30 knots (56 km/h). [132]

Pikas use a wall of pebbles to store dry plants and grasses for the winter in order to protect the food from being blown away. [133] Cockroaches use slight winds that precede the attacks of potential predators, such as toads, to survive their encounters. Their cerci are very sensitive to the wind, and help them survive half of their attacks. [134] Elk have a keen sense of smell that can detect potential upwind predators at a distance of 0.5 miles (800 m). [135] Increases in wind above 15 kilometers per hour (9.3 mph) signals glaucous gulls to increase their foraging and aerial attacks on thick-billed murres. [136]

Sound generation

Wind causes the generation of sound. The movement of air causes movements of parts of natural objects, such as leaves or grass. These objects will produce sound if they touch each other. Even a soft wind will cause a low level of environmental noise. If the wind is blowing harder, it may produce howling sounds of varying frequencies. This may be caused by the wind blowing over cavities, or by vortices created in the air downstream of an object. [137] Especially on high buildings, many structural parts may be a cause of annoying noise at certain wind conditions. Examples of these parts are balconies, ventilation openings, roof openings or cables.

Damage from Hurricane Andrew Destruction following hurricane andrew.jpg
Damage from Hurricane Andrew

High winds are known to cause damage, depending upon the magnitude of their velocity and pressure differential. Wind pressures are positive on the windward side of a structure and negative on the leeward side. [138] Infrequent wind gusts can cause poorly designed suspension bridges to sway. When wind gusts are at a similar frequency to the swaying of the bridge, the bridge can be destroyed more easily, such as what occurred with the Tacoma Narrows Bridge in 1940. [139] Wind speeds as low as 23 knots (43 km/h) can lead to power outages due to tree branches disrupting the flow of energy through power lines. [140] While no species of tree is guaranteed to stand up to hurricane-force winds, those with shallow roots are more prone to uproot, and brittle trees such as eucalyptus, sea hibiscus, and avocado are more prone to damage. [141] Hurricane-force winds cause substantial damage to mobile homes, and begin to structurally damage homes with foundations. Winds of this strength due to downsloped winds off terrain have been known to shatter windows and sandblast paint from cars. [56] Once winds exceed 135 knots (250 km/h), homes completely collapse, and significant damage is done to larger buildings. Total destruction to man-made structures occurs when winds reach 175 knots (324 km/h). The Saffir–Simpson scale and Enhanced Fujita scale were designed to help estimate wind speed from the damage caused by high winds related to tropical cyclones and tornadoes, and vice versa. [142] [143]

Australia's Barrow Island holds the record for the strongest wind gust, reaching 408 km/h (253 mph) during tropical cyclone Olivia on 10 April 1996, surpassing the previous record of 372 km/h (231 mph) set on Mount Washington (New Hampshire) on the afternoon of 12 April 1934. [144] The most powerful gusts of wind on Earth were created by nuclear detonations. The blast wave is similar to a strong wind gust over the ground. The largest nuclear explosion (50–58 megatons at an altitude of about 13,000 feet (4,000 m)) generated a 20 bar blast pressure at ground zero, which is similar to a wind gust of 3,100 miles per hour (5,000 km/h).

Wildfire intensity increases during daytime hours. For example, burn rates of smoldering logs are up to five times greater during the day because of lower humidity, increased temperatures, and increased wind speeds. [145] Sunlight warms the ground during the day and causes air currents to travel uphill, and downhill during the night as the land cools. Wildfires are fanned by these winds and often follow the air currents over hills and through valleys. [146] United States wildfire operations revolve around a 24-hour fire day that begins at 10:00 a.m. because of the predictable increase in intensity resulting from the daytime warmth. [147]

In outer space

The solar wind is quite different from a terrestrial wind, in that its origin is the sun, and it is composed of charged particles that have escaped the sun's atmosphere. Similar to the solar wind, the planetary wind is composed of light gases that escape planetary atmospheres. Over long periods of time, the planetary wind can radically change the composition of planetary atmospheres.

The fastest wind ever recorded is coming from the accretion disc of the IGR J17091-3624 black hole. Its speed is 20,000,000 miles per hour (32,000,000 km/h), which is 3% of the speed of light. [148]

Planetary wind

Possible future for Earth due to the planetary wind: Venus Venuspioneeruv.jpg
Possible future for Earth due to the planetary wind: Venus

The hydrodynamic wind within the upper portion of a planet's atmosphere allows light chemical elements such as hydrogen to move up to the exobase, the lower limit of the exosphere, where the gases can then reach escape velocity, entering outer space without impacting other particles of gas. This type of gas loss from a planet into space is known as planetary wind. [149] Such a process over geologic time causes water-rich planets such as the Earth to evolve into planets like Venus. [150] Additionally, planets with hotter lower atmospheres could accelerate the loss rate of hydrogen. [151]

Solar wind

Rather than air, the solar wind is a stream of charged particles—a plasma—ejected from the upper atmosphere of the sun at a rate of 400 kilometers per second (890,000 mph). It consists mostly of electrons and protons with energies of about 1 keV. The stream of particles varies in temperature and speed with the passage of time. These particles are able to escape the sun's gravity, in part because of the high temperature of the corona, [152] but also because of high kinetic energy that particles gain through a process that is not well understood. The solar wind creates the Heliosphere, a vast bubble in the interstellar medium surrounding the Solar System. [153] Planets require large magnetic fields in order to reduce the ionization of their upper atmosphere by the solar wind. [151] Other phenomena caused by the solar wind include geomagnetic storms that can knock out power grids on Earth, [154] the aurorae such as the Northern Lights, [155] and the plasma tails of comets that always point away from the sun. [156]

On other planets

Strong 300 kilometers per hour (190 mph) winds at Venus's cloud tops circle the planet every four to five earth days. [157] When the poles of Mars are exposed to sunlight after their winter, the frozen CO2 sublimates, creating significant winds that sweep off the poles as fast as 400 kilometers per hour (250 mph), which subsequently transports large amounts of dust and water vapor over its landscape. [158] Other Martian winds have resulted in cleaning events and dust devils. [159] [160] On Jupiter, wind speeds of 100 meters per second (220 mph) are common in zonal jet streams. [161] Saturn's winds are among the Solar System's fastest. Cassini–Huygens data indicated peak easterly winds of 375 meters per second (840 mph). [162] On Uranus, northern hemisphere wind speeds reach as high as 240 meters per second (540 mph) near 50 degrees north latitude. [163] [164] [165] At the cloud tops of Neptune, prevailing winds range in speed from 400 meters per second (890 mph) along the equator to 250 meters per second (560 mph) at the poles. [166] At 70° S latitude on Neptune, a high-speed jet stream travels at a speed of 300 meters per second (670 mph). [167] The fastest wind on any known planet is on HD 80606 b located 190 light years away, where it blows at more than 11,000 mph or 5 km/s. [168]

See also

Related Research Articles

Cyclone large scale air mass that rotates around a strong center of low pressure

In meteorology, a cyclone is a large scale air mass that rotates around a strong center of low atmospheric pressure. Cyclones are characterized by inward spiraling winds that rotate about a zone of low pressure. The largest low-pressure systems are polar vortices and extratropical cyclones of the largest scale. Warm-core cyclones such as tropical cyclones and subtropical cyclones also lie within the synoptic scale. Mesocyclones, tornadoes and dust devils lie within smaller mesoscale. Upper level cyclones can exist without the presence of a surface low, and can pinch off from the base of the tropical upper tropospheric trough during the summer months in the Northern Hemisphere. Cyclones have also been seen on extraterrestrial planets, such as Mars and Neptune. Cyclogenesis is the process of cyclone formation and intensification. Extratropical cyclones begin as waves in large regions of enhanced mid-latitude temperature contrasts called baroclinic zones. These zones contract and form weather fronts as the cyclonic circulation closes and intensifies. Later in their life cycle, extratropical cyclones occlude as cold air masses undercut the warmer air and become cold core systems. A cyclone's track is guided over the course of its 2 to 6 day life cycle by the steering flow of the subtropical jet stream.

Thunderstorm type of weather

A thunderstorm, also known as an electrical storm or a lightning storm, is a storm characterized by the presence of lightning and its acoustic effect on the Earth's atmosphere, known as thunder. Relatively weak thunderstorms are sometimes called thundershowers. Thunderstorms occur in a type of cloud known as a cumulonimbus. They are usually accompanied by strong winds, and often produce heavy rain and sometimes snow, sleet, or hail, but some thunderstorms produce little precipitation or no precipitation at all. Thunderstorms may line up in a series or become a rainband, known as a squall line. Strong or severe thunderstorms include some of the most dangerous weather phenomena, including large hail, strong winds, and tornadoes. Some of the most persistent severe thunderstorms, known as supercells, rotate as do cyclones. While most thunderstorms move with the mean wind flow through the layer of the troposphere that they occupy, vertical wind shear sometimes causes a deviation in their course at a right angle to the wind shear direction.

Surface weather analysis

Surface weather analysis is a special type of weather map that provides a view of weather elements over a geographical area at a specified time based on information from ground-based weather stations.

Anticyclone opposite to a cyclone

An anticyclone is a weather phenomenon defined by the United States National Weather Service's glossary as "a large-scale circulation of winds around a central region of high atmospheric pressure, clockwise in the Northern Hemisphere, counterclockwise in the Southern Hemisphere". Effects of surface-based anticyclones include clearing skies as well as cooler, drier air. Fog can also form overnight within a region of higher pressure. Mid-tropospheric systems, such as the subtropical ridge, deflect tropical cyclones around their periphery and cause a temperature inversion inhibiting free convection near their center, building up surface-based haze under their base. Anticyclones aloft can form within warm core lows such as tropical cyclones, due to descending cool air from the backside of upper troughs such as polar highs, or from large scale sinking such as the subtropical ridge. The evolution of an anticyclone depends on a few variables such as its size, intensity, moist-convection, Coriolis force etc.

High-pressure area region where the atmospheric pressure at the surface of the planet is greater than its surrounding environment

A high-pressure area, high or anticyclone is a region where the atmospheric pressure at the surface of the planet is greater than its surrounding environment.

A low-pressure area, low, depression or cyclone is a region on the topographic map where the atmospheric pressure is lower than that of surrounding locations. Low-pressure systems form under areas of wind divergence that occur in the upper levels of the troposphere. The formation process of a low-pressure area is known as cyclogenesis. Within the field of meteorology, atmospheric divergence aloft occurs in two areas. The first area is on the east side of upper troughs, which form half of a Rossby wave within the Westerlies. A second area of wind divergence aloft occurs ahead of embedded shortwave troughs, which are of smaller wavelength. Diverging winds aloft ahead of these troughs cause atmospheric lift within the troposphere below, which lowers surface pressures as upward motion partially counteracts the force of gravity.

Trade winds

The trade winds are the prevailing pattern of surface winds from the east toward the west (easterly) found in the tropics, within the lower portion of the Earth's atmosphere, in the lower part of the troposphere near the Earth's equator. The trade winds blow predominantly from the northeast in the Northern Hemisphere and from the southeast in the Southern Hemisphere, strengthening during the winter and when the Arctic oscillation is in its warm phase. Trade winds have been used by captains of sailing ships to cross the world's oceans for centuries, and enabled colonial expansion into the Americas and trade routes to become established across the Atlantic and Pacific oceans.

Prevailing winds

Prevailing winds are winds that blow predominantly from an individual direction over a particular point on the Earth's surface. The dominant winds are the trends in direction of wind with the highest speed over a particular point on the Earth's surface. A region's prevailing and dominant winds are enacted by global patterns of movement in the Earth's atmosphere. In general, easterly flow occurs at low and medium latitudes globally. In the mid-latitudes, westerly winds are dominant, and their strength is largely determined by the polar cyclone. In areas where winds tend to be light, the sea breeze/land breeze cycle is the most important to the prevailing wind; in areas which have variable terrain, mountain and valley breezes dominate the wind pattern. Highly elevated surfaces can induce a thermal low, which then augments the environmental wind flow.

Pressure system relative peak or lull in the sea level pressure distribution

A pressure system is a relative peak or lull in the sea level pressure distribution. The surface pressure at sea level varies minimally, with the lowest value measured 87 kilopascals (26 inHg) and the highest recorded 108.57 kilopascals (32.06 inHg). High- and low-pressure systems evolve due to interactions of temperature differentials in the atmosphere, temperature differences between the atmosphere and water within oceans and lakes, the influence of upper-level disturbances, as well as the amount of solar heating or radiationized cooling an area receives. Pressure systems cause weather to be experienced locally. Low-pressure systems are associated with clouds and precipitation that minimize temperature changes throughout the day, whereas high-pressure systems normally associate with dry weather and mostly clear skies with larger diurnal temperature changes due to greater radiation at night and greater sunshine during the day. Pressure systems are analyzed by those in the field of meteorology within surface weather maps.

Outflow boundary

An outflow boundary, also known as a gust front, is a storm-scale or mesoscale boundary separating thunderstorm-cooled air (outflow) from the surrounding air; similar in effect to a cold front, with passage marked by a wind shift and usually a drop in temperature and a related pressure jump. Outflow boundaries can persist for 24 hours or more after the thunderstorms that generated them dissipate, and can travel hundreds of kilometers from their area of origin. New thunderstorms often develop along outflow boundaries, especially near the point of intersection with another boundary. Outflow boundaries can be seen either as fine lines on weather radar imagery or else as arcs of low clouds on weather satellite imagery. From the ground, outflow boundaries can be co-located with the appearance of roll clouds and shelf clouds.

Weather front boundary separating two masses of air of different densities

A weather front is a boundary separating two masses of air of different densities, and is the principal cause of meteorological phenomena outside the tropics. In surface weather analyses, fronts are depicted using various colored triangles and half-circles, depending on the type of front. The air masses separated by a front usually differ in temperature and humidity.


A rainband is a cloud and precipitation structure associated with an area of rainfall which is significantly elongated. Rainbands can be stratiform or convective, and are generated by differences in temperature. When noted on weather radar imagery, this precipitation elongation is referred to as banded structure. Rainbands within tropical cyclones are curved in orientation. Tropical cyclone rainbands contain showers and thunderstorms that, together with the eyewall and the eye, constitute a hurricane or tropical storm. The extent of rainbands around a tropical cyclone can help determine the cyclone's intensity.

Extratropical cyclone type of cyclone

Extratropical cyclones, sometimes called mid-latitude cyclones or wave cyclones, are low-pressure areas which, along with the anticyclones of high-pressure areas, drive the weather over much of the Earth. Extratropical cyclones are capable of producing anything from cloudiness and mild showers to heavy gales, thunderstorms, blizzards, and tornadoes. These types of cyclones are defined as large scale (synoptic) low pressure weather systems that occur in the middle latitudes of the Earth. In contrast with tropical cyclones, extratropical cyclones produce rapid changes in temperature and dew point along broad lines, called weather fronts, about the center of the cyclone.

Air-mass thunderstorm

An air-mass thunderstorm, also called an "ordinary", "single cell", or "garden variety" thunderstorm, is a thunderstorm that is generally weak and usually not severe. These storms form in environments where at least some amount of Convective Available Potential Energy (CAPE) is present, but very low levels of wind shear and helicity. The lifting source, which is a crucial factor in thunderstorm development, is usually the result of uneven heating of the surface, though they can be induced by weather fronts and other low-level boundaries associated with wind convergence. The energy needed for these storms to form comes in the form of insolation, or solar radiation. Air-mass thunderstorms do not move quickly, last no longer than an hour, and have the threats of lightning, as well as showery light, moderate, or heavy rainfall. Heavy rainfall can interfere with microwave transmissions within the atmosphere.

Severe weather

Severe weather refers to any dangerous meteorological phenomena with the potential to cause damage, serious social disruption, or loss of human life. Types of severe weather phenomena vary, depending on the latitude, altitude, topography, and atmospheric conditions. High winds, hail, excessive precipitation, and wildfires are forms and effects of severe weather, as are thunderstorms, downbursts, tornadoes, waterspouts, tropical cyclones, and extratropical cyclones. Regional and seasonal severe weather phenomena include blizzards (snowstorms), ice storms, and duststorms.

Atmospheric convection

Atmospheric convection is the result of a parcel-environment instability, or temperature difference layer in the atmosphere. Different lapse rates within dry and moist air masses lead to instability. Mixing of air during the day which expands the height of the planetary boundary layer leads to increased winds, cumulus cloud development, and decreased surface dew points. Moist convection leads to thunderstorm development, which is often responsible for severe weather throughout the world. Special threats from thunderstorms include hail, downbursts, and tornadoes.

Outline of meteorology Overview of and topical guide to meteorology

The following outline is provided as an overview of and topical guide to meteorology:

Thermal low

Thermal lows, or heat lows, are non-frontal low-pressure areas that occur over the continents in the subtropics during the warm season, as the result of intense heating when compared to their surrounding environments. Thermal lows occur near the Sonoran Desert, on the Mexican plateau, in California's Great Central Valley, the Sahara, over north-west Argentina in South America, over the Kimberley region of north-west Australia, the Iberian peninsula, and the Tibetan plateau.

Glossary of meteorology Wikimedia list article

This glossary of meteorology is a list of terms and concepts relevant to meteorology and the atmospheric sciences, their sub-disciplines, and related fields.


  1. JetStream (2008). "Origin of Wind". National Weather Service Southern Region Headquarters. Retrieved 2009-02-16.
  2. Makarieva, Anastassia; V. G. Gorshkov, D. Sheil, A. D. Nobre, B.-L. Li (February 2013). "Where do winds come from? A new theory on how water vapor condensation influences atmospheric pressure and dynamics". Atmospheric Chemistry and Physics. 13 (2): 1039–1056. arXiv: 1004.0355 . Bibcode:2013ACP....13.1039M. doi:10.5194/acp-13-1039-2013 . Retrieved 2013-02-01.CS1 maint: Multiple names: authors list (link)
  3. Glossary of Meteorology (2009). "Geostrophic wind". American Meteorological Society. Archived from the original on 2007-10-16. Retrieved 2009-03-18.
  4. Glossary of Meteorology (2009). "Thermal wind". American Meteorological Society. Archived from the original on 2011-07-17. Retrieved 2009-03-18.
  5. Glossary of Meteorology (2009). "Ageostrophic wind". American Meteorological Society. Archived from the original on 2011-08-22. Retrieved 2009-03-18.
  6. Glossary of Meteorology (2009). "Gradient wind". American Meteorological Society. Archived from the original on 2008-05-28. Retrieved 2009-03-18.
  7. JetStream (2008). "How to read weather maps". National Weather Service. Archived from the original on 2012-06-22. Retrieved 2009-05-16.
  8. Glossary of Meteorology (2009). "Wind vane". American Meteorological Society. Archived from the original on 2007-10-18. Retrieved 2009-03-17.
  9. Glossary of Meteorology (2009). "Wind sock". American Meteorological Society. Archived from the original on 2012-06-22. Retrieved 2009-03-17.
  10. Glossary of Meteorology (2009). "Anemometer". American Meteorological Society. Archived from the original on 2011-06-06. Retrieved 2009-03-17.
  11. Glossary of Meteorology (2009). "Pitot tube". American Meteorological Society. Archived from the original on 2012-06-22. Retrieved 2009-03-17.
  12. Tropical Cyclone Weather Services Program (2006-06-01). "Tropical cyclone definitions" (PDF). National Weather Service. Retrieved 2006-11-30.
  13. Office of the Federal Coordinator for Meteorology. Federal Meteorological Handbook No. 1 – Surface Weather Observations and Reports September 2005 Appendix A: Glossary. Retrieved 2008-04-06.
  14. Sharad K. Jain; Pushpendra K. Agarwal; Vijay P. Singh (2007). Hydrology and Water Resources of India. Springer. p. 187. ISBN   978-1-4020-5179-1 . Retrieved 2009-04-22.
  15. Jan-Hwa Chu (1999). "Section 2. Intensity Observation and Forecast Errors". United States Navy . Retrieved 2008-07-04.
  16. Glossary of Meteorology (2009). "Rawinsonde". American Meteorological Society. Archived from the original on 2011-06-06. Retrieved 2009-03-17.
  17. Glossary of Meteorology (2009). "Pibal". American Meteorological Society. Archived from the original on 2007-11-10. Retrieved 2009-03-17.
  18. 1 2 Walter J. Saucier (2003). Principles of Meteorological Analysis. Courier Dover Publications. ISBN   978-0-486-49541-5 . Retrieved 2009-01-09.
  19. Glossary of Meteorology (2009). "G". American Meteorological Society. Archived from the original on 2012-06-22. Retrieved 2009-03-18.
  20. Glossary of Meteorology (2009). "Storm". American Meteorological Society. Archived from the original on 2007-10-15. Retrieved 2009-03-18.
  21. Coastguard Southern Region (2009). "The Beaufort Wind Scale". Archived from the original on 2008-11-18. Retrieved 2009-03-18.
  22. "Decoding the station model". Hydrometeorological Prediction Center . National Centers for Environmental Prediction. 2009. Retrieved 2007-05-16.
  23. "How to read weather maps". JetStream. National Weather Service. 2008. Archived from the original on 2012-06-22. Retrieved 2009-06-27.
  24. Terry T. Lankford (2000). Aviation Weather Handbook. McGraw-Hill Professional. ISBN   978-0-07-136103-3 . Retrieved 2008-01-22.
  25. The Physics of Wind Turbines. Kira Grogg Carleton College (2005) p. 8. (PDF). Retrieved 2011-11-03.
  26. Michael A. Mares (1999). Encyclopedia of Deserts. University of Oklahoma Press. p. 121. ISBN   978-0-8061-3146-7 . Retrieved 2009-06-20.
  27. Glossary of Meteorology (2000). "trade winds". American Meteorological Society. Archived from the original on 2008-12-11. Retrieved 2008-09-08.
  28. 1 2 Ralph Stockman Tarr and Frank Morton McMurry (1909). Advanced geography. W.W. Shannon, State Printing. p. 246. Retrieved 2009-04-15.
  29. Joint Typhoon Warning Center (2006). "3.3 JTWC Forecasting Philosophies" (PDF). United States Navy. Retrieved 2007-02-11.
  30. "African Dust Called A Major Factor Affecting Southeast U.S. Air Quality". Science Daily . 1999-07-14. Retrieved 2007-06-10.
  31. Glossary of Meteorology (2009). "Monsoon". American Meteorological Society. Archived from the original on 2008-03-22. Retrieved 2008-03-14.
  32. "Chapter-II Monsoon-2004: Onset, Advancement and Circulation Features" (PDF). National Centre for Medium Range Forecasting. 2004-10-23. Archived from the original (PDF) on 2009-08-04. Retrieved 2008-05-03.
  33. "Monsoon". Australian Broadcasting Corporation. 2000. Archived from the original on 2001-02-23. Retrieved 2008-05-03.
  34. Alex DeCaria (2007-10-02). "Lesson 4 – Seasonal-mean Wind Fields" (PDF). Millersville Meteorology. Retrieved 2008-05-03.
  35. Glossary of Meteorology (2009). "Westerlies". American Meteorological Society. Archived from the original on 2010-06-22. Retrieved 2009-04-15.
  36. Sue Ferguson (2001-09-07). "Climatology of the Interior Columbia River Basin" (PDF). Interior Columbia Basin Ecosystem Management Project. Archived from the original (PDF) on 2009-05-15. Retrieved 2009-09-12.
  37. Halldór Björnsson (2005). "Global circulation". Veðurstofu Íslands. Archived from the original on 2011-08-07. Retrieved 2008-06-15.
  38. National Environmental Satellite, Data, and Information Service (2009). "Investigating the Gulf Stream". North Carolina State University. Archived from the original on 2010-05-03. Retrieved 2009-05-06.CS1 maint: Multiple names: authors list (link)
  39. Stuart Walker (1998). The sailor's wind. W. W. Norton & Company. p. 91. ISBN   978-0-393-04555-0 . Retrieved 2009-06-17.
  40. Barbie Bischof; Arthur J. Mariano; Edward H. Ryan (2003). "The North Atlantic Drift Current". The National Oceanographic Partnership Program . Retrieved 2008-09-10.
  41. Erik A. Rasmussen; John Turner (2003). Polar Lows. Cambridge University Press. p. 68.
  42. Glossary of Meteorology (2009). "Polar easterlies". American Meteorological Society. Archived from the original on 2012-06-22. Retrieved 2009-04-15.
  43. Michael E. Ritter (2008). "The Physical Environment: Global scale circulation". University of Wisconsin–Stevens Point. Archived from the original on 2009-05-06. Retrieved 2009-04-15.
  44. Steve Ackerman (1995). "Sea and Land Breezes". University of Wisconsin. Retrieved 2006-10-24.
  45. JetStream: An Online School For Weather (2008). "The Sea Breeze". National Weather Service. Archived from the original on 2006-09-23. Retrieved 2006-10-24.
  46. National Weather Service Forecast Office in Tucson, Arizona (2008). "What is a monsoon?". National Weather Service Western Region Headquarters. Retrieved 2009-03-08.
  47. Douglas G. Hahn and Syukuro Manabe (1975). "The Role of Mountains in the South Asian Monsoon Circulation". Journal of the Atmospheric Sciences . 32 (8): 1515–1541. Bibcode:1975JAtS...32.1515H. doi:10.1175/1520-0469(1975)032<1515:TROMIT>2.0.CO;2.
  48. J. D. Doyle (1997). "The influence of mesoscale orography on a coastal jet and rainband". Monthly Weather Review . 125 (7): 1465–1488. Bibcode:1997MWRv..125.1465D. doi:10.1175/1520-0493(1997)125<1465:TIOMOO>2.0.CO;2.
  49. 1 2 National Center for Atmospheric Research (2006). "T-REX: Catching the Sierra's waves and rotors". University Corporation for Atmospheric Research. Archived from the original on 2006-11-21. Retrieved 2006-10-21.
  50. Anthony Drake (2008-02-08). "The Papaguayo Wind". NASA Goddard Earth Sciences Data and Information Services Center. Archived from the original on 2009-06-14. Retrieved 2009-06-16.
  51. Michael Pidwirny (2008). "CHAPTER 8: Introduction to the Hydrosphere (e). Cloud Formation Processes". Physical Geography. Archived from the original on 2008-12-20. Retrieved 2009-01-01.
  52. Michael Dunn (2003). New Zealand Painting. Auckland University Press. p. 93. ISBN   978-1-86940-297-6 . Retrieved 2009-06-21.
  53. Gaffin, David M. (2007). "Foehn Winds That Produced Large Temperature Differences near the Southern Appalachian Mountains". Weather and Forecasting. 22 (1): 145–159. Bibcode:2007WtFor..22..145G. CiteSeerX . doi:10.1175/WAF970.1.
  54. Gaffin, David M. (2009). "On High Winds and Foehn Warming Associated with Mountain-Wave Events in the Western Foothills of the Southern Appalachian Mountains". Weather and Forecasting. 24 (1): 53–75. Bibcode:2009WtFor..24...53G. doi:10.1175/2008WAF2007096.1.
  55. Gaffin, David M. (2002). "Unexpected Warming Induced by Foehn Winds in the Lee of the Smoky Mountains". Weather and Forecasting. 17 (4): 907–915. doi:10.1175/1520-0434(2002)017<0907:UWIBFW>2.0.CO;2.
  56. 1 2 Rene Munoz (2000-04-10). "Boulder's downslope winds". University Corporation for Atmospheric Research. Archived from the original on 2012-06-22. Retrieved 2009-06-16.
  57. Kansas Wind Energy Project, Affiliated Atlantic & Western Group Inc, 5250 W 94th Terrace, Prairie Village, Kansas 66207
  58. 1 2 World Wind Energy Association (2009-02-06). "120 Gigawatt of wind turbines globally contribute to secure electricity generation". Press release. Archived from the original on 2009-02-07. Retrieved 2009-02-06.
  59. David Strahan (2009-03-11). "From AC to DC: Going green with supergrids". New Scientist . Retrieved 2009-03-13.
  60. pg31
  61. Glenday, Craig (2013). Guinness world records 2014. The Jim Pattison Group. p. 002. ISBN   978-1-908843-15-9.
  62. D. C. Beaudette (1988). "FAA Advisory Circular Pilot Wind Shear Guide via the Internet Wayback Machine" (PDF). Federal Aviation Administration . Retrieved 2009-03-18.
  63. David M. Roth (2006). "Unified Surface Analysis Manual" (PDF). Hydrometeorological Prediction Center . Retrieved 2006-10-22.
  64. Glossary of Meteorology (2007). "E". American Meteorological Society. Archived from the original on 2012-06-22. Retrieved 2007-06-03.
  65. "Jet Streams in the UK". BBC. 2009. Archived from the original on 2009-02-14. Retrieved 2009-06-20.
  66. 1 2 Cheryl W. Cleghorn (2004). "Making the Skies Safer From Windshear". NASA Langley Air Force Base. Archived from the original on August 23, 2006. Retrieved 2006-10-22.
  67. National Center for Atmospheric Research (Spring 2006). "T-REX: Catching the Sierra's waves and rotors". University Corporation for Atmospheric Research Quarterly. Archived from the original on 2009-02-21. Retrieved 2009-06-21.
  68. Hans M. Soekkha (1997). Aviation Safety. VSP. p. 229. ISBN   978-90-6764-258-3 . Retrieved 2009-06-21.
  69. Robert Harrison (2001). Large Wind Turbines. Chichester: John Wiley & Sons. p. 30. ISBN   978-0-471-49456-0.
  70. Ross Garrett (1996). The Symmetry of Sailing. Dobbs Ferry: Sheridan House. pp. 97–99. ISBN   978-1-57409-000-0.
  71. Gail S. Langevin (2009). "Wind Shear". National Aeronautic and Space Administration. Archived from the original on October 9, 2007. Retrieved 2007-10-09.
  72. Rene N. Foss (June 1978). "Ground Plane Wind Shear Interaction on Acoustic Transmission". WA-RD 033.1. Washington State Department of Transportation. Retrieved 2007-05-30.
  73. University of Illinois (1999). "Hurricanes" . Retrieved 2006-10-21.
  74. University of Illinois (1999). "Vertical Wind Shear" . Retrieved 2006-10-21.
  75. Integrated Publishing (2007). "Unit 6—Lesson 1: Low-Level Wind Shear" . Retrieved 2009-06-21.
  76. Laura Gibbs (2007-10-16). "Vayu". Encyclopedia for Epics of Ancient India. Retrieved 2009-04-09.
  77. 1 2 3 4 5 Michael Jordan (1993). Encyclopedia of Gods: Over 2, 500 Deities of the World. New York: Facts on File. pp. 5, 45, 80, 187–188, 243, 280, 295. ISBN   978-0-8160-2909-9.
  78. Theoi Greek Mythology (2008). "Anemi: Greek Gods of the Winds". Aaron Atsma. Retrieved 2009-04-10.
  79. John Boardman (1994). The Diffusion of Classical Art in Antiquity. Princeton University Press. ISBN   978-0-691-03680-9.
  80. Andy Orchard (1997). Dictionary of Norse Myth and Legend. Cassell. ISBN   978-0-304-36385-8.
  81. History Detectives (2008). "Feature – Kamikaze Attacks". PBS. Archived from the original on 2008-10-25. Retrieved 2009-03-21.
  82. Colin Martin; Geoffrey Parker (1999). The Spanish Armada. Manchester University Press. pp. 144–181. ISBN   978-1-901341-14-0 . Retrieved 2009-06-20.
  83. S. Lindgrén & J. Neumann (1985). "Great Historical Events That Were Significantly Affected by the Weather: 7, "Protestant Wind"—"Popish Wind": The Revolusion of 1688 in England". Bulletin of the American Meteorological Society. 66 (6): 634–644. Bibcode:1985BAMS...66..634L. doi:10.1175/1520-0477(1985)066<0634:GHETWS>2.0.CO;2.
  84. Nina Burleigh (2007). Mirage. Harper. p. 135. ISBN   978-0-06-059767-2.
  85. Jan DeBlieu (1998). Wind. Houghton Mifflin Harcourt. p. 57. ISBN   978-0-395-78033-6.
  86. Ernest Edwin Speight & Robert Morton Nance (1906). Britain's Sea Story, B.C. 55-A.D. 1805. Hodder and Stoughton. p. 30. Retrieved 2009-03-19.
  87. Brandon Griggs & Jeff King (2009-03-09). "Boat made of plastic bottles to make ocean voyage". CNN. Retrieved 2009-03-19.
  88. Jerry Cardwell (1997). Sailing Big on a Small Sailboat. Sheridan House, Inc. p. 118. ISBN   978-1-57409-007-9 . Retrieved 2009-03-19.
  89. Brian Lavery & Patrick O'Brian (1989). Nelson's navy. Naval Institute Press. p. 191. ISBN   978-1-59114-611-7 . Retrieved 2009-06-20.
  90. Underwater Archaeology Kids' Corner (2009). "Shipwrecks, Shipwrecks Everywhere". Wisconsin Historical Society . Retrieved 2009-03-19.
  91. Carla Rahn Phillips (1993). The Worlds of Christopher Columbus. Cambridge University Press. p. 67. ISBN   978-0-521-44652-5 . Retrieved 2009-03-19.
  92. Tom Benson (2008). "Relative Velocities: Aircraft Reference". NASA Glenn Research Center . Retrieved 2009-03-19.
  93. Library of Congress (2006-01-06). "The Dream of Flight". Archived from the original on 2009-07-28. Retrieved 2009-06-20.
  94. "Flight Paths" (PDF). Bristol International Airport. 2004. Archived from the original (PDF) on 2009-03-26. Retrieved 2009-03-19.
  95. G. Juleff (1996). "An ancient wind powered iron smelting technology in Sri Lanka". Nature. 379 (3): 60–63. Bibcode:1996Natur.379...60J. doi:10.1038/379060a0.
  96. A.G. Drachmann (1961). "Heron's Windmill". Centaurus. 7 (2): 145–151. Bibcode:1960Cent....7..145R. doi:10.1111/j.1600-0498.1960.tb00263.x.
  97. Ahmad Y Hassan and Donald Routledge Hill (1986). Islamic Technology: An illustrated history. Cambridge University Press. p. 54. ISBN   978-0-521-42239-0.
  98. Donald Routledge Hill (May 1991). Mechanical Engineering in the Medieval Near East. Scientific American. pp. 64–69.
  99. Dietrich Lohrmann (1995). "Von der östlichen zur westlichen Windmühle". Archiv für Kulturgeschichte. 77 (1): 1–30. doi:10.7788/akg.1995.77.1.1.
  100. SkySails. SkySails. Retrieved 2011-11-03.
  101. Glider Flying Handbook. U.S. Government Printing Office, Washington, D.C.: U.S. Federal Aviation Administration. 2003. pp. 7–16. FAA-8083-13_GFH. Archived from the original on 2005-12-18. Retrieved 2009-06-17.
  102. Derek Piggott (1997). Gliding: a Handbook on Soaring Flight. Knauff & Grove. pp. 85–86, 130–132. ISBN   978-0-9605676-4-5.
  103. 1 2 Vern Hofman & Dave Franzen (1997). "Emergency Tillage to Control Wind Erosion". North Dakota State University Extension Service. Retrieved 2009-03-21.
  104. 1 2 James K. B. Bishop, Russ E. Davis, and Jeffrey T. Sherman (2002). "Robotic Observations of Dust Storm Enhancement of Carbon Biomass in the North Pacific" (PDF). Science. 298 (5594): 817–821. Bibcode:2002Sci...298..817B. doi:10.1126/science.1074961. PMID   12399588. Archived from the original (PDF) on 2010-06-01. Retrieved 2009-06-20.CS1 maint: Multiple names: authors list (link)
  105. United States Geological Survey (2004). "Dunes – Getting Started" . Retrieved 2009-03-21.
  106. F. von Richthofen (1882). "On the mode of origin of the loess". Geological Magazine (Decade II). 9 (7): 293–305. Bibcode:1882GeoM....9..293R. doi:10.1017/S001675680017164X.
  107. K.E.K. Neuendorf; J.P. Mehl, Jr. & J.A. Jackson (2005). Glossary of Geology. Springer-Verlag, New York. p. 779. ISBN   978-3-540-27951-8.
  108. Arthur Getis; Judith Getis and Jerome D. Fellmann (2000). Introduction to Geography, Seventh Edition. McGraw-Hill. p. 99. ISBN   978-0-697-38506-2.
  109. Science Daily (1999-07-14). "African Dust Called A Major Factor Affecting Southeast U.S. Air Quality" . Retrieved 2007-06-10.
  110. Science Daily (2001-06-15). "Microbes And The Dust They Ride In On Pose Potential Health Risks" . Retrieved 2007-06-10.
  111. (2003). "Study Says African Dust Affects Climate in U.S., Caribbean" (PDF). Archived from the original (PDF) on 2007-06-20. Retrieved 2007-06-10.
  112. U. S. Geological Survey (2006). "Coral Mortality and African Dust" . Retrieved 2007-06-10.
  113. Weather Online (2009). "Calima" . Retrieved 2009-06-17.
  114. Henrik Breuning-Madsen and Theodore W. Awadzi (2005). "Harmattan dust deposition and particle size in Ghana". Catena. 63 (1): 23–38. doi:10.1016/j.catena.2005.04.001.
  115. Weather Online (2009). "Sirocco (Scirocco)" . Retrieved 2009-06-17.
  116. Bill Giles (O.B.E) (2009). "The Khamsin". BBC. Archived from the original on 2009-03-13. Retrieved 2009-06-17.
  117. Thomas J. Perrone (August 1979). "Table of Contents: Wind Climatology of the Winter Shamal". United States Navy. Retrieved 2009-06-17.
  118. J. Gurevitch; S. M. Scheiner & G. A. Fox (2006). Plant Ecology, 2nd ed. Sinauer Associates, Inc., Massachusetts.
  119. M. L. Cody and J. M. Overton (1996). "Short-term evolution of reduced dispersal in island plant populations". Journal of Ecology. 84 (1): 53–61. doi:10.2307/2261699. JSTOR   2261699.CS1 maint: Uses authors parameter (link)
  120. A. J. Richards (1997). Plant Breeding Systems. Taylor & Francis. p. 88. ISBN   978-0-412-57450-4 . Retrieved 2009-06-19.
  121. Leif Kullman (2005). "Wind-Conditioned 20th Century Decline of Birch Treeline Vegetation in the Swedish Scandes" (PDF). Arctic. 58 (3): 286–294. doi:10.14430/arctic430 . Retrieved 2009-06-20.
  122. Mathieu Bouchard; David Pothier & Jean-Claude Ruel (2009). "Stand-replacing windthrow in the boreal forests of eastern Quebec". Canadian Journal of Forest Research. 39 (2): 481–487. doi:10.1139/X08-174.
  123. Michael A. Arnold (2009). "Coccoloba uvifera" (PDF). Texas A&M University . Retrieved 2009-06-20.
  124. National Park Service (2006-09-01). "Plants". Department of the Interior . Retrieved 2009-06-20.
  125. ARS Studies Effect of Wind Sandblasting on Cotton Plants / January 26, 2010 / News from the USDA Agricultural Research Service. Retrieved 2011-11-03.
  126. "ARS Studies Effect of Wind Sandblasting on Cotton Plants". USDA Agricultural Research Service. January 26, 2010.
  127. D. R. Ames & L. W. lnsley (1975). "Wind Chill Effect for Cattle and Sheep". Journal of Animal Science. 40 (1): 161–165. doi:10.2527/jas1975.401161x. hdl:2097/10789. PMID   1110212.
  128. Australian Antarctic Division (2008-12-08). "Adapting to the Cold". Australian Government Department of the Environment, Water, Heritage, and the Arts Australian Antarctic Division. Archived from the original on 2009-06-15. Retrieved 2009-06-20.
  129. Diana Yates (2008). "Birds migrate together at night in dispersed flocks, new study indicates". University of Illinois at Urbana – Champaign. Retrieved 2009-04-26.
  130. Gary Ritchison (2009-01-04). "BIO 554/754 Ornithology Lecture Notes 2 – Bird Flight I". Eastern Kentucky University . Retrieved 2009-06-19.
  131. Bart Geerts & Dave Leon (2003). "P5A.6 Fine-Scale Vertical Structure of a Cold Front As Revealed By Airborne 95 GHZ Radar" (PDF). University of Wyoming . Retrieved 2009-04-26.
  132. Thomas A. Niziol (August 1998). "Contamination of WSR-88D VAD Winds Due to Bird Migration: A Case Study" (PDF). Eastern Region WSR-88D Operations Note No. 12. Retrieved 2009-04-26.
  133. Jennifer Owen (1982). Feeding strategy. University of Chicago Press. pp. 34–35. ISBN   978-0-226-64186-7.
  134. Robert C. Eaton (1984). Neural mechanisms of startle behavior. Springer. pp. 98–99. ISBN   978-0-306-41556-2 . Retrieved 2009-06-19.
  135. Bob Robb; Gerald Bethge; Gerry Bethge (2000). The Ultimate Guide to Elk Hunting. Globe Pequot. p. 161. ISBN   978-1-58574-180-9 . Retrieved 2009-06-19.
  136. H. G. Gilchrist; A. J. Gaston & J. N. M. Smith (1998). "Wind and prey nest sites as foraging constraints on an avian predator, the glaucous gull". Ecology. 79 (7): 2403–2414. doi:10.1890/0012-9658(1998)079[2403:WAPNSA]2.0.CO;2. JSTOR   176831.
  137. "How does wind produce sounds?".
  139. T. P. Grazulis (2001). The tornado. University of Oklahoma Press. pp. 126–127. ISBN   978-0-8061-3258-7 . Retrieved 2009-05-13.
  140. Hans Dieter Betz; Ulrich Schumann; Pierre Laroche (2009). Lightning: Principles, Instruments and Applications. Springer. pp. 202–203. ISBN   978-1-4020-9078-3 . Retrieved 2009-05-13.
  141. Derek Burch (2006-04-26). "How to Minimize Wind Damage in the South Florida Garden". University of Florida. Retrieved 2009-05-13.
  142. National Hurricane Center (2006-06-22). "Saffir-Simpson Hurricane Scale Information". National Oceanic and Atmospheric Administration . Retrieved 2007-02-25.
  143. Storm Prediction Center (2007-02-01). "Enhanced F Scale for Tornado Damage" . Retrieved 2009-05-13.
  144. "Info note No.58 — World Record Wind Gust: 408 km/h". World Meteorological Association. 2010-01-22. Archived from the original on 2013-01-20.
  145. Feranando de Souza Costa & David Sandberg (2004). "Mathematical model of a smoldering log" (PDF). Combustion and Flame. 139 (3): 227–238 [228]. doi:10.1016/j.combustflame.2004.07.009 . Retrieved 2009-02-06.
  146. National Wildfire Coordinating Group (2007-02-08). NWCG Communicator's Guide for Wildland Fire Management: Fire Education, Prevention, and Mitigation Practices, Wildland Fire Overview (PDF). p. 5. Retrieved 2008-12-11.
  147. National Wildfire Coordinating Group (2008). Glossary of Wildland Fire Terminology (PDF). p. 73. Archived from the original (PDF) on 2008-08-21. Retrieved 2008-12-18.
  148. Ashley King; et al. (February 21, 2012). "Chandra Finds Fastest Winds from Stellar Black Hole". NASA. Retrieved September 27, 2012.
  149. Ruth Murray-Clay (2008). "Atmospheric Escape Hot Jupiters & Interactions Between Planetary and Stellar Winds" (PDF). Boston University. Archived from the original (PDF) on 2009-08-04. Retrieved 2009-05-05.
  150. E. Chassefiere (1996). "Hydrodynamic escape of hydrogen from a hot water-rich atmosphere: The case of Venus". Journal of Geophysical Research. 101 (11): 26039–26056. Bibcode:1996JGR...10126039C. doi:10.1029/96JE01951.
  151. 1 2 Rudolf Dvořák (2007). Extrasolar Planets. Wiley-VCH. pp. 139–140. ISBN   978-3-527-40671-5 . Retrieved 2009-05-05.
  152. David H. Hathaway (2007). "The Solar Wind". National Aeronautic and Space Administration Marshall Space Flight Center . Retrieved 2009-03-19.
  153. Robert Roy Britt (2000-03-15). "A Glowing Discovery at the Forefront of Our Plunge Through Space".
  154. John G. Kappenman; et al. (1997). "Geomagnetic Storms Can Threaten Electric Power Grid". Earth in Space. 9 (7): 9–11. Archived from the original on 2008-06-11. Retrieved 2009-03-19.
  155. T. Neil Davis (1976-03-22). "Cause of the Aurora". Alaska Science Forum. Archived from the original on 2012-06-22. Retrieved 2009-03-19.
  156. Donald K. Yeomans (2005). "World Book at NASA: Comets". National Aeronautics and Space Administration. Archived from the original on 2015-03-21. Retrieved 2009-06-20.
  157. W. B. Rossow, A. D. del Genio, T. Eichler (1990). "Cloud-tracked winds from Pioneer Venus OCPP images". Journal of the Atmospheric Sciences. 47 (17): 2053–2084. Bibcode:1990JAtS...47.2053R. doi:10.1175/1520-0469(1990)047<2053:CTWFVO>2.0.CO;2.CS1 maint: Multiple names: authors list (link)
  158. NASA (2004-12-13). "Mars Rovers Spot Water-Clue Mineral, Frost, Clouds" . Retrieved 2006-03-17.
  159. NASA – NASA Mars Rover Churns Up Questions With Sulfur-Rich Soil. Retrieved 2011-11-03.
  160. David, Leonard (12 March 2005). "Spirit Gets A Dust Devil Once-Over". Retrieved 2006-12-01.
  161. A. P. Ingersoll; T. E. Dowling; P. J. Gierasch; G. S. Orton; P. L. Read; A. Sanchez-Lavega; A. P. Showman; A. A. Simon-Miller; A. R. Vasavada (2003-07-29). Dynamics of Jupiter's Atmosphere (PDF). Lunar & Planetary Institute. Retrieved 2007-02-01.
  162. C.C. Porco; et al. (2005). "Cassini Imaging Science: Initial Results on Saturn's Atmosphere". Science. 307 (5713): 1243–1247. Bibcode:2005Sci...307.1243P. doi:10.1126/science.1107691. PMID   15731441.
  163. L. A. Sromovsky & P. M. Fry (2005). "Dynamics of cloud features on Uranus". Icarus. 179 (2): 459–484. arXiv: 1503.03714 . Bibcode:2005Icar..179..459S. doi:10.1016/j.icarus.2005.07.022.
  164. H.B. Hammel; I. de Pater; S. Gibbard; G.W. Lockwoodd; K. Rages (2005). "Uranus in 2003: Zonal winds, banded structure, and discrete features" (PDF). Icarus. 175 (2): 534–545. Bibcode:2005Icar..175..534H. doi:10.1016/j.icarus.2004.11.012.
  165. H.B. Hammel; K. Rages; G.W. Lockwoodd; E. Karkoschka; I. de Pater (2001). "New Measurements of the Winds of Uranus". Icarus. 153 (2): 229–235. Bibcode:2001Icar..153..229H. doi:10.1006/icar.2001.6689.
  166. Linda T. Elkins-Tanton (2006). Uranus, Neptune, Pluto, and the Outer Solar System. New York: Chelsea House. pp. 79–83. ISBN   978-0-8160-5197-7.
  167. Jonathan I. Lunine (1993). "The Atmospheres of Uranus and Neptune". Annual Review of Astronomy and Astrophysics. 31: 217–263. Bibcode:1993ARA&A..31..217L. doi:10.1146/annurev.aa.31.090193.001245.
  168. "Exoplanet Sees Extreme Heat Waves". 28 January 2009.