Long-term mean precipitation by month

In meteorology, precipitation (also known as one of the classes of hydrometeors, which are atmospheric water phenomena) is any product of the condensation of atmospheric water vapor that falls under gravity.^[1] The main forms of precipitation include drizzle (sometimes called mist - especially "Scotch mist"), rain, sleet, snow, graupel and hail. Precipitation occurs when a local portion of the atmosphere becomes saturated with water vapour, so that the water condenses and "precipitates". Thus, fog and mist (except when the terms are used to mean "drizzle") are not precipitation but suspensions, because the water vapour does not condense sufficiently to precipitate. Likewise, frost does not precipitate out of the atmosphere but rises from the ground; so it, too, is not precipitation.^[2] Two processes, possibly acting together, can lead to air becoming saturated: cooling the air or adding water vapour to the air. Generally, precipitation will fall to the surface; an exception is Virga which evaporates before reaching the surface. Precipitation forms as smaller droplets coalesce via collision with other rain drops or ice crystals within a cloud. Rain drops range in size from oblate, pancake-like shapes for larger drops, to small spheres for smaller drops. Unlike raindrops, snowflakes grow in a variety of different shapes and patterns, determined by the temperature and humidity characteristics of the air the snowflake moves through on its way to the ground. While snow and ice pellets require temperatures close to the ground to be near or below freezing, hail can occur during much warmer temperature regimes due to the process of its formation.

Moisture overriding associated with weather fronts is an overall major method of precipitation production. If enough moisture and upward motion is present, precipitation falls from convective clouds such as cumulonimbus and can organize into narrow rainbands. Where relatively warm water bodies are present, for example due to water evaporation from lakes, lake-effect snowfall becomes a concern downwind of the warm lakes within the cold cyclonic flow around the backside of extratropical cyclones. Lake-effect snowfall can be locally heavy. Thundersnow is possible within a cyclone's comma head and within lake effect precipitation bands. In mountainous areas, heavy precipitation is possible where upslope flow is maximized within windward sides of the terrain at elevation. On the leeward side of mountains, desert climates can exist due to the dry air caused by compressional heating. The movement of the monsoon trough, or intertropical convergence zone, brings rainy seasons to savannah climes.

Precipitation is a major component of the water cycle, and is responsible for depositing the fresh water on the planet. Approximately 505,000 cubic kilometres (121,000 cu mi) of water falls as precipitation each year; 398,000 cubic kilometres (95,000 cu mi) of it over the oceans and 107,000 cubic kilometres (26,000 cu mi) over land.^[3] Given the Earth's surface area, that means the globally averaged annual precipitation is 990 millimetres (39 in), but over land it is only 715 millimetres (28.1 in). Climate classification systems such as the Köppen climate classification system use average annual rainfall to help differentiate between differing climate regimes. The urban heat island effect may lead to increased rainfall, both in amounts and intensity, downwind of cities. Global warming is also causing changes in the precipitation pattern globally. Precipitation may occur on other celestial bodies, e.g. when it gets cold, Mars has precipitation which most likely takes the form of ice needles, rather than rain or snow.^[4]

Hydrometeor[link]

This anvil-shaped Cumulonimbus incus cloud is composed of hydrometeors.

Any phenomenon which was at some point produced due to condensation or precipitation of moisture within the Earth's atmosphere is known as a hydrometeor. Particles composed of fallen precipitation which fell onto the Earth's surface can become hydrometeors if blown off the landscape by wind. Formations due to condensation such as clouds, haze, fog, and mist are composed of hydrometeors. All precipitation types are hydrometeors by definition, including virga, which is precipitation which evaporates before reaching the ground. Particles removed from the Earth's surface by wind such as blowing snow and blowing sea spray are also hydrometeors.^[5]

Hydrometeors are unrelated to meteors, which are objects from outer space which have entered the Earth's atmosphere and have produced a light phenomenon.^[6]

Types[link]

A thunderstorm with heavy precipitation

Precipitation is a major component of the water cycle, and is responsible for depositing most of the fresh water on the planet. Approximately 505,000 km³ (121,000 cu mi) of water falls as precipitation each year, 398,000 km³ (95,000 cu mi) of it over the oceans.^[3] Given the Earth's surface area, that means the globally averaged annual precipitation is 990 millimetres (39 in).

Mechanisms of producing precipitation include convective, stratiform,^[7] and orographic rainfall.^[8] Convective processes involve strong vertical motions that can cause the overturning of the atmosphere in that location within an hour and cause heavy precipitation,^[9] while stratiform processes involve weaker upward motions and less intense precipitation. Precipitation can be divided into three categories, based on whether it falls as liquid water, liquid water that freezes on contact with the surface, or ice. Mixtures of different types of precipitation, including types in different categories, can fall simultaneously. Liquid forms of precipitation include rain and drizzle. Rain or drizzle that freezes on contact within a subfreezing air mass is called "freezing rain" or "freezing drizzle". Frozen forms of precipitation include snow, ice needles, ice pellets, hail, and graupel.^[10]

How the air becomes saturated[link]

Cooling air to its dew point[link]

Late-summer rainstorm in Denmark

The dew point is the temperature to which a parcel must be cooled in order to become saturated, and (unless super-saturation occurs) condenses to water.^[11] Water vapour normally begins to condense on condensation nuclei such as dust, ice, and salt in order to form clouds. An elevated portion of a frontal zone forces broad areas of lift, which form clouds decks such as altostratus or cirrostratus. Stratus is a stable cloud deck which tends to form when a cool, stable air mass is trapped underneath a warm air mass. It can also form due to the lifting of advection fog during breezy conditions.^[12]

There are four main mechanisms for cooling the air to its dew point: adiabatic cooling, conductive cooling, radiational cooling, and evaporative cooling. Adiabatic cooling occurs when air rises and expands.^[13] The air can rise due to convection, large-scale atmospheric motions, or a physical barrier such as a mountain (orographic lift). Conductive cooling occurs when the air comes into contact with a colder surface,^[14] usually by being blown from one surface to another, for example from a liquid water surface to colder land. Radiational cooling occurs due to the emission of infrared radiation, either by the air or by the surface underneath.^[15] Evaporative cooling occurs when moisture is added to the air through evaporation, which forces the air temperature to cool to its wet-bulb temperature, or until it reaches saturation.^[16]

Adding moisture to the air[link]

The main ways water vapour is added to the air are: wind convergence into areas of upward motion,^[9] precipitation or virga falling from above,^[17] daytime heating evaporating water from the surface of oceans, water bodies or wet land,^[18] transpiration from plants,^[19] cool or dry air moving over warmer water,^[20] and lifting air over mountains.^[21]

Formation[link]

Condensation and coalescence are important parts of the water cycle.

Raindrops[link]

Coalescence occurs when water droplets fuse to create larger water droplets, or when water droplets freeze onto an ice crystal, which is known as the Bergeron process. The fall rate of very small droplets is negligible, hence clouds do not fall out of the sky; precipitation will only occur when these coalesce into larger drops. When air turbulence occurs, water droplets collide, producing larger droplets. As these larger water droplets descend, coalescence continues, so that drops become heavy enough to overcome air resistance and fall as rain.^[22]

Raindrops have sizes ranging from 0.1 millimetres (0.0039 in) to 9 millimetres (0.35 in) mean diameter, above which they tend to break up. Smaller drops are called cloud droplets, and their shape is spherical. As a raindrop increases in size, its shape becomes more oblate, with its largest cross-section facing the oncoming airflow. Contrary to the cartoon pictures of raindrops, their shape does not resemble a teardrop.^[23] Intensity and duration of rainfall are usually inversely related, i.e., high intensity storms are likely to be of short duration and low intensity storms can have a long duration.^[24][25] Rain drops associated with melting hail tend to be larger than other rain drops.^[26] The METAR code for rain is RA, while the coding for rain showers is SHRA.^[27]

Ice pellets[link]

An accumulation of ice pellets

Ice pellets or sleet are a form of precipitation consisting of small, translucent balls of ice. Ice pellets are usually (but not always) smaller than hailstones.^[28] They often bounce when they hit the ground, and generally do not freeze into a solid mass unless mixed with freezing rain. The METAR code for ice pellets is PL.^[27]

Ice pellets form when a layer of above-freezing air exists with sub-freezing air both above and below it. This causes the partial or complete melting of any snowflakes falling through the warm layer. As they fall back into the sub-freezing layer closer to the surface, they re-freeze into ice pellets. However, if the sub-freezing layer beneath the warm layer is too small, the precipitation will not have time to re-freeze, and freezing rain will be the result at the surface. A temperature profile showing a warm layer above the ground is most likely to be found in advance of a warm front during the cold season,^[29] but can occasionally be found behind a passing cold front.

Hail[link]

A large hailstone, about 6 cm (2.36 in) in diameter

Like other precipitation, hail forms in storm clouds when supercooled water droplets freeze on contact with condensation nuclei, such as dust or dirt. The storm's updraft blows the hailstones to the upper part of the cloud. The updraft dissipates and the hailstones fall down, back into the updraft, and are lifted again. Hail has a diameter of 5 millimetres (0.20 in) or more.^[30] Within METAR code, GR is used to indicate larger hail, of a diameter of at least 6.4 millimetres (0.25 in). GR is derived from the French word grêle. Smaller-sized hail, as well as snow pellets, use the coding of GS, which is short for the French word grésil.^[27] Stones just larger than golf ball-sized are one of the most frequently reported hail sizes.^[31] Hailstones can grow to 15 centimetres (6 in) and weigh more than .5 kilograms (1.1 lb).^[32] In large hailstones, latent heat released by further freezing may melt the outer shell of the hailstone. The hailstone then may undergo 'wet growth', where the liquid outer shell collects other smaller hailstones.^[33] The hailstone gains an ice layer and grows increasingly larger with each ascent. Once a hailstone becomes too heavy to be supported by the storm's updraft, it falls from the cloud.^[34]

Snowflakes[link]

Snowflake viewed in an optical microscope

Snow crystals form when tiny supercooled cloud droplets (about 10 μm in diameter) freeze. Once a droplet has frozen, it grows in the supersaturated environment. Because water droplets are more numerous than the ice crystals the crystals are able to grow to hundreds of micrometers or millimeters in size at the expense of the water droplets. This process is known as the Wegner-Bergeron-Findeison process. The corresponding depletion of water vapor causes the droplets to evaporate, meaning that the ice crystals grow at the droplets' expense. These large crystals are an efficient source of precipitation, since they fall through the atmosphere due to their mass, and may collide and stick together in clusters, or aggregates. These aggregates are snowflakes, and are usually the type of ice particle that falls to the ground.^[35] Guinness World Records list the world's largest snowflakes as those of January 1887 at Fort Keogh, Montana; allegedly one measured 38 cm (15 inches) wide.^[36] The exact details of the sticking mechanism remain a subject of research.

Although the ice is clear, scattering of light by the crystal facets and hollows/imperfections mean that the crystals often appear white in color due to diffuse reflection of the whole spectrum of light by the small ice particles.^[37] The shape of the snowflake is determined broadly by the temperature and humidity at which it is formed.^[35] Rarely, at a temperature of around −2 °C (28 °F), snowflakes can form in threefold symmetry—triangular snowflakes.^[38] The most common snow particles are visibly irregular, although near-perfect snowflakes may be more common in pictures because they are more visually appealing. No two snowflakes are alike,^[39] which grow at different rates and in different patterns depending on the changing temperature and humidity within the atmosphere that the snowflake falls through on its way to the ground.^[40] The METAR code for snow is SN, while snow showers are coded SHSN.^[27]

Diamond dust[link]

Diamond dust, also known as ice needles or ice crystals, forms at temperatures approaching −40 °F (−40 °C) due to air with slightly higher moisture from aloft mixing with colder, surface based air.^[41] They are made of simple ice crystals that are hexagonal in shape.^[42] The METAR identifier for diamond dust within international hourly weather reports is IC.^[27]

Causes[link]

Frontal activity[link]

Stratiform or dynamic precipitation occurs as a consequence of slow ascent of air in synoptic systems (on the order of cm/s), such as over surface cold fronts, and over and ahead of warm fronts. Similar ascent is seen around tropical cyclones outside of the eyewall, and in comma-head precipitation patterns around mid-latitude cyclones.^[43] A wide variety of weather can be found along an occluded front, with thunderstorms possible, but usually their passage is associated with a drying of the air mass. Occluded fronts usually form around mature low-pressure areas.^[44] Precipitation may occur on celestial bodies other than Earth. When it gets cold, Mars has precipitation that most likely takes the form of ice needles, rather than rain or snow.^[4]

Convection[link]

Convective precipitation

Convective rain, or showery precipitation, occurs from convective clouds, e.g., cumulonimbus or cumulus congestus. It falls as showers with rapidly changing intensity. Convective precipitation falls over a certain area for a relatively short time, as convective clouds have limited horizontal extent. Most precipitation in the tropics appears to be convective; however, it has been suggested that stratiform precipitation also occurs.^[25][43] Graupel and hail indicate convection.^[45] In mid-latitudes, convective precipitation is intermittent and often associated with baroclinic boundaries such as cold fronts, squall lines, and warm fronts.^[46]

Orographic effects[link]

Orographic precipitation

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, 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 (see katabatic wind) on the descending and generally warming, leeward side where a rain shadow is observed.^[21]

In Hawaii, Mount Waiʻaleʻale, on the island of Kauai, is notable for its extreme rainfall, as it has the second highest average annual rainfall on Earth, with 460 inches (12,000 mm).^[47] Storm systems affect the state with heavy rains between October and March. Local climates vary considerably on each island due to their topography, divisible into windward (Koʻolau) and leeward (Kona) regions based upon location relative to the higher mountains. Windward sides face the east to northeast trade winds and receive much more rainfall; leeward sides are drier and sunnier, with less rain and less cloud cover.^[48]

In South America, the Andes mountain range blocks Pacific moisture that arrives in that continent, resulting in a desertlike climate just downwind across western Argentina.^[49] The Sierra Nevada range creates the same effect in North America forming the Great Basin and Mojave Deserts.^[50][51]

Snow[link]

Lake-effect snow bands near the Korean Peninsula

Extratropical cyclones can bring cold and dangerous conditions with heavy rain and snow with winds exceeding 119 km/h (74 mph),^[52] (sometimes referred to as windstorms in Europe). The band of precipitation that is associated with their warm front is often extensive, forced by weak upward vertical motion of air over the frontal boundary which condenses as it cools and produces precipitation within an elongated band,^[53] which is wide and stratiform, meaning falling out of nimbostratus clouds.^[54] When moist air tries to dislodge an arctic air mass, overrunning snow can result within the poleward side of the elongated precipitation band. In the Northern Hemisphere, poleward is towards the North Pole, or north. Within the Southern Hemisphere, poleward is towards the South Pole, or south.

Southwest of extratropical cyclones, curved cyclonic flow bringing cold air across the relatively warm water bodies can lead to narrow lake-effect snow bands. Those bands bring strong localized snowfall which can be understood as follows: Large water bodies such as lakes efficiently store heat that results in significant temperature differences (larger than 13 °C or 23 °F) between the water surface and the air above.^[55] Because of this temperature difference, warmth and moisture are transported upward, condensing into vertically oriented clouds (see satellite picture) which produce snow showers. The temperature decrease with height and cloud depth are directly affected by both the water temperature and the large-scale environment. The stronger the temperature decrease with height, the deeper the clouds get, and the greater the precipitation rate becomes.^[56]

In mountainous areas, heavy snowfall accumulates when air is forced to ascend the mountains and squeeze out precipitation along their windward slopes, which in cold conditions, falls in the form of snow. Because of the ruggedness of terrain, forecasting the location of heavy snowfall remains a significant challenge.^[57]

Within the tropics[link]

The wet, or rainy, season is the time of year, covering one or more months, when most of the average annual rainfall in a region falls.^[58] The term green season is also sometimes used as a euphemism by tourist authorities.^[59] Areas with wet seasons are dispersed across portions of the tropics and subtropics.^[60] Savanna climates and areas with monsoon regimes have wet summers and dry winters. Tropical rainforests technically do not have dry or wet seasons, since their rainfall is equally distributed through the year.^[61] Some areas with pronounced rainy seasons will see a break in rainfall mid-season when the intertropical convergence zone or monsoon trough move poleward of their location during the middle of the warm season.^[24] When the wet season occurs during the warm season, or summer, rain falls mainly during the late afternoon and early evening hours. The wet season is a time when air quality improves,^[62] freshwater quality improves,^[63][64] and vegetation grows significantly. Soil nutrients diminish and erosion increases.^[24] Animals have adaptation and survival strategies for the wetter regime. The previous dry season leads to food shortages into the wet season, as the crops have yet to mature. Developing countries have noted that their populations show seasonal weight fluctuations due to food shortages seen before the first harvest, which occurs late in the wet season.^[65]

Tropical cyclones, a source of very heavy rainfall, consist of large air masses several hundred miles across with low pressure at the centre and with winds blowing inward towards the centre in either a clockwise direction (southern hemisphere) or counterclockwise (northern hemisphere).^[66] Although cyclones can take an enormous toll in lives and personal property, they may be important factors in the precipitation regimes of places they impact, as they may bring much-needed precipitation to otherwise dry regions.^[67] Areas in their path can receive a year's worth of rainfall from a tropical cyclone passage.^[68]

Large-scale geographical distribution[link]

On the large scale, the highest precipitation amounts outside topography fall in the tropics, closely tied to the Intertropical Convergence Zone, itself the ascending branch of the Hadley cell. Mountainous locales near the equator in Colombia are amongst the wettest places on Earth.^[69] North and south of this are regions of descending air that form subtropical ridges where precipitation is low;^[70] the land surface underneath is usually arid, which forms most of the Earth's deserts.^[71] An exception to this rule is in Hawaii, where upslope flow due to the trade winds lead to one of the wettest locations on Earth.^[72] Otherwise, the flow of the Westerlies into the Rocky Mountains lead to the wettest, and at elevation snowiest,^[73] locations within North America. In Asia during the wet season, the flow of moist air into the Himalayas leads to some of the greatest rainfall amounts measured on Earth in northeast India.

Measurement[link]

Standard rain gauge

The standard way of measuring rainfall or snowfall is the standard rain gauge, which can be found in 100 mm (4 in) plastic and 200 mm (8 in) metal varieties.^[74] The inner cylinder is filled by 25 mm (1 in) of rain, with overflow flowing into the outer cylinder. Plastic gauges have markings on the inner cylinder down to 0.25 mm (0.01 in) resolution, while metal gauges require use of a stick designed with the appropriate 0.25 mm (0.01 in) markings. After the inner cylinder is filled, the amount inside it is discarded, then filled with the remaining rainfall in the outer cylinder until all the fluid in the outer cylinder is gone, adding to the overall total until the outer cylinder is empty. These gauges are used in the winter by removing the funnel and inner cylinder and allowing snow and freezing rain to collect inside the outer cylinder. Some add anti-freeze to their gauge so they do not have to melt the snow or ice that falls into the gauge.^[75] Once the snowfall/ice is finished accumulating, or as 300 mm (12 in) is approached, one can either bring it inside to melt, or use lukewarm water to fill the inner cylinder with in order to melt the frozen precipitation in the outer cylinder, keeping track of the warm fluid added, which is subsequently subtracted from the overall total once all the ice/snow is melted.^[76]

Other types of gauges include the popular wedge gauge (the cheapest rain gauge and most fragile), the tipping bucket rain gauge, and the weighing rain gauge.^[77] The wedge and tipping bucket gauges will have problems with snow. Attempts to compensate for snow/ice by warming the tipping bucket meet with limited success, since snow may sublimate if the gauge is kept much above freezing. Weighing gauges with antifreeze should do fine with snow, but again, the funnel needs to be removed before the event begins. For those looking to measure rainfall the most inexpensively, a can that is cylindrical with straight sides will act as a rain gauge if left out in the open, but its accuracy will depend on what ruler is used to measure the rain with. Any of the above rain gauges can be made at home, with enough know-how.^[78]

When a precipitation measurement is made, various networks exist across the United States and elsewhere where rainfall measurements can be submitted through the Internet, such as CoCoRAHS or GLOBE.^[79][80] If a network is not available in the area where one lives, the nearest local weather office will likely be interested in the measurement.^[81]

Return period[link]

The likelihood or probability of an event with a specified intensity and duration, is called the return period or frequency.^[82] The intensity of a storm can be predicted for any return period and storm duration, from charts based on historic data for the location.^[83] The term 1 in 10 year storm describes a rainfall event which is rare and is only likely to occur once every 10 years, so it has a 10 percent likelihood any given year. The rainfall will be greater and the flooding will be worse than the worst storm expected in any single year. The term 1 in 100 year storm describes a rainfall event which is extremely rare and which will occur with a likelihood of only once in a century, so has a 1 percent likelihood in any given year. The rainfall will be extreme and flooding to be worse than a 1 in 10 year event. As with all probability events, it is possible to have multiple "1 in 100 Year Storms" in a single year.^[84]

Role in Köppen climate classification[link]

Updated Köppen-Geiger climate map^[85]

Af   Am   Aw

BWh   BWk   BSh   BSk

Csa   Csb

Cwa   Cwb

Cfa   Cfb   Cfc

Dsa   Dsb   Dsc   Dsd

Dwa   Dwb   Dwc   Dwd

Dfa   Dfb   Dfc   Dfd

ET   EF

The Köppen classification depends on average monthly values of temperature and precipitation. The most commonly used form of the Köppen classification has five primary types labeled A through E. Specifically, the primary types are A, tropical; B, dry; C, mild mid-latitude; D, cold mid-latitude; and E, polar. The five primary classifications can be further divided into secondary classifications such as rain forest, monsoon, tropical savanna, humid subtropical, humid continental, oceanic climate, Mediterranean climate, steppe, subarctic climate, tundra, polar ice cap, and desert.

Rain forests are characterized by high rainfall, with definitions setting minimum normal annual rainfall between 1,750 millimetres (69 in) and 2,000 millimetres (79 in).^[86] A tropical savanna is a grassland biome located in semi-arid to semi-humid climate regions of subtropical and tropical latitudes, with rainfall between 750 millimetres (30 in) and 1,270 millimetres (50 in) a year. They are widespread on Africa, and are also found in India, the northern parts of South America, Malaysia, and Australia.^[87] The humid subtropical climate zone where winter rainfall (and sometimes snowfall) is associated with large storms that the westerlies steer from west to east. Most summer rainfall occurs during thunderstorms and from occasional tropical cyclones.^[88] Humid subtropical climates lie on the east side continents, roughly between latitudes 20° and 40° degrees away from the equator.^[89]

An oceanic (or maritime) climate is typically found along the west coasts at the middle latitudes of all the world's continents, bordering cool oceans, as well as southeastern Australia, and is accompanied by plentiful precipitation year round.^[90] The Mediterranean climate regime resembles the climate of the lands in the Mediterranean Basin, parts of western North America, parts of Western and South Australia, in southwestern South Africa and in parts of central Chile. The climate is characterized by hot, dry summers and cool, wet winters.^[91] A steppe is a dry grassland.^[92] Subarctic climates are cold with continuous permafrost and little precipitation.^[93]

Effect on agriculture[link]

Rainfall estimates for southern Japan and the surrounding region from July 20 to 27, 2009.

Precipitation, especially rain, has a dramatic effect on agriculture. All plants need at least some water to survive, therefore rain (being the most effective means of watering) is important to agriculture. While a regular rain pattern is usually vital to healthy plants, too much or too little rainfall can be harmful, even devastating to crops. Drought can kill crops and increase erosion,^[94] while overly wet weather can cause harmful fungus growth.^[95] Plants need varying amounts of rainfall to survive. For example, certain cacti require small amounts of water,^[96] while tropical plants may need up to hundreds of inches of rain per year to survive.

In areas with wet and dry seasons, soil nutrients diminish and erosion increases during the wet season.^[24] Animals have adaptation and survival strategies for the wetter regime. The previous dry season leads to food shortages into the wet season, as the crops have yet to mature.^[97] Developing countries have noted that their populations show seasonal weight fluctuations due to food shortages seen before the first harvest, which occurs late in the wet season.^[65]

Changes due to global warming[link]

Increasing temperatures tend to increase evaporation which leads to more precipitation. Precipitation has generally increased over land north of 30°N from 1900 through 2005 but has declined over the tropics since the 1970s. Globally there has been no statistically significant overall trend in precipitation over the past century, although trends have varied widely by region and over time. Eastern portions of North and South America, northern Europe, and northern and central Asia have become wetter. The Sahel, the Mediterranean, southern Africa and parts of southern Asia have become drier. There has been an increase in the number of heavy precipitation events over many areas during the past century, as well as an increase since the 1970s in the prevalence of droughts—especially in the tropics and subtropics. Changes in precipitation and evaporation over the oceans are suggested by the decreased salinity of mid- and high-latitude waters (implying more precipitation), along with increased salinity in lower latitudes (implying less precipitation, more evaporation, or both). Over the contiguous United States, total annual precipitation increased at an average rate of 6.1 percent per century since 1900, with the greatest increases within the East North Central climate region (11.6 percent per century) and the South (11.1 percent). Hawaii was the only region to show a decrease (-9.25 percent).^[98]

Changes due to urban heat island[link]

Image of Atlanta, Georgia, showing temperature distribution, with hot areas appearing white

The urban heat island warms cities 0.6 °C (1.1 °F) to 5.6 °C (10.1 °F) above surrounding suburbs and rural areas. This extra heat leads to greater upward motion, which can induce additional shower and thunderstorm activity. Rainfall rates downwind of cities are increased between 48% and 116%. Partly as a result of this warming, monthly rainfall is about 28% greater between 20 miles (32 km) to 40 miles (64 km) downwind of cities, compared with upwind.^[99] Some cities induce a total precipitation increase of 51%.^[100]

Forecasting[link]

The Quantitative Precipitation Forecast (abbreviated QPF) is the expected amount of liquid precipitation accumulated over a specified time period over a specified area.^[101] A QPF will be specified when a measurable precipitation type reaching a minimum threshold is forecast for any hour during a QPF valid period. Precipitation forecasts tend to be bound by synoptic hours such as 0000, 0600, 1200 and 1800 GMT. Terrain is considered in QPFs by use of topography or based upon climatological precipitation patterns from observations with fine detail.^[102] Starting in the mid to late 1990s, QPFs were used within hydrologic forecast models to simulate impact to rivers throughout the United States.^[103] Forecast models show significant sensitivity to humidity levels within the planetary boundary layer, or in the lowest levels of the atmosphere, which decreases with height.^[104] QPF can be generated on a quantitative, forecasting amounts, or a qualitative, forecasting the probability of a specific amount, basis.^[105] Radar imagery forecasting techniques show higher skill than model forecasts within six to seven hours of the time of the radar image. The forecasts can be verified through use of rain gauge measurements, weather radar estimates, or a combination of both. Various skill scores can be determined to measure the value of the rainfall forecast.^[106]

See also[link]

• List of meteorology topics
• Mango showers, pre-monsoon showers in the Indian states of Karnataka and Kerala that help in the ripening of mangoes.
• Sunshower, an unusual meteorological phenomenon in which rain falls while the sun is shining.
• Wintry showers, an informal meteorological term for various mixtures of rain, freezing rain, sleet and snow.

References[link]

External links[link]

Look up precipitation in Wiktionary, the free dictionary.

• World precipitation map
• Collision/Coalescence; The Bergeron Process
• Report local rainfall inside the United States at this site (CoCoRaHS)
• Report local rainfall related to tropical cyclones worldwide at this site
• Global Precipitation Climatology Center GPCC
• Types of rainfall (BBC)

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There are many people in history who are commonly appended with the phrase "the Great", or who were called that or an equivalent phrase in their own language. Other languages have their own suffixes such as e Bozorg and e azam in Persian and Urdu respectively.

In Persia, the title "the Great" at first seems to be a colloquial version of the Old Persian title "Great King". This title was first used by the conqueror Cyrus II of Persia.^[1]

The Persian title was inherited by Alexander III of Macedon (336–323 BC) when he conquered the Persian Empire, and the epithet "Great" eventually became personally associated with him. The first reference (in a comedy by Plautus)^[2] assumes that everyone knew who "Alexander the Great" was; however, there is no earlier evidence that Alexander III of Macedon was called "the Great".

The early Seleucid kings, who succeeded Alexander in Persia, used "Great King" in local documents, but the title was most notably used for Antiochus the Great (223–187 BC).

Later rulers and commanders began to use the epithet "the Great" as a personal name, like the Roman general Pompey. Others received the surname retrospectively, like the Carthaginian Hanno and the Indian emperor Ashoka the Great. Once the surname gained currency, it was also used as an honorific surname for people without political careers, like the philosopher Albert the Great.

As there are no objective criteria for "greatness", the persistence of later generations in using the designation greatly varies. For example, Louis XIV of France was often referred to as "The Great" in his lifetime but is rarely called such nowadays, while Frederick II of Prussia is still called "The Great". A later Hohenzollern - Wilhelm I - was often called "The Great" in the time of his grandson Wilhelm II, but rarely later.

Rulers[link]

• Abbas I of Persia (1571–1629), Shah of Iran
• Akbar (1542–1605), ruler of the Mughal Empire of South Asia, mainly India
• Alain I of Albret (1440–1522), French aristocrat
• Alexander the Great (356-323 BC), King of Macedonia, Persia, Greece, Egypt, and all of Mesopotamia
• Alexander I of Georgia (1386–1446), King of Georgia
• Alfonso III of León (c. 848-910), King of León, Galicia and Asturias
• Alfred the Great (848/849-899), King of Wessex
• Antiochus III the Great (c. 241–187 BC), ruler of the Seleucid Empire
• Ashoka the Great (c. 304–232 BC), Indian emperor of the Maurya dynasty
• Ashot I of Iberia “the Great”(died 826/830), presiding prince of Iberia (modern Georgia),
• Askia Mohammad I (c. 1442–1538), ruler of the Songhai Empire
• Bhumibol Adulyadej (born 1927), King of Thailand
• Bolesław I Chrobry (967-1025), sometimes called "the Great", first King of Poland
• Bruno the Great (925–965), Archbishop of Cologne and Duke of Lotharingia (also listed in the following section)
• Buddha Yodfa Chulaloke (1736–1809), founder and ruler of the Rattanakosin Kingdom (in what is now Thailand)
• Cnut the Great (c. 985 or 995-1035), King of Denmark, England, Norway and parts of Sweden
• Casimir III the Great (1310–1370), King of Poland
• Catherine the Great (1729–1796), Empress of Russia
• Chandragupta II (reigned 375-413/415), also known as Vikramaditya, ruler of the Gupta empire in India
• Charlemagne (died 814), King of the Franks and Emperor of the Romans
• Chulalongkorn (1853–1910), King of Siam (now Thailand)
• Chlothar II (584-629), King of Neustria and King of the Franks
• Conrad, Margrave of Meissen (c. 1097-1157), Margrave of Meissen
• Constantine I (c. 272-337), Roman emperor
• Cyaxares the Great (c. 625-585 BC), third king of Media
• Cyrus the Great (c. 600 BC or 576 BC–530 BC), founder and ruler of the Persian or Achaemenid Empire
• Darius the Great (550 – 486 BC), third ruler of the Persian Empire
• Devapala (died 850), ruler of the Pala Empire in the Indian subcontinent
• Dionysius I, Greek tyrant of Syracuse^[3]
• Ferdinand I of León and Castile (c. 1015–1065), King of León and Count of Castile
• Frederick the Great (1712–1786), King of Prussia
• Genghis Khan (1162?-1227), founder and Great Khan of the Mongol Empire
• Gero (c. 900–965), ruler of Marca Geronis, a very large march in Europe
• Gustavus Adolphus of Sweden (1594–1632), King of Sweden, founder of the Swedish Empire, and noted military leader
• Gwanggaeto the Great, King of Goguryeo, one of the Three Kingdoms of Korea^[4][5]
• Hanno the Great, the name of three leaders of Carthage, in the 4th, 3rd, and 2nd centuries BC
• Henry I, Duke of Burgundy (946–1002)
• Henry IV of France (1553–1610), King of France and King of Navarre
• Herod the Great (73/74 BC-4 BC), King of Judea
• Hugh the Great (898-956), Duke of the Franks and Count of Paris
• Hugh Magnus of France (1007–1025), co-King of France
• Hugh I, Count of Vermandois (1057–1101)
• Humphrey I de Bohun (died c. 1123), Anglo-Norman aristocrat
• Ivan III of Russia (1440–1505), Tsar of Russia
• John I of Portugal (1358–1433), King of Portugal and the Algarve
• John II of Aragon (1398–1479), King of Aragon and, through his wife, King of Navarre
• Justinian I (483-565), Byzantine Emperor
• Kamehameha I (c. 1758-1819), first King of Hawai'i
• Kanishka (died c. 127), ruler of the Kushan Empire in Central Asia and parts of India
• Kvirike III of Kakheti (1010–1029), King of Kakheti in eastern Georgia
• Kublai Khan (1215–1294), Mongol ruler in the 13th century and Emperor of China; founder of the Yuan Dynasty
• Llywelyn the Great (c. 1172–1240), Prince of Gwynedd and de facto ruler of most of Wales
• Louis I of Hungary (1326–1382), King of Hungary, Croatia and Poland
• Mangrai the Great (1238–1317), Lanna, northern Thailand
• Emperor Meiji (1852–1912), Emperor of Japan
• Mircea I of Wallachia (1355–1418)
• Mithridates II of Parthia (died 88 BC), ruler of the Parthian Empire (in present day Iran)
• Mithridates VI of Pontus (134 BC–63 BC), ruler of Pontus and the Bosporan Kingdom
• Mstislav I of Kiev (1076–1132), Grand Prince of Kievan Rus
• Naresuan (1555–1605), King of Ayutthaya
• Narai (1633–1688), King of Ayutthaya (in what is now modern Thailand)
• Odo the Great (died c. 735), Duke of Aquitaine
• Otto I, Holy Roman Emperor (912-973)
• K'inich Janaab' Pakal (603-683), ruler of the Mayan city-state of Palenque
• Parakramabahu I of Polonnaruwa (1123–1186), King of Sri Lanka
• Peter Krešimir IV of Croatia (died 1075), King of Croatia
• Peter the Great (1672–1725), Tsar of Russia
• Peter III of Aragon (1239–1285), King of Aragon and King of Sicily
• Pompey (106 BC-48 BC), military and political leader of the late Roman Republic, rival of Julius Caesar
• Radama I (1793–1828), first king of greater Madagascar
• Raja Raja Chola I (c. 947-1014), Indian emperor of the Cholas.^[6][7][8]
• Rajendra Chola I (reigned 1014–1044), Tamil King of India
• Ramesses II (reigned 1279 BC – 1213 BC), considered the greatest pharaoh of Ancient Egypt
• Ram Khamhaeng (around 1237 to 1247-1298), King of Sukhothai (in present day Thailand)
• Ramon Berenguer III, Count of Barcelona (1082–1131), also Count of Provence and various other counties
• Rhodri the Great (c. 820–878), King of Gwynedd (in present day Wales)
• Roman the Great (after 1160-1205), Grand Prince of Kiev
• Saladin (c. 1138-1193), Kurdish Sultan of Egypt and Syria, founder of the Ayyubid dynasty, and victor over the Crusaders
• Samudragupta (c. 335–375), ruler of the Gupta empire in the Indian subcontinent
• Sancho III of Navarre (c. 992-1035), King of Kingdom of Navarre
• Sargon of Akkad (died c. 2215 BC), ruler of the Akkadian Empire
• Sejong the Great (1397–1450), Korean king^[9]
• Shapur II (309-379), king of the Sassanid Empire, Persia
• Simeon I of Bulgaria (864/865-927), ruler of the First Bulgarian Empire
• Stephen III of Moldavia (1433–1504), Prince of Moldavia (Romania)
• Stephen Uroš IV Dušan of Serbia (c. 1308-1355), King of Serbia and Emperor of the Serbs and Greeks
• Taksin (1734–1782), King of the Thonburi Kingdom (Thailand)
• Tamar (1160-1123), Queen of the Georgian Empire
• Timur (1336–1405), better known as Tamerlane, founder of the Timurid Dynasty
• Theobald II, Count of Champagne (1090–1151), Count of Blois and of Chartres as Theobald IV, Count of Champagne and of Brie
• Theodoric the Great (454-526), King of the Ostrogoths, regent of the Visigoths and a viceroy of the Byzantine Empire
• Theodosius I (347-395), Roman emperor
• Tigranes the Great (140-55 BC), Emperor of Armenia
• Tiridates III of Armenia (285-339), King of Armenia
• Umar (c. 586 to 590–644), second caliph of the Muslim Empire
• Valdemar I of Denmark (1131–1182), King of Denmark
• Valentinian I (364-375), Roman Emperor
• Vladimir I of Kiev (c. 958-1015), ruler of Kievan Rus
• Vytautas (c. 1350-1430), archduke of the Lithuanian Grand Duchy
• William I, Count of Burgundy (1020–1087), Count of Burgandy and Mâcon
• William V, Duke of Aquitaine (969-1030), also Count of Poitou
• Xerxes I (519-465 BC), King of Kings of the Achaemenid Empire (Persia)
• Yu the Great (c. 2200-2100 BC), legendary ruler in ancient China

Religious figures[link]

• Abraham the Great of Kashkar (ca. 492-586), monk and saint of the Assyrian Church of the East
• Abraham Kidunaia (died c. 366, hermit, priest, and Christian saint of Mesopotamia
• Albertus Magnus (1193/1206–1280), medieval German philosopher and theologian
• Anthony the Great (c. 251–356), early Christian saint of Egypt
• Babai the Great (c. 551–628), Assyrian church leader
• Basil of Caesarea (330-379), Greek bishop and theologian
• Bruno the Great (925–965), Archbishop of Cologne and Duke of Lotharingia (also listed in the previous section)
• Euthymius the Great (377-473), abbot and Roman Catholic and Eastern Orthodox saint
• Gertrude the Great (1256-c. 1302), German Benedictine, mystic, theologian and Roman Catholic saint
• Pope Gregory I (c. 540-604)
• Hiyya the Great, 3rd-century rabbi, Palestine
• Pope John Paul II (1920–2005)
• Pope Leo I (c. 391 or 400-461)
• Macarius of Egypt (c. 300-391), Egyptian hermit
• Pope Nicholas I (c. 800-867)
• Photius I of Constantinople (c. 810–c. 893), Eastern Orthodox saint and Patriarch of Constantinople
• William of Maleval (died 1157), founder of the Catholic congregation of Williamites

Other[link]

• Beli Mawr, a figure in medieval Welsh literature and genealogies
• Emmy the Great, folk singer
• Matteo Rosso the Great, Roman politician and father of Pope Nicholas III
• Prokop the Great, Hussite general in Bohemia

See also[link]

• Epithet
• List of monarchs by nickname
• List of nicknames of European Royalty and Nobility: G-I
• James, son of Zebedee, also known as James the Greater, one of the twelve apostles of Jesus
• Ajax (mythology), called Ajax the Greater
• Mohandas Karamchand Gandhi, whose common honorific "Mahatma" means "Great Soul"

Notes[link]

This article does not cite any references or sources. Please help improve this article by adding citations to reliable sources. Unsourced material may be challenged and removed. (December 2009)

"Can I Get a Witness" is a 1963 hit song by Marvin Gaye on the Tamla (Motown) label. Written and produced by Motown songwriting and producing team Holland–Dozier–Holland, the song was built among gospel-styled music and heralded Gaye's beginnings in the church with a rhythm and blues/rock and roll setting. The song featured Gaye on piano, playing a boogie pattern, The Funk Brothers, and members of The Supremes in the background accompanying Gaye. The song became a hit in both the U.S. and the United Kingdom, and British musicians Lulu, Dusty Springfield, The Rolling Stones, Sam Brown and Steampacket (which featured a very young Rod Stewart) recorded cover versions of the song. Gaye's version peaked at #22 on the Hot 100 chart and its title soon became a catchphrase. Lee Michaels' 1971 version reached #39 on the Hot 100; both his and Gaye's versions peaked during Christmas week.

In popular culture[link]

• Gaye's recording is featured in the 1999 biographical film The Hurricane.

Personnel[link]

• Lead vocals by Marvin Gaye
• Background vocals by The Supremes: Diana Ross, Florence Ballard, and Mary Wilson
• Instrumentation by The Funk Brothers