Atmospheric humidification. Humidification, humidification coefficients At what humidification coefficient
Humidification of the territory is determined not only by the amount of precipitation, but also by evaporation. With the same amount of precipitation, but different volatility, the moisture conditions can be different.
Humidification coefficients are used to characterize the humidification conditions. There are over 20 ways to express it. The most common are the following moisture indicators:
- Hydrothermal coefficient G.T. Selyaninov.
where R is the monthly amount of precipitation;
Σt is the sum of temperatures for a month (close to the evaporation rate).
- Moisture coefficient of Vysotsky-Ivanov.
where R is the amount of precipitation for the month;
E p - monthly evaporation.
Humidification coefficient of about 1 - normal humidification, less than 1 - insufficient, more than 1 - excessive.
- Radiation dryness index M.I. Budyko.
where R i is the radiation index of dryness, it shows the ratio of the value of the radiation balance R to the amount of heat Lr required for evaporation of precipitation per year (L is the latent heat of vaporization).
The Radiation Dryness Index shows how much of the residual radiation is spent on evaporation. If the heat is less than that required for the evaporation of the annual precipitation, moisture will be excessive. At R i 0.45, the moisture is excessive; when R i = 0.45-1.00 humidification is sufficient; when R i = 1.00-3.00 humidification is insufficient.
Atmospheric humidification
The amount of precipitation falling without taking into account landscape conditions is an abstract value, because it does not determine the conditions for wetting the territory. So, in the tundra of Yamal and the semi-deserts of the Caspian lowland, the same amount of precipitation falls - about 300 mm, but in the first case, moisture is excessive, swampiness is great, in the second, there is insufficient moisture, the vegetation here is dry-loving, xerophytic.
The wetting of the territory is understood as the ratio between the amount of atmospheric precipitation ( R) falling out in a given area, and evaporation ( E n) for the same period (year, season, month). This ratio, expressed as a percentage, or in fractions of one, is called the moisture coefficient ( K yv = R/E n) (according to N. N. Ivanov). The moisture coefficient shows either excessive moisture (K uv> 1), if precipitation exceeds the evaporation possible at a given temperature, or various degrees of insufficient moisture (K uv<1), если осадки меньше испаряемости.
The nature of humidification, that is, the ratio of heat and moisture in the atmosphere, is the main reason for the existence of natural plant zones on Earth.
According to hydrothermal conditions, several types of territories are distinguished:
1. Areas with excessive moisture - TO UV is more than 1, i.e. 100-150%. These are zones of tundra and forest-tundra, and with sufficient heat, forests of temperate, tropical and equatorial latitudes. Such waterlogged areas are called humid, and waterlogged areas are called extra-humid (Latin humidus - wet).
2. Territories of optimal (sufficient) humidification are narrow zones where TO SW about 1 (about 100%). Within their limits, there is a proportionality between the amount of precipitation and evaporation. These are narrow strips of deciduous forests, sparsely variably humid forests and humid savannas. The conditions here are favorable for the growth of mesophilic plants.
3. Territories of moderately insufficient (unstable) moisture. Different degrees of unstable moisture are distinguished: territories with TO hv = 1-0.6 (100-60%) typical meadow steppes (forest-steppe) and savanna, with TO hv = 0.6-0.3 (60-30%) - dry steppes, dry savannas. They are characterized by a dry season, which complicates agricultural development due to frequent droughts.
4. Territories of insufficient moisture. Allocate arid zones (Latin aridus - dry) with TO hv = 0.3-0.1 (30-10%), semi-deserts are typical here, and extra-arid zones with TO sw less than 0.1 (less than 10%) - deserts.
In areas with excessive moisture, the abundance of moisture negatively affects the processes of aeration (ventilation) of the soil, i.e., on the gas exchange of soil air with atmospheric air. The lack of oxygen in the soil is formed due to the filling of the pores with water, which is why air does not enter there. This disrupts biological aerobic processes in the soil, the normal development of many plants is disrupted or even stopped. In such areas, hygrophyte plants grow and hygrophilic animals live, which are adapted to damp and humid habitats. To involve territories with excessive moisture in the economic, primarily agricultural, turnover, drainage reclamation is necessary, that is, measures aimed at improving the water regime of the territory, removal of excess water (drainage).
There are more areas with insufficient moisture on Earth than waterlogged ones. In arid zones, agriculture is impossible without irrigation. The main reclamation measure in them is irrigation - artificial replenishment of moisture reserves in the soil for the normal development of plants and watering - the creation of sources of moisture (ponds, wells and other reservoirs) for domestic and economic needs and livestock watering.
Under natural conditions, in deserts and semi-deserts, plants that are adapted to dryness grow - xerophytes. They usually have a powerful root system capable of extracting moisture from the soil, small leaves, sometimes turned into needles and thorns to evaporate less moisture, stems and leaves are often covered with a waxy coating. A special group of plants among them is formed by succulents, which accumulate moisture in stems or leaves (cacti, agaves, aloe). Succulents grow only in warm tropical deserts, where there are no freezing temperatures. Desert animals - xerophiles are also adapted to dryness in different ways, for example, they hibernate during the driest period (ground squirrels), are content with the moisture contained in food (some rodents).
Droughts are inherent in areas with insufficient moisture. In deserts and semi-deserts, these are annual phenomena. In the steppes, which are often called the arid zone, and in the forest-steppe, droughts occur in the summer once every few years, sometimes they cover the end of spring - the beginning of autumn. Drought is a long (1-3 months) period without rain or with very little rainfall, at elevated temperatures and low absolute and relative humidity of air and soil. Distinguish between atmospheric and soil droughts. Drought occurs earlier. Due to high temperatures and a large moisture deficit, the transpiration of plants increases sharply, the roots do not have time to supply moisture to the leaves, and they wither. Soil drought is expressed in the drying out of the soil, due to which the normal vital activity of plants is completely disrupted and they die. Soil drought is shorter than atmospheric drought due to the spring moisture reserves in the soil and groundwater. Droughts are caused by the anticyclonic weather regime. In anticyclones, the air sinks, heats up adiabatically and dries up. On the periphery of anticyclones, winds are possible - dry winds with high temperatures and low relative humidity (up to 10-15%), which increase evaporation and even more destructive effect on plants.
In the steppes, irrigation is most effective with sufficient river flow. Additional measures are snow accumulation - preserved stubble in the fields and planting shrubs along the edge of the beams so that snow does not blow away in them, and snow retention - rolling snow, creating snow banks, covering snow with straw in order to increase the duration of snow melting and replenish groundwater reserves. Also effective are forest shelter belts, which delay the flow of melted snow water and lengthen the period of snow melting. Windproof (windbreaking) forest strips of great length, planted in several rows, weaken the speed of winds, including dry winds, and thereby reduce moisture evaporation.
Literature
- Zubashchenko E.M. Regional physical geography. Climates of the Earth: teaching aid. Part 1. / E.M. Zubashchenko, V.I. Shmykov, A. Ya. Nemykin, N.V. Polyakova. - Voronezh: VSPU, 2007 .-- 183 p.
1) Using the maps of the textbook and the atlas, establish what changes in the location of vegetation zones occurred on the territory of the Russian Plain after the Quaternary glaciation.
After the glaciation, the area of the natural zone of the tundra and forest-tundra decreased. She moved north. The area of forest zones has increased.
2) Which countries of the near abroad (former republics of the USSR) are located within the Russian Plain?
Belarus, Latvia, Lithuania, Estonia, Moldova, Ukraine, Poland, Romania, Kazakhstan.
Questions in paragraph
* Using Figure 85, determine which zonal natural complexes are distinguished on the Russian Plain. Which ones occupy the largest area? Which are the smallest?
Zonal natural complexes - tundra and forest-tundra, taiga, mixed and deciduous forests, forest-steppe and steppe, desert and semi-desert.
The largest area is occupied by forests - taiga, mixed and deciduous. The smallest are deserts and semi-deserts.
* According to the profile and schedule, determine what temperatures prevail in this natural complex in winter and summer. What is the relationship between air temperature and humidification coefficient? Explain why the soils of the steppe zone have the most powerful humus horizon.
The Russian Plain is characterized by an increase in temperatures from north to south. Winter temperatures are on average -100-00C, summer temperatures are from +5 to 300C. The moisture coefficient also changes. In the northern regions, waterlogging is observed, the middle strip has sufficient moisture, in the southern regions there is a lack of moisture. In general, with increasing temperatures, the moisture coefficient decreases. In the steppes, there is little precipitation, and the evaporation rate is 2 times higher than the amount of precipitation, there are no conditions for the leaching of humus into the depths of the soil horizons. Chernozems with a very dark color and granular structure are widespread in the steppe.
* Remember what is the mechanism of formation of salt licks and salt marshes.
The reason for the formation of salt marshes is a large evaporation of water from the soil surface under conditions of an effusion type of water regime. When the groundwater is located close to the surface, the water consumption for evaporation is compensated by their inflow. If the groundwater is mineralized, then after the evaporation of water, salts remain in the capillaries, which gradually accumulate. Saline soil-forming rocks, impulse formation, bringing of salt by the wind, improper irrigation, mineralization of halophytic plants rich in sodium, sulfur, and chlorine can also be the cause of the genesis of saline soils. Solonets soils are formed during desalinization of salt marshes in conditions of a large amount of sodium salts and periodic soaking of the soil
Questions at the end of a paragraph
1. What large natural complexes are located on the Russian Plain?
Tundra and forest-tundra, taiga, mixed and deciduous forests, forest-steppe and steppe, deserts and semi-deserts.
2. Explain how a change in at least one of the components of nature, for example, the moisture coefficient, changes the appearance of the entire natural complex.
All components of the natural complex are closely interconnected. For example, when the moisture coefficient changes towards a decrease, the vegetation changes: forests are replaced by forest-steppe, forest-steppe - by steppes, steppes - by semi-deserts, semi-deserts - by deserts. The animal world is inextricably linked with the vegetation cover. Different types of soil are formed under different types of vegetation.
3. Tell us which of the natural complexes of the Russian Plain have been most strongly modified by man.
The steppes of the Russian Plain have been most strongly changed by man. They are almost universally plowed up.
Humidity coefficient is a special indicator developed by experts in the field of meteorology to assess the degree of climate humidity in a particular region. At the same time, it was taken into account that the climate is a long-term characteristic of weather conditions in a given area. Therefore, it was also decided to consider the moisture coefficient in a long time frame: as a rule, this coefficient is calculated on the basis of data collected during the year.
Thus, the moisture coefficient shows how much precipitation falls during this period in the region under consideration. This, in turn, is one of the main factors determining the prevailing type of vegetation in this area.
The formula for calculating the moisture coefficient is as follows: K = R / E. In this formula, the symbol K denotes the actual moisture coefficient, and the symbol R - the amount of precipitation that fell in a given area during the year, expressed in millimeters. Finally, the E symbol represents the amount of precipitation that has evaporated from the surface of the earth during the same period of time.
The specified amount of precipitation, which is also expressed in millimeters, depends on the type of soil, the temperature in the region at a particular time, and other factors. Therefore, despite the seeming simplicity of the above formula, the calculation of the moisture coefficient requires a large number of preliminary measurements using precise instruments and can only be carried out by a sufficiently large team of meteorologists.
In turn, the value of the moisture coefficient in a particular territory, taking into account all these indicators, as a rule, allows determining with a high degree of reliability which type of vegetation is predominant in this region. So, if the moisture coefficient exceeds 1, this indicates a high level of moisture in this area, which entails the predominance of such types of vegetation as taiga, tundra or forest-tundra.
Adequate moisture level corresponds to a moisture coefficient of 1, and, as a rule, is characterized by a predominance of mixed or deciduous forests. Moisture coefficient in the range from 0.6 to 1 is typical for forest-steppe areas, from 0.3 to 0.6 - for steppes, from 0.1 to 0.3 - for semi-desert territories, and from 0 to 0.1 - for deserts ...
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House Atmospheric humidification
On the earth's surface, two oppositely directed processes constantly occur - irrigation of the area with precipitation and drying it by evaporation. Both of these processes merge into a single and contradictory process. atmospheric humidification, under which it is customary to understand the ratio of precipitation and evaporation.
There are over twenty ways to express atmospheric moisture. The indicators are called indices and coefficients or dryness or atmospheric humidification. The most famous are the following:
Hydrothermal coefficient G.T . Selyaninova :
GTK = 10 R / Et, where
R - monthly amount of precipitation,
Еt - the sum of temperatures for the same time; it is close to the evaporation rate.
Radiation index of dryness M. I. Budyko:
Ri = R / LE is the ratio of the radiation balance to the amount of heat, which is extremely important for the evaporation of precipitation over a year.
In the range of the radiation index of dryness from 0.35 to 1.1, there are humid zones (tudra zone and forest zones of different latitudes); from 1.1 to 2.2 - seven-humid zones (forest-steppe, savanna, steppe); from 2.2 to 3.4 - semi-desert; over 3.4 - deserts.
Humidification coefficient of G.N. Vysotsky - N.N. Ivanov:
where R is the amount of precipitation (in mm) per month,
Ep is the monthly evaporation rate.
It is best expressed as a percentage (٪). For example, in the tundra, precipitation is 300 mm, and the evaporation rate is only 200 mm.
502: Bad Gateway
Consequently, precipitation exceeds evaporation by 1.5 times; atmospheric humidification is equal to 150%, or K = 1.5.
Humidification happens redundant, more than 100%, or K> 1.0, when there is more precipitation than it can evaporate; sufficient at which the amount of precipitation and evaporation are approximately equal (about 100%), or K = 1.0; insufficient less than 100%, or K< 1,0, если испаряемость превосходит количество осадков; в последней градации полезно выделить ничтожное увлажнение, в котором осадки составляют ничтожную (13% и меньше, или = 0,13) долю испаряемости.
In the zone of tundra, forests of temperate latitudes and equatorial forests, moisture is excessive (from 100 to 150%).
In the forest-steppe and savannas, it is normal - slightly more or less than 100%, usually from 99 to 60%.
From the forest-steppe towards the deserts of the temperate latitudes and from the savannahs to the tropical deserts, moisture decreases; it is insufficient everywhere: in the steppes 60%, in dry steppes from 60 to 30%, in semi-deserts less than 30% and in deserts from 13 to 10%.
According to the degree of humidity, the zones are humid - moist with excessive moisture and arid - dry with insufficient moisture. The degree of aridity and humidity is different and is expressed by the ratio of precipitation and evaporation.
Droughts. In the zones of forest-steppe and steppes, where moisture is 100% or slightly less, even a slight decrease in precipitation leads to droughts. Meanwhile, the variability of monthly precipitation amounts here fluctuates around 50-70%, and in some places reaches 90%.
Drought - a long, sometimes up to 60-70 days, spring or summer period without rain or with precipitation below normal and with high temperatures. As a result, the reserves of soil moisture are depleted, the yield is reduced or completely dies.
Distinguish atmospheric and soil drought. The first is characterized by a lack of precipitation, low humidity and high air temperatures. The second is expressed in the drying out of the soil, leading to the death of plants. Soil drought can be shorter than atmospheric drought due to the spring moisture reserves in the soil or its input from the soil.
Droughts occur in years of particularly intense atmospheric circulation, when anticyclones are stable and extensive on the Great Continental Axis of Voeikov, the sinking air heats up and dries up.
News and Society
What is moisture coefficient and how is it determined?
The water cycle in nature is one of the most important processes in the geographic envelope. It is based on two interrelated processes: the moistening of the earth's surface by precipitation and the evaporation of moisture from it into the atmosphere. Both of these processes determine the moisture coefficient for a particular area. What is moisture coefficient and how is it determined? This is what this white paper is about.
Humidification factor: definition
Humidification of a territory and evaporation of moisture from its surface are exactly the same all over the world. However, the question of what the moisture coefficient is, in different countries of the planet, they answer completely differently. And the concept itself in such a formulation is not accepted in all countries. For example, in the USA this is the "precipitation-evaporation ratio", which can be literally translated as "the index (ratio) of moisture and evaporation".
But still, what is the moisture coefficient? This is a certain ratio between the amount of precipitation and the level of evaporation in a given area for a specific period of time. The formula for calculating this coefficient is very simple:
where O is the amount of precipitation (in millimeters);
and And is the amount of evaporation (also in millimeters).
Different approaches to determining the coefficient
How to determine the moisture coefficient? Today, about 20 different methods are known.
In our country (as well as in the post-Soviet space), the determination method proposed by Georgy Nikolaevich Vysotsky is most often used. He is an outstanding Ukrainian scientist, geobotanist and soil scientist, the founder of forest science. During his life, he wrote over 200 scientific papers.
It is worth noting that in Europe, as well as in the USA, the Tortwaite coefficient is used. However, the method for calculating it is much more complicated and has its drawbacks.
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Determination of the coefficient
It is not at all difficult to determine this indicator for a specific territory. Let's consider this technique in the following example.
The territory for which it is necessary to calculate the moisture coefficient is given. At the same time, it is known that this territory receives 900 mm of atmospheric precipitation per year, and evaporates from it during the same period of time - 600 mm. To calculate the coefficient, divide the amount of precipitation by evaporation, that is, 900/600 mm. As a result, we get a value of 1.5. This will be the moisture coefficient for this area.
The moisture coefficient of Ivanov-Vysotsky can be equal to one, be lower or higher than 1. Moreover, if:
- K = 0, then the moisture for this area is considered sufficient;
- K is more than 1, then the moisture is excessive;
- K is less than 1, then the moisture is insufficient.
The value of this indicator, of course, will directly depend on the temperature regime in a particular territory, as well as on the amount of atmospheric precipitation falling per year.
What is the humidification factor used for?
The Ivanov-Vysotsky coefficient is an extremely important climatic indicator.
After all, he is able to give a picture of the provision of the area with water resources. This coefficient is simply necessary for the development of agriculture, as well as for the general economic planning of the territory.
It also determines the level of dryness of the climate: the larger it is, the more humid the climate. In areas with excessive moisture, there is always an abundance of lakes and wetlands. The vegetation cover is dominated by meadow and forest vegetation.
The maximum values of the coefficient are typical for high-mountainous regions (above 1000-1200 meters). Here, as a rule, there is an excess of moisture, which can reach 300-500 millimeters per year! The steppe zone receives the same amount of atmospheric moisture per year. The moisture coefficient in mountainous regions reaches its maximum values: 1.8-2.4.
Excessive moisture is also observed in the natural zone of taiga, tundra, forest-tundra, as well as temperate broad-leaved forests. In these areas, the coefficient is not more than 1.5. In the forest-steppe zone, it ranges from 0.7 to 1.0, but in the steppe zone, insufficient moisture is already observed in the territory (K = 0.3-0.6).
The minimum values of moisture are typical for the semi-desert zone (about 0.2-0.3 in total), as well as for the desert zone (up to 0.1).
Humidification coefficient in Russia
Russia is a huge country with a wide variety of climatic conditions. If we talk about the moisture coefficient, then its values within Russia fluctuate within wide limits from 0.3 to 1.5. The scantiest moisture is observed in the Caspian region (about 0.3). In the steppe and forest-steppe zones, it is slightly higher - 0.5-0.8. Maximum moisture is typical for the forest-tundra zone, as well as for the high-mountainous regions of the Caucasus, Altai, and the Ural Mountains.
Now you know what the moisture coefficient is. This is a fairly important indicator that plays a very important role for the development of the national economy and the agro-industrial complex. This coefficient depends on two values: on the amount of precipitation and on the volume of evaporation over a certain period of time.
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HUMIDIFICATION COEFFICIENT
| www.asyan.org | 1 2 3 Group work
Mixed and deciduous forests, forest-steppe
Steppes, semi-deserts and deserts
|
Using the text of the tutorial, fill in the table
Working in pairs
Exercise 1
- determine the change in temperature, precipitation, evaporation in Western Siberia from west to east.
- What is the reason for the increase in precipitation in the eastern part?
Assignment 2
- Determine the change in temperature, precipitation and evaporation in Western Siberia from north to south.
- In which part of the plain is excessive moisture?
- Geographical position
- Relief
- Minerals
- Climate (average temperatures in January, July, annual precipitation, humidification)
- Water - rivers, lakes, permafrost
- Natural area
- Population activities (hunting, fishing, mining ...)
- Problems and solutions
Mark the following objects on the map:
Altai, Western Sayan, Eastern Sayan, Salair ridge, Kuznetsk Alatau, Baikal, Khoma-Daban, Borshchovochny ridge, Stanovoy, Yablonovy.
Highlands: Patomskoe, Aldan
Summits: Belukha
Depressions: Kuznetskaya, Minusinskaya, Tuvinskaya.
Fill the table
Describe PTC
- Karelia
- Yamal Peninsula
- Altai
- Volga Upland
- Northern Ural
- Taimyr Peninsula
- Sakhalin island
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| 1 | Geographical position (which region of Russia belongs to, the position on the territory of the region) | 5 |
| 2 | Geological structure and relief (age of the territory, nature of the earth's crust, mountainous or flat relief) Prevailing height and highest height. The influence of external processes on the formation of the relief (glacier, water erosion, anthropogenic influence ...) |
5 |
| 3 | Minerals (why exactly like that) | 5 |
| 4 | Climatic (zone, type of climate, average January and July temperatures, precipitation, winds, special phenomena) | 5 |
| 5 | Waters (rivers, lakes, swamps, permafrost, groundwater). Features of rivers - pool, ocean, food, regime) | 4 |
| 6 | Natural areas, their use protection | 4 |
| 7 | Soil | 4 |
| 8 | Plants and Animals | 3 |
| 9 | Environmental problems of the territory | 5 |
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What is moisture coefficient and how to calculate it
Humidification coefficient is an indicator used to determine climate parameters. It can be calculated by having information about precipitation in the region over a sufficiently long period.
Humidification coefficient
Humidity coefficient is a special indicator developed by experts in the field of meteorology to assess the degree of climate humidity in a particular region. At the same time, it was taken into account that the climate is a long-term characteristic of weather conditions in a given area. Therefore, it was decided to consider the humidity coefficient in a long time frame: as a rule, this coefficient is calculated on the basis of data collected during the year. Thus, the humidity coefficient shows how much precipitation falls during this period in the region under consideration. This, in turn, is one of the main factors determining the prevailing type of vegetation in this area.
Calculation of the moisture coefficient
The formula for calculating the moisture coefficient is as follows: K = R / E. In this formula, the symbol K denotes the actual moisture coefficient, and the symbol R - the amount of precipitation that fell in a given area during the year, expressed in millimeters. Finally, the E symbol represents the amount of precipitation that has evaporated from the surface of the earth during the same period of time. The specified amount of precipitation, which is also expressed in millimeters, depends on the type of soil, the temperature in the region at a particular time, and other factors. Therefore, despite the seeming simplicity of the above formula, the calculation of the moisture coefficient requires a large number of preliminary measurements using precise instruments and can only be carried out by a sufficiently large team of meteorologists. , allows to determine with a high degree of certainty what type of vegetation is predominant in this region.
Humidification coefficient
So, if the moisture coefficient exceeds 1, this indicates a high level of moisture in this area, which entails the predominance of such types of vegetation as taiga, tundra or forest-tundra. Adequate moisture level corresponds to a moisture coefficient of 1, and, as a rule, is characterized by a predominance of mixed or deciduous forests. Moisture coefficient in the range from 0.6 to 1 is typical for forest-steppe areas, from 0.3 to 0.6 - for steppes, from 0.1 to 0.3 - for semi-desert territories, and from 0 to 0.1 - for deserts ...
Humidification coefficient
Moisture coefficient is the ratio of the average annual precipitation to the average annual evaporation. Evaporation is the amount of moisture that can evaporate from a certain surface. Both precipitation and volatility are measured in millimeters. You can find out the volatility experimentally - set up a wide open container with water and constantly note how much water evaporates over a period of time. So during the whole frost-free period. In fact, evaporation also occurs from the surface of the snow. There are methods for calculating it, they are studied by the science of ice - glaciology.
Moisture coefficient, abbreviated to K wet, is an important geographical indicator. If there is more precipitation than moisture can evaporate (K sw.> 1), then excess water accumulates on the surface of the earth and waterlogging will occur in the depressions. This happens, for example, in natural areas such as tundra and taiga. If the amount of precipitation is equal to the evaporation rate (K vl. = 1), then theoretically all the precipitation that has fallen out can evaporate. These are the best conditions for plants - there is enough moisture, but there is no stagnation. This is typical for the zone of mixed (coniferous-deciduous) forests. If the precipitation falls less than evaporation (K uvl.< 1), значит в году будут сезоны, более или менее продолжительные, когда влаги хватать не будет. Для растений это не очень хорошо. На территории России такие условия характерны для природных зон, находящихся южнее смешанных лесов — лесостепи, степи и полупустыни.
The amount of precipitation does not yet give a complete picture of the provision of the territory with moisture, since part of it evaporates from the surface, and the other part seeps into.
At different temperatures, different amounts of moisture evaporate from the surface. The amount of moisture that can evaporate from a water surface at a given temperature is called volatility. It is measured in millimeters of the evaporated water layer. Evaporation characterizes possible evaporation. The actual evaporation cannot be more than the annual precipitation. Therefore, in Central Asia it is no more than 150-200 mm per year, although the evaporation rate here is 6-12 times higher. To the north, evaporation increases, reaching 450 mm in the southern part and 500-550 mm in the Russian. Further north of this strip, evaporation again decreases to 100–150 mm in coastal areas. In the northern part of the country, evaporation is not limited by the amount of precipitation, as in the deserts, but by the amount of evaporation.
To characterize the provision of the territory with moisture, the moisture coefficient is used - the ratio of the annual precipitation to evaporation for the same period: k = O / U
The lower the moisture coefficient, the drier.
Near the northern border, the amount of precipitation is approximately equal to the annual evaporation rate. The moisture coefficient here is close to unity. This moisture is considered sufficient. Humidification of the forest-steppe zone and the southern part of the zone fluctuates from year to year in the direction of either increasing or decreasing, therefore it is unstable. If the humidification coefficient is less than one, the humidification is considered insufficient (zone). In the northern part of the country (taiga, tundra), the amount of precipitation exceeds evaporation. The humidification coefficient is greater than one here. This is called excessive moisture.
The relationship between precipitation and volatility (or temperature, since volatility depends on the latter). With excessive moisture, precipitation exceeds evaporation and part of the precipitated water is removed from the area by underground and river runoff. With insufficient moisture, precipitation falls less than it can evaporate. [...]
Moisture coefficient in the southern part of the zone is 0.25-0.30, in the central - 0.30-0.35, in the northern - 0.35-0.45. In the driest years, in the summer months, the relative humidity of the air drops sharply. Dry winds are frequent, which have a detrimental effect on the development of vegetation. [...]
HUMIDIFICATION COEFFICIENT - the ratio of the annual amount of precipitation to the possible annual evaporation (from the open surface of fresh water): K = I / E, where I is the annual amount of precipitation, E is the possible annual evaporation. Expressed in%. [...]
The boundaries between the moistening rows are outlined by the values of the Vysotsky moistening coefficient. So, for example, the hydrolayer O is a series of balanced moisture. Rows SB and B are limited by humidification coefficients 0.60 and 0.99. The moisture coefficient of the steppe zone is in the range of 0.5-1.0. Accordingly, the area of chernozem-steppe soils is located in the CO and O. [...]
In the eastern regions, precipitation is even less - 200-300 mm. Humidification coefficient in different parts of the zone from south to north ranges from 0.25 to 0.45. The water regime is non-flush. [...]
The ratio of the annual precipitation to the annual evaporation is called the moisture coefficient (KU). In different natural zones, KU ranges from 3 to OD. [...]
The modulus of elasticity of dry slabs is on average 3650 MPa. Taking humidification coefficients 0.7 and operating conditions 0.9, we get B = 0.9-0.7-3650 = 2300 MPa. [...]
Of the agroclimatic indicators, the most closely related to yield are the sum of temperatures> 10 ° C, the moisture coefficient (according to Vysotsky-Ivanov), in some cases, the hydrothermal coefficient (according to Selyaninov), the degree of continental climate. [...]
The evaporation rate in the landscapes of dry and desert steppe significantly exceeds the amount of atmospheric precipitation, the moisture coefficient is about 0.33-0.5. Strong winds dry up the soil even more and cause vigorous erosion. [...]
Possessing relative radiation-thermal homogeneity, the type of climate - and, accordingly, the climatic zone - according to the conditions of humidification, is subdivided into subtypes: wet, dry, semi-dry. In the wet subtype, the moisture coefficient of Dokuchaev-Vysotsky is greater than 1 (precipitation is greater than evaporation), in the semi-dry subtype, from 1 to 0.5, in the dry subtype, less than 0.5. The areas of subtypes form climatic zones in the latitudinal direction, and climatic zones in the meridional direction. [...]
Of the characteristics of the water regime, the most important are the average annual precipitation, its fluctuation, seasonal distribution, moisture coefficient or hydrothermal coefficient, the presence of dry periods, their duration and frequency, recurrence, depth, time of establishment and destruction of snow cover, seasonal dynamics of air humidity, presence dry winds, dust storms and other beneficial natural phenomena. [...]
The climate is characterized by a set of indicators, but only a few are used to understand the processes of soil formation in soil science: the annual amount of precipitation, the coefficient of soil moisture, the average annual air temperature, the average long-term temperatures of January and July, the sum of the average daily air temperatures for the period with temperatures above 10 ° С, the duration of this period, the length of the growing season. [...]
The degree of supply of the area with moisture necessary for the development of vegetation, natural and cultural. It is characterized by the ratio between precipitation and evaporation (N. N. Ivanov's moisture coefficient) or between precipitation and the radiation balance of the earth's surface (M. I. Budyko's dryness index), or between precipitation and temperature sums (G. T. Selyaninov's hydrothermal coefficient) . [...]
When compiling the table, I.I. Karmanov found correlations of yield with soil properties and with three agroclimatic indicators (sums of temperatures for the growing season, moisture coefficient according to Vysotsky - Ivanov and coefficient of continentalism) and constructed empirical formulas for calculations. Since the bonitet points for low and high levels of farming were calculated according to independent hundred-point systems, the concept of the yield point price (in kg / ha), which was used earlier, was introduced. Table 113 shows the change in the degree of increase in yield during the transition from a low intensity of agriculture to a high one for the main types of soils of the agricultural belt of the USSR and for the five main provincial sectors. [...]
The completeness of using the incoming solar energy for soil formation is determined by the ratio of the total energy consumption for soil formation to the radiation balance. This ratio depends on the degree of moisture. In arid conditions, with low values of the moisture coefficient, the degree of use of solar energy for soil formation is very low. In well-moistened landscapes, the degree of use of solar energy for soil formation increases sharply, reaching 70-80%. As follows from Fig. 41, with an increase in the moisture coefficient, the use of solar energy increases, however, with a moisture coefficient of more than two, the fullness of energy use increases much more slowly than the moisture content of the landscape increases. The completeness of the use of solar energy in soil formation does not reach unity. [...]
To create optimal conditions for the growth and development of cultivated plants, it is necessary to strive to equalize the amount of moisture entering the soil with its consumption for transpiration and physical evaporation, that is, creating a moisture coefficient close to unity. [...]
Each zonal ecological group is characterized by the type of vegetation (taiga-forest, forest-steppe, steppe, etc.), the sum of soil temperatures at a depth of 20 cm from the surface, the duration of soil freezing at the same depth in months and the moisture coefficient. [... ]
Heat and water balances play a decisive role in the formation of landscape biota. The partial solution gives the moisture balance - the difference between precipitation and evaporation over a given period of time. Both precipitation and volatility are measured in millimeters, but the second value here represents the heat balance, since the potential (maximum) evaporation in a given location depends primarily on thermal conditions. In forest zones and tundra, the moisture balance is positive (precipitation exceeds evaporation), in steppes and deserts - negative (precipitation is less than evaporation). In the north of the forest-steppe, the moisture balance is close to neutral. The moisture balance can be converted into a moisture coefficient, which means the ratio of atmospheric precipitation to the amount of evaporation for a known period of time. To the north of the forest-steppe, the moisture coefficient is above unity, to the south - less than unity. [...]
To the south of the northern taiga, there is enough heat everywhere for the formation of a powerful biostrome, but here another controlling factor of its development comes into force - the ratio of heat and moisture. The biostrome reaches its maximum development with forest landscapes in places where the ratio of heat and moisture is optimal, where the Vysotsky-Ivanov moisture coefficient and the radiation dryness index of MI Budyko are close to unity. [...]
The differences are due to the geographic and climatic irregularities in precipitation. There are places on the planet where not a drop of moisture falls (Aswan region), and places where it rains almost incessantly, giving a huge annual rainfall - up to 12,500 mm (Cherrapunji region in India). 60% of the world's population lives in areas with a moisture coefficient of less than unity. [...]
The main indicators characterizing the influence of climate on soil formation are the average annual temperatures of air and soil, the sum of active temperatures is more than 0; 5; 10 ° С, the annual amplitude of soil and air temperature fluctuations, the duration of the frost-free period, the value of the radiation balance, the amount of precipitation (average monthly, average annual, for the warm and cold periods), the degree of continental, evaporation, moisture coefficient, radiation index of dryness, etc. indicators, there are a number of parameters characterizing precipitation and wind speed, which determine the manifestation of water and wind erosion. [...]
In recent years, a soil-ecological assessment has been developed and widely used (Shishov, Durmanov, Karmanov et al., 1991). The methodology allows to determine soil-ecological indicators and points of soil bonitet of different lands, at any level - a specific site, region, zone, country as a whole. For this purpose, the following are calculated: soil indices (taking into account washout, deflation, gravel, etc.), average humus content, agrochemical indicators (coefficients for the content of nutrients, soil acidity, etc.), climatic indicators (sum of temperatures, moisture coefficients, etc. .). The final indicators (soil, agrochemical, climatic) and, in general, the final soil-ecological index are also calculated. [...]
In practice, the nature of the water regime is determined by the ratio between the amount of precipitation according to the average long-term data and the evaporation rate for the year. Evaporation is the largest amount of moisture that can evaporate from an open water surface or from the surface of permanently waterlogged soil in a given climatic conditions for a certain period of time, expressed in mm. The ratio of the annual precipitation to the annual evaporation rate is called the moisture coefficient (CA). In various natural zones, KU ranges from 3 to 0.1.