In meteorology, a cloud is a visible mass of liquid droplets or frozen crystals made of water or various chemicals suspended in the atmosphere above the surface of a planetary body. These suspended particles are also known as aerosols. Clouds in earth's atmosphere are studied in the cloud physics branch of meteorology. Two processes, possibly acting together, can lead to air becoming saturated: cooling the air or adding water vapor to the air. In general, precipitation will fall to the surface; an exception is virga, which evaporates before reaching the surface.
Clouds can show convective development like cumulus, appear in layered sheets such as stratus, or take the form of thin fibrous wisps, as in the case of cirrus. Prefixes are used in connection with clouds: strato- for low cumuliform-category clouds that show some stratiform characteristics, nimbo- for thick stratiform clouds that can produce moderate to heavy precipitation, alto- for middle clouds, and cirro- for high clouds. Whether or not a cloud is low, middle, or high level depends on how far above the ground its base forms.
Cloud types with significant vertical extent can form in the low or middle ranges depending on the moisture content of the air. Clouds in the troposphere have Latin names due to the popular adaptation of Luke Howard's cloud categorization system, which began to spread in popularity during December 1802. Synoptic surface weather observations use code numbers for the types of tropospheric cloud visible at each scheduled observation time based on the height and physical appearance of the clouds.
While a majority of clouds form in Earth's troposphere, there are occasions where clouds in the stratosphere and mesosphere are observed. These three main layers of the atmosphere where clouds may be seen are collectively known as the homosphere. Above this lie the thermosphere and exosphere, which together make up the heterosphere that marks the transition to outer space. Clouds have been observed on other planets and moons within the Solar System, but, due to their different temperature characteristics, they are composed of other substances such as methane, ammonia, and sulfuric acid.
Cloud evolution in under a minute.
Late-summer
rainstorm in
Denmark. Nearly black color of base indicates main cloud in foreground probably cumulonimbus.
In general, clouds form in the troposphere when one or more lifting agents causes air containing invisible water vapor to rise and cool to its dew point, the temperature at which the air becomes saturated. The main mechanism behind this process is adiabatic cooling.[1] Atmospheric pressure decreases with altitude, so the rising air expands in a process that expends energy and causes the air to cool, which reduces its capacity to hold water vapor. If the air is cooled to its dew point and becomes saturated, it normally sheds vapor it can no longer retain which condenses into cloud.
The altitude at which this begins to happen is called the lifted condensation level, which roughly determines the height of the cloud base.[1] Water vapor in saturated air is normally attracted to condensation nuclei such as dust, ice, and salt that are small enough to be held aloft by normal circulation of the air. If the condensation process occurs below the freezing level in the troposphere, the nuclei help transform the vapor into very small water droplets. The average size of a newly formed droplet is around .002 mm (.00008 in). High clouds that form above the freezing level are composed mostly of ice crystals. An absence of sufficient condensation particles at and above the condensation level causes the rising air to become supersaturated and the formation of cloud tends to be inhibited.
There are three main agents of vertical lift. One comprises two closely related processes working together. Frontal lift and cyclonic lift occur when stable or slightly unstable air, which has been subjected to little or no surface heating, is forced aloft at weather fronts and around centers of low pressure. Newly formed cloud droplets that are lifted beyond the condensation level tend to increase in number and coalesce until they grow to a size of up to .04 mm (.002 in). They remain aloft as long as the drag force of the air dominates over the gravitational force for small particles. If the cloud droplets continue to grow past this size, they become too heavy to be held aloft as the gravitational force overcomes the atmospheric drag, and they fall from the cloud as rain.[2] When this process takes place just above the freezing level, the vapor tends to condense into supercooled water droplets, which with additional lifting and growth in size, can eventually turn into freezing rain. At temperatures well below freezing, the vapor desublimates into ice crystals that average about 0.25 mm in length.[3] Continuing lift and desublimation will tend to increase the number of ice crystals which may combine until they are too heavy to be supported by the vertical air currents and fall out as snow.
Another agent is the buoyant convective upward motion caused by significant daytime solar heating at surface level, or by relatively high absolute humidity. Air warmed in this way becomes increasingly unstable. This causes it to rise and cool until temperature equilibrium is achieved with the surrounding air aloft. If air near the surface becomes extremely warm and unstable, its upward motion can become quite explosive resulting in towering clouds that can break through the tropopause or cause severe weather. Strong convection upcurrents may allow the droplets to grow to nearly .08 mm (.003 in) before precipitating as heavy rain from an active thundercloud.[4] More occasionally, very warm unstable air is present around fronts and low pressure centers. As with non-frontal convective lift, increasing instability promotes upward vertical cloud growth and raises the potential for severe weather.
A third source of lift is wind circulation forcing stable or slightly unstable air over a physical barrier such as a mountain (orographic lift). If the air is generally stable, nothing more than lenticular cap clouds will form. However, if the air becomes sufficiently moist and unstable, orographic showers or thunderstorms may appear.[5]
Along with adiabatic cooling that requires a lifting agent, there are three other main mechanisms for lowering the temperature of the air to its dew point, all of which occur near surface level and do not require any lifting of the air. Conductive, radiational, and evaporative cooling can cause condensation at surface level resulting in the formation of fog. Conductive cooling takes place when air from a relatively mild source area comes into contact with a colder surface, as when mild marine air moves across a colder land area. Radiational cooling occurs due to the emission of infrared radiation, either by the air or by the surface underneath.[6] This type of cooling is common during the night when the sky is clear. Evaporative cooling happens when moisture is added to the air through evaporation, which forces the air temperature to cool to its wet-bulb temperature, or sometimes to the point of saturation.[7]
There are five main ways water vapor can be added to the air. Increased vapor content can result from wind convergence over water or moist ground into areas of upward motion.[8] Precipitation or virga falling from above also enhances moisture content.[9] Daytime heating causes water to evaporate from the surface of oceans, water bodies or wet land.[10] Transpiration from plants is another typical source of water vapor.[11] Lastly, cool or dry air moving over warmer water will become more humid. As with daytime heating, the addition of moisture to the air increases its heat content and instability and helps set into motion those processes that lead to the formation of cloud or fog.[12]
An idealised view of three large circulation cells.
Although the local distribution of clouds can be significantly influenced by topography, the global prevalence of cloud cover tends to vary more by latitude. This is the result of atmospheric motion driven by the uneven horizontal distribution of net incoming radiation from the sun. Cloudiness reaches maxima close to the equator and near the 50th parallels of latitude in the northern and southern hemispheres.[13] These are zones of low pressure that encircle the Earth as part of a system of large latitudinal cells that influence atmospheric circulation. In both hemispheres working away from the equator, they are the tropical Hadley cells, the mid-latitude Ferrel, and the polar cells. The 50th parallels coincide roughly with bands of low pressure situated just below the polar highs. These extratropical convergence zones are occupied by the polar fronts where air masses of polar origin meet and clash with those of tropical or subtropical origin.[14] This leads to the formation of weather-making extratropical cyclones.[15]
February position of the ITCZ and monsoon trough in the Pacific Ocean, depicted by area of convergent streamlines offshore Australia and in the equatorial eastern Pacific
Near the equator, increased cloudiness is due to the presence of the low pressure Intertropical Convergence Zone or monsoon trough. Monsoon troughing in the western Pacific reaches its latitudinal zenith in each hemisphere above and below the equator during the late summer when the wintertime surface high pressure ridge in the opposite hemisphere is strongest. The trough can reach as far as the 40th parallel north in East Asia during August and the 20th parallel south in Australia during February. Its poleward progression is accelerated by the onset of the summer monsoon which is characterized by the development of lower air pressure over the warmest parts of the various continents.[16] In the southern hemisphere, the trough associated with the Australian monsoon reaches its most southerly latitude in February, oriented along a west-northwest to east-southeast axis.[17]
Cloudiness reaches minima near the poles and in the subtropics close to the 20th parallels, north and south. The latter are sometimes referred to as the horse latitudes. The presence of a large scale subtropical ridge on each side of the equator reduces cloudiness at these low latitudes. Heating of the earth near the equator leads to large amounts of upward motion and convection along the monsoon trough or intertropical convergence zone. These rising air currents diverge in the upper troposphere and move away from the equator at high altitude in both northerly and southerly directions. As it moves towards the mid-latitudes on both sides of the equator, the air cools and sinks. The resulting air mass subsidence creates a subtropical ridge near the 30th parallel of latitude in both hemispheres where the formation of cloud is minimal. At surface level, the sinking air diverges again with some moving back to the equator and completing the vertical cycle. This circulation on each side of the equator is known as the Hadley cell in the tropics. Many of the world's deserts are caused by these climatological high-pressure areas.[18]
Similar patterns also occur at higher latitudes in both hemispheres. Upward currents of air along the polar fronts diverge at high tropospheric altitudes. Some of the diverging air moves to the poles where air mass subsidence inhibits cloud formation and leads to the creation of the polar areas of high pressure. Divergence occurs near surface level resulting in a return of the circulating air to the polar fronts where rising air currents can create extensive cloud cover and precipitation.[14] This vertical cycle comprises the polar cell in each latitudinal hemisphere. Some of the air rising at the polar fronts diverges away from the poles and moves in the opposite direction to the high level zones of convergence and subsidence at the subtropical ridges on each side of the equator. These mid-latitude counter-circulations create the Ferrel cells that encircle the globe in the northern and southern hemispheres.
Luke Howard, a methodical observer with a strong grounding in the Latin language, used his background to categorize the various tropospheric cloud types and forms during December 1802. He believed that the changing cloud forms in the sky could unlock the key to weather forecasting. Jean-Baptiste Lamarck worked independently on cloud categorization and came up with a different naming scheme that failed to make an impression even in his home country of France because it used unusual French names for cloud types. His system of nomenclature included twelve categories of clouds, with such names as (translated from French) hazy clouds, dappled clouds and broom-like clouds. Howard used universally accepted Latin, which caught on quickly. As a sign of the popularity of the naming scheme, the German dramatist and poet Johann Wolfgang von Goethe composed four poems about clouds, dedicating them to Howard. Classification systems would be proposed by Heinrich Dove of Germany in 1828 and Elias Loomis of the United States in 1841, but neither became the international standard that Howard's system became. It was formally adopted by the International Meteorological Commission in 1929.[19]
Howard's original system established three general cloud categories based on physical appearance and process of formation: cirriform (mainly detached and wispy), cumuliform or convective (mostly detached and heaped, rolled, or rippled), and non-convective stratiform (mainly continuous layers in sheets). These were cross-classified into lower and upper families. Cumuliform clouds forming in the lower level were given the genus name cumulus, and low stratiform clouds the genus name stratus. Physically similar clouds forming in the upper height range were given the genus names cirrocumulus (generally showing more limited convective activity than low level cumulus) and cirrostratus, respectively. Cirriform category clouds were identified as always upper level and given the genus name cirrus. To these, Howard added the genus nimbus for all clouds producing significant precipitation.[20]
Around 1840–41, German meteorologist Ludwig Kaemtz added stratocumulus as a mostly detached low-cloud genus of limited convection with both cumuliform and stratiform characteristics, similar to upper level cirrocumulus. About fifteen years later, Emilien Renou, director of the Parc Saint-Maur and Montsouris observatories, began work on an elaboration of Howard's classifications that would lead to the introduction of altocumulus (physically more closely related to stratocumulus than to cumulus) and altostratus during the 1870s. These were cumuliform (of limited convection) and stratiform cloud genera, respectively, of a newly defined middle height range above stratocumulus and stratus but below cirrocumulus and cirrostratus, with free convective cumulus and non-convective nimbus occupying more than one altitude range as clouds with vertical extent. In 1880, Philip Weilbach, secretary and librarian at the Art Academy in Copenhagen, and like Luke Howard, an amateur meteorologist, proposed and had accepted by the International Meteorological Committee (IMC) the designation of a new free-convective vertical genus type, cumulonimbus, which would be distinct from cumulus and nimbus and identifiable by its appearance and ability to produce thunder. With this addition, a canon of ten cloud genera was established that came to be officially and universally accepted. At about the same time, several cloud specialists proposed variations that came to be accepted as species subdivisions and varieties determined by more specific variable aspects of the structure of each genus. One further modification of the genus classification system came when an IMC commission for the study of clouds put forward a refined and more restricted definition of the genus nimbus renamed nimbostratus.[20]
As established by Howard, clouds are grouped into three physical categories: cirriform, cumuliform, and stratiform. These designations distinguish a cloud's physical structure and process of formation. All weather-related clouds form in the troposphere, the lowest major layer of the Earth's atmosphere.[21]
Towering vertical cumulonimbus capillatus with anvil-shaped incus supplementary feature. High layer of cirrus spissatus near top of image.
Cumuliform-category clouds are the product of localized convective or orographic lift. Incoming shortwave radiation generated by the sun reflects back as longwave radiation when it reaches the earth's surface, a process that warms the air closest to ground. The more the air is heated, the more unstable it will tend to become.[21] If the airmass is only slightly unstable, clouds of limited convection that show both cumuliform and stratiform characteristics will form at any altitude in the troposphere where there is sufficient condensation. If a poorly organized weather system is present, weak intermittent virga or precipitation may fall from those clouds that form mostly in the lower half of the troposphere. Greater airmass instability caused by more intense radiational surface heating by the sun will create a steeper temperature gradient from warm or hot at surface level to cold aloft. This may cause larger clouds of free convection to form in the lower half of the troposphere and grow upward to greater heights, especially if associated with fast-moving unstable cold fronts. Large free-convective types can produce light to moderate showers if the airmass is sufficiently moist. The largest free-convective towering clouds produce thunderstorms and a variety of types of lightning including cloud-to-ground that can cause wildfires.[22] Other convective severe weather may or may not be associated with thunderstorms and include heavy rain or snow showers, hail,[23] strong wind shear, downbursts,[24] and tornadoes.[25]
In general, stratiform-category clouds form at any altitude in the troposphere where there is sufficient condensation as the result of non-convective lift of relatively stable air, especially along slow-moving warm fronts, around areas of low pressure, and sometimes along stable slow moving cold fronts.[21] In general, precipitation falls from stratiform clouds in the lower half of the troposphere. If the weather system is well-organized, the precipitation is generally steady and widespread. The intensity varies from light to heavy according to the thickness of the stratiform layer as determined by moisture content of the air and the intensity of the weather system creating the clouds and weather. Unlike free convective cumuliform clouds that tend to grow upward, stratiform clouds achieve their greatest thickness when precipitation that forms in the cloud just below the upper half of the troposphere triggers downward growth of the cloud base to near surface level. Stratiform clouds can also form in precipitation below the main frontal cloud deck where the colder air is trapped under the warmer airmass being forced above by the front. Non-frontal low stratiform cloud can form when advection fog is lifted above surface level during breezy conditions.
Cirriform-category clouds form mostly at high altitudes along the very leading edges of a frontal or low-pressure weather disturbance and often along the fringes of its other borders. In general, they are non-convective but occasionally acquire a tufted or turreted appearance caused by small scale high-altitude convection. These high clouds do not produce precipitation as such but can merge and thicken into lower stratiform layers that do.[26]
Cloud classification by altitude of occurrence. Towering vertical cumulus congestus not shown.
The individual genus types result from the physical categories being cross-classified by height range family within the troposphere. These include the families of high, middle, low, moderate upward or downward-growing vertical, and upward growing towering vertical clouds. Moderate or towering vertical clouds can have low or middle bases depending on the moisture content of the air. The family designation for a particular genus is determined by the base height of the cloud and its vertical extent. The base-height range for each family varies depending on the latitudinal geographical zone.[27]
High and middle: All cirriform-category clouds are classified as high-range and thus constitute a single genus cirrus (Ci). Cumuliform and stratiform-category clouds in the high-altitude family carry the prefix cirro-, yielding the respective genus names cirrocumulus (Cc) and cirrostratus (Cs). Similar genera in the middle-range family are prefixed by alto-, yielding the genus names altocumulus (Ac) and altostratus (As).[21]
Low and moderate vertical: Any cumuliform or stratiform genus in these two families either has no prefix or carries one that refers to a characteristic other than altitude. The two non-prefixed genera are non-convective low stratus (St) that usually forms into a comparatively thin layer, and free-convective cumulus (Cu) that has moderate upward-growing vertical extent. One prefixed cloud in this group is stratocumulus (Sc), a low-range genus of limited convection that has some stratiform characteristics (as do the middle and high-based genera altocumulus and cirrocumulus, the genus names of which exclude strato- to avoid double-prefixing). The other prefixed cloud is nimbostratus (Ns), a non-convective genus that has moderate downward-growing vertical extent,[21][28][29] and whose prefix refers to its ability to produce significant precipitation.
Towering vertical: This family comprises towering free-convective clouds that typically grow upward to occupy all altitude ranges. Their genus names also carry no height-related prefixes. They comprise the genus cumulonimbus (Cb) and the cumulus species cumulus congestus (Cu con). The latter type is designated towering cumulus (Tcu) by the International Civil Aviation Organization. Under conditions of very low humidity, free-convective clouds may form above the low-altitude range and, therefore, be found only at middle- and high-tropospheric altitudes. In the modern system of cloud nomenclature, cumulonimbus is something of an anomaly. The cumuliform-category designation appears in the prefix rather than the root, which refers instead to the cloud's ability to produce storms and heavy precipitation. This apparent reversal of prefix and root is a carry-over from the 19th century, when nimbus was the root word for all precipitating clouds.[20]
Major precipitation clouds: Although they do not comprise a family as such, cloud genera with nimbo- or -nimbus in their names are the principal bearers of precipitation. Nimbostratus initially forms from altostratus in the middle height range. However, it can be classified as moderate vertical because it achieves considerable thickness despite not being a convective cloud like cumulonimbus, the other main precipitating cloud genus. Frontal lift can push the top of a nimbostratus deck into the high-altitude range while precipitation drags the base down to low altitudes.[21] The World Meteorological Organization (WMO) classifies nimbostratus as a middle cloud whose base typically thickens down into the low altitude range during precipitation.[26]
Natural beauty of cumulus fractus clouds in
Nepali sky
Cumulus partly spreading into stratocumulus over the port of
Piraeus in
Greece
Genus types are divided into species that indicate specific structural details. However, because these latter types are not always restricted by height range, some species can be common to several genera that are differentiated mainly by altitude. The best examples of these are the species stratiformis, lenticularis, and castellanus, which are common to cumuliform genera of limited convection in the high-, middle-, and low-height ranges (cirrocumulus, altocumulus, and stratocumulus, respectively). Stratiformis species normally occur in extensive sheets or in smaller patches with only minimal convective activity. Lenticularis species tend to have lens-like shapes tapered at the ends. They are most commonly seen as orographic mountain-wave clouds, but can occur anywhere in the troposphere where there is strong wind shear. Castellanus structures, which resemble the turrets of a castle when viewed from the side, can also be found in convective patches of cirrus, as can the more detached tufted floccus species, which are common to cirrus, cirrocumulus, and altocumulus. However, floccus is not associated with stratocumulus in the lower levels where local airmass instability tends to produce clouds of the more freely convective cumulus and cumulonimbus genera, whose species are mainly indicators of degrees of vertical development. A cumulus cloud will initially form as a cloudlet of the species humilis showing only slight vertical development. With increasing airmass instability, it will tend to grow vertically into the species mediocris, then congestus, the tallest cumulus species. With further instability, the cloud may continue to grow into cumulonimbus calvus (essentially a very tall congestus cloud that produces thunder), then ultimately capillatus when supercooled water droplets at the top turn into ice crystals giving it a cirriform appearance.[30]
Cirrus clouds have several additional species unique to the wispy structures of this genus, which include uncinus, filaments with upturned hooks, and spissatus, filaments that merge into dense patches. One exception is the species fibratus, which can be seen with cirrus and also with cirrostratus that is transitional to or from cirrus. Cirrostratus at its most characteristic tends to be mostly of the species nebulosus, which creates a rather diffuse appearance lacking in structural detail. All altostratus and nimbostratus clouds share this physical appearance without significant variation or deviation and, therefore, do not need to be subdivided into species. Low continuous stratus is also of the species nebulosus except when broken up into ragged sheets of stratus fractus. This latter fractus species also occurs with ragged cumulus.[26]
Genus and species types are further subdivided into varieties. Some varieties are determined by the opacities of particular low and middle cloud structures and comprise translucidus (translucent), opacus (opaque), and perlucidus (opaque with translucent breaks). These varieties are always identifiable for cloud genera and species with variable opacity, including middle family altocumulus and altostratus, and low family stratocumulus and stratus. Opacity based varieties are not applied to high clouds that are always translucent, or conversely， to clouds with significant vertical extent that are always opaque. Some cloud varieties are not restricted to a specific altitude range or physical structure, and can therefore be common to more than one genus or species.[26]
Other varieties are determined by the arrangements of the cloud structures into particular patterns that are discernable by a surface-based observer (cloud fields usually being visible only from a significant altitude above the formations). These varieties are not always present with the genera and species with which they are otherwise associated, but only appear when upper wind currents and air mass stability or humidity patterns favor their formation. The variety undulatus (having a wavy undulating base) can occur with high, middle, and low stratiform types and with limited convective cumuliform genera (usually of the stratiformis or lenticularis species) when there are uneven upper wind currents, but not with clouds of significant vertical extent. Another variety, duplicatus (closely spaced layers of the same type, one above the other), is sometimes found with any of the same genera and species except cirrocumulus, although not necessarily at the same time as the undulatus variety. The variety radiatus is seen when cloud rows of a particular type appear to converge at the horizon. It is sometimes seen with various species of cirrus, altocumulus, stratocumulus, and cumulus, and with the genus altostratus that has no species. Intortus or vertebratus varieties occur on occasion with cirrus types, and are respectively filaments twisted into irregular shapes, and those that are arranged in fishbone patterns, usually by uneven wind currents that favor the formation of these varieties. Probably the most uncommonly seen is the variety lacunosus, caused by localized downdrafts that punch circular holes into high, middle, or low cumuliform cloud layers of limited convection, usually of the stratiformis species.[26]
It is possible for some species of low and middle genera to show combined varieties at one time, especially if one variety is opacity-based and the other is pattern-based. An example of this would be an opaque layer of altocumulus stratiformis arranged in seemingly converging rows. The full technical name of a cloud in this configuration would be altocumulus stratiformis opacus radiatus, which would identify respectively its genus, species, and two combined varieties.[30]
Cumulus and stratocumulus made orange by the sun rising
Supplementary features are not further subdivisions of cloud types below the species and variety level. Rather, they are either hydrometeors or special cloud formations with their own Latin names that form in association with certain cloud genera, species, and varieties.
One group of supplementary features are not actual cloud formations but rather precipitation that falls when water droplets that make up visible clouds have grown too heavy to remain aloft. Virga is a feature seen with clouds producing precipitation that evaporates before reaching the ground, these being of the genera cirrocumulus, altocumulus, altostratus, nimbostratus, stratocumulus, cumulus, and cumulonimbus. When the precipitation reaches the ground without completely evaporating, it is designated as the feature praecipitatio. This normally occurs with altostratus opacus, which can produce widespread but usually light precipitation, and with thicker clouds of moderate vertical development. Of the latter, upward-growing cumulus mediocris produces only isolated light showers, while downward growing nimbostratus is capable of heavier, more extensive precipitation. Towering vertical clouds have the greatest ability to produce intense precipitation events, but these tend to be localized unless organized along fast-moving cold fronts. Showers of moderate to heavy intensity can fall from cumulus congestus clouds. Cumulonimbus, the largest of all cloud genera, has the capacity to produce very heavy showers. Low stratus clouds usually produce only light precipitation, but this always occurs as the feature praecipitatio due to the fact this cloud genus lies too close to the ground to allow for the formation of virga. The heavier precipitating clouds, nimbostratus, towering cumulus (cumulus congestus), and cumulonimbus, also typically see the formation in precipitation of the pannus feature, low ragged clouds of the genera and species cumulus fractus or stratus fractus.[26]
Cumulonimbus dissipating at dusk
These formations, along with several other cloud-based supplementary features, are also known as accessory clouds.
After the pannus types, the remaining supplementary features comprise cloud formations that are associated mainly with upward-growing cumuliform clouds of free convection. Pileus is a cap cloud that can form over a cumulonimbus or large cumulus cloud, whereas a velum feature is a thin horizontal sheet that sometime forms around the middle or in front of the parent cloud. A tuba feature is a cloud column that may hang from the bottom of a cumulus or cumulonimbus. An arcus feature is a roll or shelf cloud that forms along the leading edge of a squall line or thunderstorm outflow. Some arcus clouds form as a consequence of interactions with specific geographical features. Perhaps the strangest geographically specific arcus cloud in the world is the Morning Glory, a rolling cylindrical cloud that appears unpredictably over the Gulf of Carpentaria in Northern Australia. Associated with a powerful "ripple" in the atmosphere, the cloud may be "surfed" in glider aircraft. The mamma feature forms on the bases of clouds as downward-facing bubble-like protuberances caused by localized downdrafts within the cloud. It is also sometimes called mammatus, an earlier version of the term used before a standardization of Latin nomenclature brought about by the World Meterorological Organization during the 20th century. The best-known is cumulonimbus with mammatus, but the mamma feature is also seen occasionally with cirrus, cirrocumulus, altocumulus, altostratus, and stratocumulus. Incus is the most type-specific supplementary feature, seen only with cumulonimbus of the species capillatus. A cumulonimbus incus cloud top is one that has spread out into a clear anvil shape as a result of rising air currents hitting the stability layer at the tropopause where the air no longer continues to get colder with increasing altitude.[26]
Clouds initially form in clear air or become clouds when fog rises above surface level. The genus of a newly formed cloud is determined mainly by air mass characteristics such as stability and moisture content. If these characteristics change over a period of time, the genus tends to change accordingly. When this happens, the original genus is called a mother cloud. If the mother cloud retains much of its original form after the appearance of the new genus, it is termed a genitus cloud. One example of this is stratocumulus cumulogenitus, a stratocumulus cloud formed by the partial spreading of a cumulus type when there is a loss of convective lift. If the mother cloud undergoes a complete change in genus, it is considered to be a mutatus cloud.[26] It is theoretically possible for some lengthy terminologies to emerge by combining the names of all applicable genera, species, varieties, and supplementary features to provide a complete description of an active and evolving genitus or mutatus cloud formation. As an extreme example, a flat opaque layer of altocumulus formed by the spreading of cumulus arranged in parallel bands accompanied by precipitation not reaching the ground could be termed altocumulus stratiformis opacus radiatus cumulogenitus virga.[30]
Stratocumulus clouds can be organized into "fields" that take on certain specially classified shapes and characteristics. In general, these fields are more discernable from high altitudes than from ground level. They can often be found in the following forms:
- Actinoform, which resembles a leaf or a spoked wheel.
- Closed cell, which is cloudy in the center and clear on the edges, similar to a filled honeycomb.
- Open cell, which resembles a honeycomb, with clouds around the edges and clear, open space in the middle.[31]
Weather maps plotted and analyzed at weather forecasting centers employ special symbols to denote various cloud families, genera, species, varieties, mutations, and cloud movements that are considered important to identify conditions in the troposphere that will assist in preparing the forecasts. The cloud symbols are translated from numerical codes included with other meteorological data that make up the contents of international synoptic messages transmitted at regular intervals by professionally trained staff at major weather stations. In a couple of cases, an entire genus like cirrocumulus is represented by one cloud symbol, regardless of species, varieties, or any other considerations. In general though, the codes and their symbols are used to identify cloud types at the species level. A number of varieties and supplementary features are also deemed important enough to have their own weather map symbols. For the sake of economy, a particular species may share a numerical reporting code and symbol with other similar species of the same genus; a practice also extended to a few varieties. Sometimes, a separate symbol is used to indicate whether or not a particular genus has transformed or emerged from a mother cloud of another genus, or is increasing in amount or invading the sky (usually in the form of parallel bands in a radiatus configuration) ahead of an approaching weather disturbance.[26]
The international synoptic code (or SYNOP) provides for reporting the three basic altitude ranges for tropospheric clouds, but makes no special provision for multi-level clouds that can occupy more than one altitude range at a particular time. Consequently, cloud genera with significant vertical development are coded as low when they form in the low or lower-middle altitude range of the troposphere and achieve vertical extent by growing upward into the middle or high altitude range, as is the case with cumulus and cumulonimbus. Conversely, nimbostratus is coded as middle because it usually initially forms at mid-altitudes of the troposphere and becomes vertically developed by growing downward into the low altitude range.[21][28][29] Because of the structure of the SYNOP code, a maximum of three cloud symbols can be plotted for each reporting station that appears on the weather map: one symbol each for a low (or upward growing vertical) cloud type, a middle (or downward growing vertical) type, and one for a high cloud type. The symbol used on the map for each of these levels at a particular observation time will be for the genus, species, variety, mutation, or cloud motion that is considered most important according to criteria set out by the World Meteorological Organization (WMO). If these elements for any synoptic cloud level at the time of observation are deemed to be of equal importance, then the type which is predominant will be coded by the observer and plotted on the weather map. Although the SYNOP code has no separate classification for vertical or multi-level clouds, the observer procedure for selecting numerical codes is designed to give high reporting priority to those genera or species that show significant vertical development.[26]
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Lowcloudsymbols.gif
Low cloud weather map symbols: Includes low and upward-growing vertical.
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Midcloudcymbols.gif
Middle cloud weather map symbols: Includes middle and downward growing vertical.
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Highcloudsymbols.gif
High cloud weather map symbols.
The identitification and reporting of clouds contribute to the process of weather forecasting. Satellite pictures used in conjunction with the cloud symbols plotted on weather maps provide the forecaster with important information about conditions within the troposphere and the weather systems that form as a result. The presence of significant high cirrus or cirrostratus cloud cover indicates an organized low pressure disturbance or an associated warm front is about 300 km away from the point of observation. Clouds associated with warm fronts tend to be mostly stratiform in structure at all altitude levels. However, if cirrocumulus also appears, there is greater airmass instability arriving with the front which increases the risk that thunderstorms may accompany the system. When these high clouds progressively invade the sky and the barometric pressure begins to fall, precipitation associated with the disturbance is likely about 24 to 36 hours away. A thickening and lowering of cirrostratus into mid-level altostratus is a good sign the warm front or low has moved closer and precipitation may begin within 24 hours. A further thickening of the altostratus is often accompanied by virga and the arrival of precipitation is imminent. The cloud layer achieves significant vertical extent as it lowers and changes into nimbostratus.[21] Rain or snow begins to reach surface level at the beginning of a precipitation event that can last up to 36 hours depending and the size of the weather system and its speed of movememnt. As the low and the warm front pass, the nimbostratus thins out into low stratus and the precipitation tapers off.
A cold front tends to give less warning of its approach because it usually moves faster than a warm front and has a narrower band of clouds and weather. If the cold front is active enough to produce thunderstorms, anvil cirrus clouds [32] may spread ahead of the front as a warning of its approach. The other cloud types associated with a cold front are mostly cumuliform, with mid-level altocumulus giving way to lower stratocumulus and intermittent light precipitation if there is only slight airmass instability. With significant instability, vertically developed cumulus or cumulonimbus with showers and thunderstorms will form along the front. After the passage of the front, the sky usually clears as high pressure builds in behind the system, although significant amounts of stratocumulus may persist if the air mass behind the front remains humid. Small and unchanging amounts of cumulus or cirrus clouds in an otherwise clear sky are usually indications of continuing fair weather as long as the barometric pressure remains comparatively high.
High cirrus uncinus and cirrus fibratus upper-left merging into cirrostratus fibratus with some higher cirrocumulus floccus upper right.
High clouds form between 10,000 and 25,000 ft (3,000 and 7,600 m) in the polar regions, 16,500 and 40,000 ft (5,000 and 12,200 m) in the temperate regions and 20,000 and 60,000 ft (6,100 and 18,300 m) in the tropical region. It is the only height range family that includes genera from all three physical categories.[27]
- Genus cirrus (Ci): Fibrous wisps of delicate white ice crystal cloud that show up clearly against the blue sky. Cirrus clouds are generally non-convective except castellanus and floccus species. They often form along a high altitude jetstream and at the very leading edge of a frontal or low pressure disturbance where they may merge into cirrostratus.
- Species cirrus fibratus (Ci fib): Fibrous cirrus with no tufts or hooks (CH1).
- Species cirrus uncinus (Ci unc): Hooked cirrus filaments (CH1).
- Species cirrus spissatus (Ci spi): Patchy dense cirrus (CH2).
- Species cirrus castellanus (Ci cas): Partly turreted cirrus (CH2).
- Species cirrus floccus (Ci flo): Partly tufted cirrus (CH2).
- Opacity-based varieties: None (always translucent).
- Pattern-based varieties: Radiatus (CH4 except CH5 or 6 if accompanied by cirrostratus), intortus, vertebratus, duplicatus.
- Precipitation-based supplementary features: None.
- Accessory cloud: Mamma.
- Genitus mother clouds: Cumulonimbus (CH3), altocumulus, cirrocumulus; Mutatus: Cirrostratus.
- Genus cirrocumulus (Cc): A cloud layer of limited convection composed of ice crystals or supercooled water droplets appearing as small white rounded masses or flakes in groups or lines with ripples like sand on a beach (CH9 for all species). They occasionally form alongside cirrus or cirrostratus clouds at the very leading edge of an active weather system.
- Species cirrocumulus stratiformis (Cc str): Sheets or relatively flat patches of cirrocumulus.
- Species cirrocumulus lenticularis (Cc len): Lens-shaped cirrocumulus.
- Species cirrocumulus castellanus (Cc cas): Turreted cirrocumulus.
- Species cirrocumulus floccus (Cc flo): Tufted cirrocumulus.
- Opacity-based varieties: None (always translucent).
- Pattern-based varieties: Undulatus, lacunosus.
- Precipitation-based supplementary feature: Virga.
- Accessory cloud: Mamma.
- Genitus mother clouds: None; Mutatus: Cirrus, cirrostratus, altocumulus.
- Genus cirrostratus (Cs): A thin non-convective ice crystal veil that typically gives rise to halos caused by refraction of the sun's rays. The sun and moon are visible in clear outline. Cirrostratus typically thickens into altostratus ahead of a warm front or low-pressure area.
- Species cirrostratus fibratus (Cs fib): Fibrous cirrostratus less detached than cirrus (CH8 except CH5 or 6 if increasing in amount) .
- Species cirrostratus nebulosus (Cs neb): A featureless veil of cirrostratus covering the entire sky (CH7).
- Opacity-based varieties: None (always translucent).
- Pattern-based varieties: Duplicatus, undulatus.
- Precipitation-based supplementary features: None.
- Accessory clouds: None.
- Genitus mother clouds: Cirrocumulus, cumulonimbus; Mutatus: Cirrus, cirrocumulus, altostratus.[26]
These clouds tend to form at 6,500 ft (2,000 m) but may form at heights up to 13,000 ft (4,000 m), 23,000 ft (7,000 m) or 25,000 ft (7,600 m) depending on the latitudinal region. In general, the warmer the climate the higher the cloud base. The family of middle clouds typically comprises one cumuliform and one stratiform-category genus.[21]
- Genus altocumulus (Ac): A cloud layer of limited convection usually in the form of irregular patches or rounded masses in groups, lines, or waves. High altocumulus may resemble cirrocumulus but is usually thicker and composed of water droplets so that the bases show at least some light-grey shading. Opaque altocumulus associated with a weak frontal or low-pressure disturbance can produce virga, very light intermittent precipitation that evaporates before reaching the ground. If the altocumulus is mixed with moisture-laden altostratus, the precipitation may reach the ground.
- Species altocumulus stratiformis (Ac str): Sheets or relatively flat patches of altocumulus (synoptic coding determined by predominant variety or by genitus mother cloud).
- Species altocumulus lenticularis (Ac len): Lens-shaped altocumulus (CM4).
- Species altocumulus castellanus (Ac cas): Turreted altocumulus (CM8).
- Species altocumulus floccus (Ac flo): Tufted altocumulus (CM8).
- Opacity-based varieties: Translucidus (CM3), perlucidus (CM3 or 7 depending on predominant opacity), opacus (CM7).
- Pattern-based varieties: Duplicatus (CM7 or occasionally CM9), radiatus (CM5 if increasing in amount), undulatus, lacunosus.
- Precipitation-based supplementary features: Virga.
- Accessory cloud: Mamma.
- Genitus Mother clouds: Cumulus or cumulonimbus (CM6); Mutatus: Cirrocumulus, altostratus, nimbostratus, stratocumulus.
- Genus altostratus (As): An opaque or translucent non-convective veil of grey/blue-grey cloud that often forms along warm fronts and around low-pressure areas where it may thicken into nimbostratus. Altostratus is usually composed of water droplets but may be mixed with ice crystals at higher altitudes. Widespread opaque altostratus can produce light continuous or intermittent precipitation.
- Species: None (always nebulous).
- Opacity-based varieties: Translucidus (CM1), opacus (CM2).
- Pattern-based varieties: Duplicatus, undulatus, radiatus.
- Precipitation-based supplementary features: Virga, praecipitatio.
- Accessory clouds: Pannus (CL7), mamma.
- Genitus Mother clouds: Altocumulus, cumulonimbus; Mutatus: Cirrostratus, nimbostratus.[26]
Low stratocumulus stratiformis clouds mainly in foreground with moderate vertical cumulus humilis and cumulus mediocris in the foreground and background
Low clouds are found from near surface up to 6,500 ft (2,000 m).[27] This family also typically includes one cumuliform and one stratiform-category genus.[29] When low stratiform clouds contact the ground, they are called fog, although radiation and advection types of fog do not form from stratus layers.
- Genus stratocumulus (Sc): A cloud layer of limited convection usually in the form of irregular patches or rounded masses similar to altocumulus but having larger elements with deeper-gray shading (CL5 for all species except CL4 when formed from free convective mother clouds and CL8 when formed separately from co-existent cumulus). Opaque stratocumulus associated with a weak frontal or low-pressure distrubance can produce very light intermittent precipitation. This cloud often forms under a precipitating deck of altostratus or high-based nimbostratus associated with a well-developed warm front, slow-moving cold front, or low-pressure area. This can create the illusion of continuous precipitation of more than very light intensity falling from stratocumulus.
- Species stratocumulus stratiformis (Sc str): Sheets or relatively flat patches of stratocumulus.
- Species stratocumulus lenticularis (Sc len): Lens-shaped stratocumulus.
- Species stratocumulus castellanus (Sc cas): Turreted stratocumulus.
- Opacity-based varieties: Translucidus, perlucidus, opacus.
- Pattern-based varieties: Duplicatus, undulatus, radiatus, lacunosus.
- Precipitation-based supplementary features: Virga, praecipitatio.
- Accessory cloud: Mamma.
- Genitus mother clouds: Cumulus or cumulonimbus (CL4), altostratus, nimbostratus; Mutatus: Altocumulus, nimbostratus, stratus.
- Genus stratus (St): A uniform layer of non-convective cloud resembling fog but not resting on the ground.
- Species stratus nebulosus (St neb): A featureless veil of stratus sometimes producing light drizzle (CL6).
- Species stratus fractus (St fra): A ragged broken up sheet of stratus that often forms in precipitation (CL7) falling from a higher cloud deck. This species may also result from a continuous sheet of stratus becoming broken up by the wind (CL6).
- Opacity-based varieties: Translucidus, opacus.
- Pattern-based variety: Undulatus.
- Precipitation-based supplementary feature: Praecipitatio.
- Accessory clouds: None.
- Genitus mother clouds: Nimbostratus, cumulus, cumulonimbus; Mutatus: Stratocumulus.[26]
Moderate vertical nimbostratus cloud covering the sky with a scattered layer of low stratus fractus in the middle of the upper-half of the image.
These clouds have low to middle bases anywhere from near surface to about 10,000 ft (3,000 m) and, therefore, do not fit very well into the conventional height ranges of low, middle, and high. This family continues the pattern of comprising one cumuliform and one stratiform-category genus. Cumulus usually forms in the low-altitude range, but bases may rise into the lower part of the middle range during conditions of very low relative humidity. Nimbostratus normally forms from altostratus in the middle-altitude range and achieves vertical extent when the base subsides into the low range during precipitation.[21][28][29] Some methods of cloud-height classification reserve the term vertical for upward-growing free-convective cumuliform clouds.[33][34] Downward-growing nimbostratus is then classified as low [33] or middle,[27] even when it becomes very thick as a result of this process – which is often augmented by frontal lift causing non-convective upward growth as well. Some authorities do not use a vertical family designation at all, and therefore also include all free-convective cumuliform types with the family of low clouds.[27] Cumulus fractus and cumulus humilis are two species included here that cannot be described as vertical in the true sense of the word. Being at or near the beginning of the convective cloud's daily life cycle, they lack the moderate vertical extent of cumulus mediocris. Consequently they are sometimes classified as low clouds [27] despite the fact their bases can be in the middle height range when the moisture content of the air is very low. When cumulus fractus and cumulus humilis are classified as vertical,[29] it is on the basis of their potential for at least moderate upward growth during their daily cycle, as well as their ability to form in the middle cloud range during conditions of very low humidity.
- Genus cumulus (Cu): Clouds of free convection with clear-cut flat bases and domed tops. Towering cumulus (cumulus congestus) are usually classified as family D2 clouds of considerable vertical development.
- Species cumulus fractus (Cu fra): Cumulus clouds broken up into ragged and changing fragments (CL1 or 7).
- Species cumulus humilis (Cu hum): Small cumulus clouds usually with just a light-grey shading underneath (CL1).
- Species cumulus mediocris (Cu med): Cumulus clouds of moderate size with medium-grey shading underneath (CL2). Cumulus mediocris can produce scattered showers of light intensity.
- Opacity-based varieties: None (always opaque).
- Pattern-based variety: Radiatus.
- Precipitation-based supplementary features: Virga, praecipitatio.
- Accessory clouds: Pannus (CL7), pileus, velum, arcus, tuba.
- Genitus mother clouds: Altocumulus, stratocumulus; Mutatus: Stratocumulus, stratus.
- Genus nimbostratus (Ns): A diffuse dark-grey non-convective layer that looks feebly illuminated from the inside (CM2). It normally forms from altostratus along warm fronts and around low-pressure areas and produces widespread steady precipitation that can reach moderate or heavy intensity.
- Species: None (always nebulous).
- Opacity-based varieties: None (always opaque).
- Pattern-based varieties: None.
- Precipitation-based supplementary features: Virga, praecipitatio.
- Accessory cloud: Pannus (CL7).
- Genitus mother clouds: Cumulus, cumulonimbus; Mutatus: Altocumulus, altostratus, stratocumulus.[26]
Stages of a cumulonimbus cloud's life.
These clouds can have strong vertical currents and rise far above their bases, which form anywhere in the low to lower-middle altitude range from near surface to about 10,000 ft (3,000 m). Like smaller cumuliform clouds, these towering giants usually form in the low-altitude range at first, but the bases can rise into the middle range when the moisture content of the air is very low. Unlike the other families that each include a cumuliform and stratiform-category genus, the family of towering clouds has instead one distinct cumuliform-category genus, cumulonimbus, and one species of cumulus, a genus otherwise considered a cloud of moderate vertical development. By definition, even very thick stratiform clouds cannot have towering vertical extent or structure, although they may be accompanied by embedded towering cumuliform types.[28] Some authorities consider moderate and towering vertical types to be a single family.[21][29] However, the International Civil Aviation Organization (ICAO) distinguishes towering vertical clouds by specifying that these very large cumuliform types must be identified by genus names or standard abbreviations in all aviation observations (METARS) and forecasts (TAFS) to warn pilots of possible severe weather and turbulance.[35]
- Genus cumulonimbus (Cb): Heavy towering masses of free convective cloud with dark-grey to nearly black bases that are associated with thunderstorms and showers. Thunderstorms can produce a range of severe weather that includes hail, tornadoes, a variety of other localized strong wind events, several types of lightning, and local very heavy downpours of rain that can cause flash floods, although lightning is the only one of these that requires a thunderstorm to be taking place. In general, cumulonimbus require moisture, an unstable air mass, and a lifting force (heat) in order to form. Cumulonimbus typically go through three stages: the developing stage, the mature stage (where the main cloud may reach supercell status in favorable conditions), and the dissipation stage.[36] The average thunderstorm has a 24 km (15 mi) diameter. Depending on the conditions present in the atmosphere, these three stages take an average of 30 minutes to go through.[37]
- Species cumulonimbus calvus (Cb cal): Cumulonimbus clouds with very high clear-cut domed tops similar to towering cumulus (CL3).
- Species cumulonimbus capillatus (Cb cap): Cumulonimbus clouds with very high tops that have become fibrous due to the presence of ice crystals (CL9).
- Opacity-based varieties: None (always opaque).
- Pattern-based varieties: None.
- Precipitation-based supplementary features: Virga, praecipitatio.
- Accessory clouds: Pannus (CL7), incus, mamma, pileus, velum, arcus, tuba.
- Genitus mother clouds: Altocumulus, altostratus, nimbostratus, stratocumulus, cumulus; Mutatus: Cumulus.
- Genus cumulus (Cu)[26]
- Species cumulus congestus (WMO: Cu Con/ICAO: TCu): Towering cumulus clouds of great vertical size, usually with dark-grey bases, and capable of producing severe turbulence and showers of moderate to heavy intensity (CL2).
- Opacity-based varieties: None (always opaque).
- Pattern-based varieties: Radiatus.
- Precipitation-based supplementary features: Virga, praecipitatio.
- Accessory clouds: Pannus (CL7), pileus, velum, arcus, tuba.
- Genitus mother clouds: Altocumulus, stratocumulus; Mutatus: Stratocumulus, stratus.[26]
Non-WMO variant
- Pyrocumulus (No official abbreviation): Cumulus clouds associated with volcanic eruptions and large-scale fires. Pyrocumulus is not recognized by the WMO as a distinct genus or species, but is, in essence, cumulus congestus formed under special circumstances that can also cause severe turbulance.[26]
- nacreous: Nacreous clouds occur occasionally in polar regions of the stratosphere where moisture is very scarce. They are found at altitudes of about 15,000–25,000 m (49,200–82,000 ft) during the winter when that part of the atmosphere is coldest and has the best chance of triggering condensation. Also known as mother of pearl clouds, they are typically very thin with a cirriform appearance.[38] Nacreous clouds are sub-classified alpha-numerically based on chemical makeup rather than variations in physical appearance.
- Type 1: Nacreous containing supercooled nitric acid and water droplets.
Subtypes
-
-
- 1A: Nacreous containing crystals of water and nitric acid.
- 1B: Also contains supercooled sulfuric acid in ternary solution.
- Type 2: Nacreous consisting of water crystals only.
- Noctilucent: The polar air in the mesosphere is coldest during the summer so it is mostly at this time of year that noctilucent clouds are seen.[39] They can occasionally be seen illuminated by the sun during deep twilight at ground level. Noctilucent clouds are the highest in the atmosphere and occur mostly at altitudes of 80 to 85 kilometers (50 to 53 mi),[40] in the mesosphere. An alpha-numeric sub-classification is used to identify variations in physical appearance.
- Type 1: Very tenuous noctilucent resembling cirrus fibratus.
- Type 2: Bands; noctilucent in the form of long streaks, often in groups or interwoven at small angles, similar to cirrus intortus.
Subtypes
-
-
- 2A: Noctilucent streaks with diffuse, blurred edges.
- 2B: Streaks with sharply defined edges.
- Type 3: Billows; noctilucent in the form of short streaks that are clearly spaced and roughly parallel.
Subtypes
-
-
- 3A: Noctilucent in the form of short, straight, narrow streaks.
- 3B: Wave-like streaks similar to cirrus undulatus.
- Type 4: Whirls; noctilucent in the form of partial or rarely complete rings with dark centers.
Subtypes
-
-
- 4A: Noctilucent whirls of small angular radius having a similar appearance to surface water ripples.
- 4B: Simple curve of medium angular radius with one or more bands.
- 4C: Whirls with large-scale ring structure.
Striking cloud colorations can be seen at many altitudes in the homosphere, which includes the troposphere, stratosphere, and mesophere. The first recorded colored cloud was seen by Nathan Ingleton in 1651, he wrote the event in his diary but the records were destroyed in 1666, in the Great Fire of London. The color of a cloud, as seen from Earth, tells much about what is going on inside the cloud.
In the troposphere, dense, deep clouds exhibit a high reflectance (70% to 95%) throughout the visible spectrum. Tiny particles of water are densely packed and sunlight cannot penetrate far into the cloud before it is reflected out, giving a cloud its characteristic white color, especially when viewed from the top.[41] Cloud droplets tend to scatter light efficiently, so that the intensity of the solar radiation decreases with depth into the gases. As a result, the cloud base can vary from a very light to very-dark-grey depending on the cloud's thickness and how much light is being reflected or transmitted back to the observer. Thin clouds may look white or appear to have acquired the color of their environment or background. High tropospheric clouds appear mostly white if composed entirely of ice crystals or supercooled water droplets.
As a tropospheric cloud matures, the dense water droplets may combine to produce larger droplets. If the droplets become too large and heavy to be kept aloft by the air circulation, they will fall from the cloud as rain. By this process of accumulation, the space between droplets becomes increasingly larger, permitting light to penetrate farther into the cloud. If the cloud is sufficiently large and the droplets within are spaced far enough apart, a percentage of the light that enters the cloud is not reflected back out but is absorbed giving the cloud a darker look. A simple example of this is one's being able to see farther in heavy rain than in heavy fog. This process of reflection/absorption is what causes the range of cloud color from white to black.[42]
Other colors occur naturally in tropospheric clouds. Bluish-grey is the result of light scattering within the cloud. In the visible spectrum, blue and green are at the short end of light's visible wavelengths, whereas red and yellow are at the long end. The short rays are more easily scattered by water droplets, and the long rays are more likely to be absorbed. The bluish color is evidence that such scattering is being produced by rain-size droplets in the cloud. A cumulonimbus cloud that appears to have a greenish/bluish tint is a sign that it contains extremely high amounts of water; hail or rain. Supercell type storms are more likely to be characterized by this but any storm can appear this way. Coloration such as this does not directly indicate that it is a severe thunderstorm, it only confirms its potential. Since a green/blue tint signifies copious amounts of water, a strong updraft to support it, high winds from the storm raining out, and wet hail; all elements that improve the chance for it to become severe, can all be inferred from this. In addition, the stronger the updraft is, the more likely the storm is to undergo tornadogenesis and to produce large hail and high winds.[43] Yellowish clouds may occur in the late spring through early fall months during forest fire season. The yellow color is due to the presence of pollutants in the smoke. Yellowish clouds caused by the presence of nitrogen dioxide are sometimes seen in urban areas with high air pollution levels.[44]
Within the troposphere, red, orange, and pink clouds occur almost entirely at sunrise/sunset and are the result of the scattering of sunlight by the atmosphere. When the angle between the sun and the horizon is less than 10 percent, as it is just after sunrise or just prior to sunset, sunlight becomes too red due to refraction for any colors other than those with a reddish hue to be seen.[45] The clouds do not become that color; they are reflecting long and unscattered rays of sunlight, which are predominant at those hours. The effect is much like if one were to shine a red spotlight on a white sheet. In combination with large, mature thunderheads, this can produce blood-red clouds. Clouds look darker in the near-infrared because water absorbs solar radiation at those wavelengths.
In high latitude regions of the stratosphere, nacreous clouds occasionally found there during the polar winter tend to display quite striking displays of mother-of-pearl colorations due to the refraction and diffusion of the sun's rays through thin ice crystal clouds that often contain compounds other than water. At still higher altitudes up in the mesospere, noctilucent clouds sometimes seen in polar regions in the summer usually appear a silvery white that can resemble brightly illuminated cirrus.
Global cloud cover, averaged over the month of October 2009.
NASA composite satellite image; larger image available
here.
The role of tropospheric clouds in regulating weather and climate remains a leading source of uncertainty in projections of global warming.[46] This uncertainty arises because of the delicate balance of processes related to clouds, spanning scales from millimeters to planetary. Hence, interactions between the large-scale (synoptic meteorology) and clouds becomes difficult to represent in global models. The complexity and diversity of clouds, as outlined above, adds to the problem. On the one hand, white-colored cloud tops promote cooling of Earth's surface by reflecting shortwave radiation from the sun. Most of the sunlight that reaches the ground is absorbed, warming the surface, which emits radiation upward at longer, infrared, wavelengths. At these wavelengths, however, water in the clouds acts as an efficient absorber. The water reacts by radiating, also in the infrared, both upward and downward, and the downward radiation results in a net warming at the surface. This is analogous to the greenhouse effect of greenhouse gases and water vapor.
High tropospheric clouds, such as cirrus, particularly show this duality with both shortwave albedo cooling and longwave greenhouse warming effects that nearly cancel or slightly favor net warming with increasing cloud cover. The shortwave effect is dominant with middle and low clouds like altocumulus and stratocumulus, which results in a net cooling with almost no longwave effect. As a consequence, much research has focused on the response of low clouds to a changing climate. Leading global models can produce quite different results, however, with some showing increasing low-level clouds and others showing decreases.[47][48]
Polar stratospheric and mesospheric clouds are not common or widespread enough to have a significant effect on climate. However an increasing frequency of occurrence of noctilucent clouds since the 19th century may be the result of climate change.[49]
New research indicates a global brightening trend.[50] The details are not fully understood, but much of the global dimming (and subsequent reversal) is thought to be a consequence of changes in aerosol loading in the atmosphere, especially sulfur-based aerosol associated with biomass burning and urban pollution. Changes in aerosol burden can have indirect effects on clouds by changing the droplet size distribution[51] or the lifetime and precipitation characteristics of clouds.[52]
Bioprecipitation, the concept of rain-making bacteria, was proposed by David Sands from Montana State University. Such microbes – called ice nucleators – are found in rain, snow, and hail throughout the world. These bacteria may be part of a constant feedback between terrestrial ecosystems and clouds and may even have evolved the ability to promote rainstorms as a means of dispersal. They may rely on the rainfall to spread to new habitats, much as some plants rely on windblown pollen grains.[53][54]
Within our Solar System, any planet or moon with an atmosphere also has clouds. Venus's thick clouds are composed of sulfur dioxide. Mars has high, thin clouds of water ice. Both Jupiter and Saturn have an outer cloud deck composed of ammonia clouds, an intermediate deck of ammonium hydrosulfide clouds and an inner deck of water clouds.[55][56] Saturn's moon Titan has clouds believed to be composed largely of methane.[57] The Cassini–Huygens Saturn mission uncovered evidence of a fluid cycle on Titan, including lakes near the poles and fluvial channels on the surface of the moon. Uranus and Neptune have cloudy atmospheres dominated by water vapor and methane gas.[58][59]
- ^ a b Glossary of Meteorology (June 2000). "Adiabatic Process". American Meteorological Society. http://amsglossary.allenpress.com/glossary/search?id=adiabatic-process1. Retrieved 2008-12-27.
- ^ Steve Horstmeyer (2008). "Why don't clouds fall?". http://lamp.tu-graz.ac.at/~hadley/whydontcloudsfall.html. Retrieved 2012-04-06.
- ^ Dowling & Radke 1990, p. 977
- ^ Steve Horstmeyer (2008). "Cloud Drops, Rain Drops". http://www.shorstmeyer.com/wxfaqs/float/float.html. Retrieved 2012-03-19.
- ^ Dr. Michael Pidwirny (2008). "CHAPTER 8: Introduction to the Hydrosphere (e). Cloud Formation Processes". Physical Geography. http://www.physicalgeography.net/fundamentals/8e.html. Retrieved 2009-01-01.
- ^ Glossary of Meteorology (2009). "Radiational cooling". American Meteorological Society. http://amsglossary.allenpress.com/glossary/search?p=1&query=radiational+cooling&submit=Search. Retrieved 2008-12-27.
- ^ Robert Fovell (2004). "Approaches to saturation". University of California in Los Angeles. http://www.atmos.ucla.edu/~fovell/AS3downloads/saturation.pdf. Retrieved 2009-02-07.
- ^ Robert Penrose Pearce (2002). Meteorology at the Millennium. Academic Press. p. 66. ISBN 978-0-12-548035-2. http://books.google.com/?id=QECy_UBdyrcC&pg=PA66&lpg=PA66&dq=ways+to+moisten+the+atmosphere. Retrieved 2009-01-02.
- ^ National Weather Service Office, Spokane, Washington (2009). "Virga and Dry Thunderstorms". National Oceanic and Atmospheric Administration. http://www.wrh.noaa.gov/otx/outreach/ttalk/virga.php. Retrieved 2009-01-02.
- ^ Bart van den Hurk and Eleanor Blyth (2008). "Global maps of Local Land-Atmosphere coupling". KNMI. http://www.knmi.nl/~hurkvd/Loco_workshop/Workshop_report.pdf. Retrieved 2009-01-02.
- ^ H. Edward Reiley, Carroll L. Shry (2002). Introductory horticulture. Cengage Learning. p. 40. ISBN 978-0-7668-1567-4. http://books.google.com/?id=jZvsnsLIkNsC&pg=PA40&lpg=PA40&dq=plant+transpiration+adds+moisture+to+air+book#v=onepage&q&f=false. Retrieved 2011-01-31.
- ^ JetStream (2008). "Air Masses". National Weather Service. http://www.srh.weather.gov/srh/jetstream/synoptic/airmass.htm. Retrieved 2009-01-02.
- ^ Kirill I︠A︡kovlevich Kondratʹev (2006). Atmospheric aerosol properties: formation, processes and impacts. Springer. p. 403. ISBN 978-3-540-26263-3. http://books.google.com/books?id=tcCTsENwgGYC&pg=PA411&dq=molecular+scattering+aerosol+in+atmosphere&hl=en&sa=X&ei=WfVGT-LlFMre0gGpyvH5DQ&ved=0CDAQ6AEwAA#v=onepage&q=molecular%20scattering%20aerosol%20in%20atmosphere&f=false.
- ^ a b Yochanan Kushnir (2000). "The Climate System: General Circulation and Climate Zones". http://eesc.columbia.edu/courses/ees/climate/lectures/gen_circ/index.html. Retrieved 2012-03-13.
- ^ Jack Williams (1997). "Extratropical storms are major weather makers". http://www.usatoday.com/weather/wstorm.htm. Retrieved 2012-03-13.
- ^ National Centre for Medium Range Forecasting. Chapter-II Monsoon-2004: Onset, Advancement and Circulation Features. Retrieved on 2008-05-03.
- ^ Australian Broadcasting Corporation. Monsoon. Retrieved on 2008-05-03.
- ^ ThinkQuest team 26634 (1999). The Formation of Deserts. Oracle ThinkQuest Education Foundation. Retrieved on 2009-02-16.
- ^ John D. Cox (2002). Storm Watchers. John Wiley & Sons, Inc.. pp. 13–17.
- ^ a b c Office National Meteorologique (1932). International Atlas of Clouds and of States of the Sky. Paris. p. II.
- ^ a b c d e f g h i j k Paul Hancock and Brian Skinner (2000). "clouds. The Oxford Companion to the Earth". http://www.encyclopedia.com/topic/cloud.aspx#1-10112:clouds-full. Retrieved 2011-02-22.
- ^ Scott, A (2000). "The Pre-Quaternary history of fire". Palaeogeography Palaeoclimatology Palaeoecology 164 (1-4): 281. DOI:10.1016/S0031-0182(00)00192-9.
- ^ National Center for Atmospheric Research (2008). "Hail". University Corporation for Atmospheric Research. http://www.ncar.ucar.edu/research/meteorology/storms/hail.php. Retrieved 2009-07-18.
- ^ Ted Fujita (1985). "The Downburst, microburst and macroburst". SMRP Research Paper 210, 122 pp.
- ^ Nilton O. Renno (August 2008). "A thermodynamically general theory for convective vortices" (PDF). Tellus A 60 (4): 688–99. Bibcode 2008TellA..60..688R. DOI:10.1111/j.1600-0870.2008.00331.x. http://vortexengine.ca/misc/Renno_2008.pdf.
- ^ a b c d e f g h i j k l m n o p q World Meteorological Organization (1995). "WMO cloud classifications". http://www.weatheranswer.com/public/Clouds_WMO.pdf. Retrieved 2012-02-01.
- ^ a b c d e f JetStream (2010-01-05). "Cloud Classifications". National Weather Service. http://www.srh.weather.gov/srh/jetstream/synoptic/clouds_max.htm. Retrieved 2011-01-31.
- ^ a b c d Jim Koermer (2011). "Plymouth State Meteorology Program Cloud Boutique". Plymouth State University. http://vortex.plymouth.edu/clouds.html/. Retrieved 2011-01-31.
- ^ a b c d e f Clouds Online (2012). "Cloud Atlas". http://www.clouds-online.com. Retrieved 2012-02-01.
- ^ a b c Morris (2008). "Clouds - Species and Varieties". http://www.morris.umn.edu/~sboyd/weather/cloudsystems/Clouds_files/speciesandvarieties.htm. Retrieved 2012-02-04.
- ^ Images/images.php.3?img-id=17053 "Cloud Formations off the West Coast of South America". NASA Earth Observatory. http://earthobservatory.nasa.gov/Newsroom/New Images/images.php.3?img-id=17053. Retrieved 2006-05-04.
- ^ Grence & Nese 2001, p. 212
- ^ a b "cloud: Classification of Clouds". Infoplease.com. http://www.infoplease.com/ce6/weather/A0857400.html.
- ^ Becca Hatheway (2009). "Cloud Types". http://www.windows2universe.org/earth/Atmosphere/clouds/cloud_types.html. Retrieved 2011-09-15.
- ^ Paul de Valk, Rudolf van Westhrenen, and Cintia Carbajal Henken (2010). "Automated CB and TCU detection using radar and satellite data: from research to application". http://www.eumetsat.int/Home/Main/AboutEUMETSAT/Publications/ConferenceandWorkshopProceedings/2010/groups/cps/documents/document/pdf_conf_p57_s7_08_devalk_v.pdf. Retrieved 2011-09-15.
- ^ Micheal H. Mogil (2007). Extreme Weather. New York: Black Dog & Leventhal Publisher. pp. 210–211. ISBN 978-1-57912-743-5.
- ^ National Severe Storms Laboratory (2006-10-15). "A Severe Weather Primer: Questions and Answers about Thunderstorms". National Oceanic and Atmospheric Administration. http://www.nssl.noaa.gov/primer/tstorm/tst_basics.html. Retrieved 2009-09-01.
- ^ Les Cowley (2011). "Nacreous clouds – Atmospheric optics". http://www.atoptics.co.uk/highsky/nacr1.htm. Retrieved 2012-01-31.
- ^ Kenneth Chang (2008-09-25). "Caltech Scientist Proposes Explanation for Puzzling Property of Night-Shining Clouds at the Edge of Space". http://www.media.caltech.edu/search?sitesearch=media.caltech.edu&query=noctilucent&start=0. Retrieved 2008-10-19.
- ^ Michael Gadsden and Pekka Parviainen (September 2006). Observing Noctilucent Clouds. International Association of Geomagnetism & Aeronomy. p. 9. http://www.iugg.org/IAGA/iaga_pages/pdf/ONC_Sep06.pdf. Retrieved 2011-01-31.
- ^ Increasing Cloud Reflectivity, Royal Geographical Society, 2010
- ^ Clouds absorb more solar radiation than previously thought (blacker than they appear), Chem. Eng. News, 1995, p33
- ^ http://www.meted.ucar.edu/spotter_training/convective/navmenu.php?tab=1&page=2.7.0 © 2011 MetEd/UCAR
- ^ Cities and Air Pollution, Nature, 1998, chapter 10
- ^ Frank W. Gallagher, III. (October 2000). "Distant Green Thunderstorms - Frazer's Theory Revisited". Journal of Applied Meteorology (American Meteorological Society) 39 (10): 1754–1757. Bibcode 2000JApMe..39.1754G. DOI:10.1175/1520-0450-39.10.1754.
- ^ D. Randall, R. Wood, S. Bony, R. Colman, T. Fichefet, J. Fyfe, V. Kattsov, A. Pitman, J. Shukla, J. Srinivasan, R. Stouffer, A. Sumi, and K. Taylor. Climate models and their evaluation. In S. Solomon, D. Qin, M. Manning, Z. Chen, M. Marquis, K. Averyt, M.Tignor, and H. Miller, editors, Climate Change 2007: The Physical Science Basis. Contribution of Working Group I to the Fourth Assessment Report of the Intergovernmental Panel on Climate Change. Cambridge University Press, Cambridge, United Kingdom and New York, NY, USA, 2007.
- ^ S. Bony and J.-L. Dufresne. Marine boundary layer clouds at the heart of tropical cloud feedback uncertainties in climate models. Geophys. Res. Lett., 32, 10 2005. URL http://dx.doi.org/10.1029/2005GL023851.
- ^ B. Medeiros, B. Stevens, I.M. Held, M. Zhao, D.L. Williamson, J.G. Olson, and C.S. Bretherton. Aquaplanets, climate sensitivity, and low clouds. J. Climate, 21(19):4974–4991, 2008.
- ^ Kenneth Chang (2008-09-25). "Caltech Scientist Proposes Explanation for Puzzling Property of Night-Shining Clouds at the Edge of Space". http://www.media.caltech.edu/search?sitesearch=media.caltech.edu&query=noctilucent&start=0. Retrieved 2012-03-13.
- ^ Martin Wild, Hans Gilgen, Andreas Roesch, Atsumu Ohmura, Charles N. Long, Ellsworth G. Dutton, Bruce Forgan, Ain Kallis, Viivi Russak, and Anatoly Tsvetkov. From dimming to brightening: Decadal changes in solar radiation at Earth's surface. Science, 308(5723):847–850, 5 2005. URL http://www.sciencemag.org/cgi/content/abstract/308/5723/847.
- ^ S. A. Twomey. Pollution and the planetary albedo. Atmos. Environ., 8:1251–1256, 1974.
- ^ B. Stevens and G. Feingold. Untangling aerosol effects on clouds and precipitation in a buffered system. Nature, 461(7264):607–613, 10 2009.
- ^ Brent Christner (2008-02-28). "LSU scientist finds evidence of 'rain-making' bacteria". American Association for the Advancement of Science. http://www.eurekalert.org/pub_releases/2008-02/lsu-lsf022808.php. Retrieved 2011-01-31.
- ^ Christine Dell'Amore (2009-01-12). "Rainmaking Bacteria Ride Clouds to "Colonize" Earth?". National Geographic. http://news.nationalgeographic.com/news/pf/64122879.html. Retrieved 2011-01-31.
- ^ 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. "Dynamics of Jupiter’s Atmosphere" (PDF). Lunar & Planetary Institute. http://www.lpl.arizona.edu/~showman/publications/ingersolletal-2004.pdf. Retrieved 2007-02-01.
- ^ Monterrey Institute for Research in Astronomy (2006-08-11). "Saturn". http://www.mira.org/fts0/planets/100/text/txt002x.htm. Retrieved 2011-01-31.
- ^ Athéna Coustenis and F.W. Taylor (2008). Titan: Exploring an Earthlike World. World Scientific. pp. 154–155. ISBN 978-981-270-501-3. http://books.google.com/?id=j3O47dxrDAQC&printsec=frontcover.
- ^ Lunine, Jonathan I. (September 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. edit
- ^ Linda T. Elkins-Tanton (2006). Uranus, Neptune, Pluto, and the Outer Solar System. New York: Chelsea House. pp. 79–83. ISBN 0-8160-5197-6.
Cloud genera and selected species, supplementary features, and other airborne hydrometeors
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| Very high-level |
Polar stratospheric cirriform type: Nacreous
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| High-level |
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| Medium-level |
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| Low-level |
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| Moderate vertical |
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| Towering vertical |
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| Surface based |
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| Non-height specific |
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vep:Pil'v
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