The maximum moisture coefficient is typical for. Moisture coefficient. Moisture coefficient calculation

It is easy to see that two oppositely directed processes are constantly taking place on the earth's surface - irrigation of the area by precipitation and drying it out by evaporation. Both of these processes merge into a single and contradictory process of atmospheric humidification, which is understood as the ratio of precipitation and evaporation.
There are over twenty ways to express it. The indicators are called indices and coefficients of either air dryness or atmospheric moisture. The most famous are the following:

1. Hydrothermal coefficient G. T. Selyaninova.
2. Radiation index of dryness M. I. Budyko.
3. Moisture coefficient of G. N. Vysotsky - N. N. Ivanov. It is best to express it in %. For example, in the European tundra, precipitation is 300 mm, and evaporation is only 200 mm, therefore, precipitation exceeds evaporation by 1.5 times, atmospheric humidification is 150%, or \u003d 1.5. Humidification is excessive, more than 100%, or / 01.0, when more precipitation falls than can evaporate; sufficient, at which the amount of precipitation and evaporation are approximately equal (about 100%), or C = 1.0; insufficient, less than 100%. or to<1,0, если испаряемость превосходит количество осадков; в последней градации полезно выделить ничтожное увлажнение, в котором осадки составляют ничтожную (13% и меньше, или К = 0,13) долю испаряемости.
4. In Europe and the USA, C. W. Tortveit's coefficient is used, which is rather complex and highly inaccurate; it is not necessary to consider it here. The abundance of ways to express air humidification suggests that none of them can be considered not only accurate, but also more true than others. N. N. Ivanov's formula for evapotranspiration and moistening coefficient are quite widely used, and for the purposes of geography it is the most expressive.

Moisture coefficient - the ratio between the amount of precipitation for a year or other time and the evaporation of a certain area. Humidity coefficient is an indicator of the ratio of heat and moisture.

The amount of precipitation does not yet give a complete picture of the moisture supply of the territory, since part of the atmospheric precipitation evaporates from the surface, and the other part seeps into the soil.
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 the volatility. It is measured in millimeters of the evaporated water layer. Evaporation characterizes the possible evaporation. The actual evaporation cannot be more than the annual amount of precipitation. Therefore, in the deserts of Central Asia, it is no more than 150-200 mm per year, although evaporation here is 6-12 times higher. To the north, evaporation increases, reaching 450 mm in the southern part of the taiga of Western Siberia and 500-550 mm in mixed and broad-leaved forests of the Russian Plain. Further north of this strip, evaporation again decreases to 100-150 mm in the coastal tundra. In the northern part of the country, evaporation is limited not by the amount of precipitation, as in deserts, but by the amount of evaporation.
To characterize the moisture content of the territory, the moisture coefficient is used - the ratio of the annual precipitation to the evaporation rate for the same period.
The lower the humidity coefficient, the drier the climate. Near the northern border of the forest-steppe zone, the amount of precipitation is approximately equal to the annual evaporation. The moisture coefficient here is close to unity. Such moisture is considered sufficient. Humidification of the forest-steppe zone and the southern part of the mixed forest zone fluctuates from year to year in the direction of increasing or decreasing, therefore it is unstable. When the moisture coefficient is less than one, moisture is considered insufficient (steppe zone). In the northern part of the country (taiga, tundra), the amount of precipitation exceeds evaporation. The moisture coefficient here is greater than unity. Such moisture is called excessive.
The moisture coefficient expresses the ratio of heat and moisture in a particular area and is one of the important climatic indicators, as it determines the direction and intensity of most natural processes.
In areas of excessive moisture, there are many rivers, lakes, swamps. Erosion dominates in the transformation of the relief. Meadows and forests are widespread.

High annual values ​​of the moisture coefficient (1.75-2.4) are typical for mountain areas with absolute surface elevations of 800-1200 m. 500 mm per year or more. The minimum values ​​of the moisture coefficient from 0.35 to 0.6 are characteristic of the steppe zone, the vast majority of the surface of which is located at elevations of less than 600 m abs. height. The moisture balance here is negative and is characterized by a deficit of 200 to 450 mm or more, and the territory as a whole is characterized by insufficient moisture, typical of a semi-arid and even arid climate. The main period of moisture evaporation lasts from March to October, and its maximum intensity falls on the hottest months (June - August). The lowest values ​​of the moisture coefficient are observed in these months. It is easy to see that the amount of excess moisture in mountainous areas is comparable, and in some cases exceeds the total amount of precipitation in the steppe zone. 

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 just determine the moisture coefficient for a particular area. What is moisture content and how is it determined? That is what this informative article will be about.

Moisture Coefficient: Definition

Humidification of the territory and evaporation of moisture from its surface all over the world occur in exactly the same way. However, the answer to the question of what is the coefficient of moisture in different countries of the planet is answered in completely different ways. And the very concept in this formulation is not accepted in all countries. For example, in the USA it is "precipitation-evaporation ratio", which can be literally translated as "index (ratio) of moisture and evaporation".

But still, what is the coefficient of moisture? 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 I - the value of evaporation (also in millimeters).

Different approaches to determining the coefficient

How to determine the moisture content? Today, about 20 different methods are known.

In our country (as well as in the post-Soviet space), the method of determination proposed by Georgy Nikolaevich Vysotsky is most often used. This 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 United States, the Torthwaite coefficient is used. However, the method of its calculation is much more complicated and has its drawbacks.

Coefficient definition

It is not at all difficult to determine this indicator for a particular area. Let's consider this technique in the following example.

Given the area for which you need to calculate the coefficient of moisture. At the same time, it is known that this territory receives 900 mm per year and evaporates from it over the same period of time - 600 mm. To calculate the coefficient, you should divide the amount of precipitation by evaporation, that is, 900/600 mm. As a result, we will get a value of 1.5. This will be the moisture coefficient for this area.

The Ivanov-Vysotsky humidification coefficient can be equal to one, be lower or higher than 1. Moreover, if:

• K = 0, then humidification for the given territory is considered sufficient;
• To more than 1, then the moisture is excessive;
• To less than 1, then moisture is insufficient.

The value of this indicator, of course, will directly depend on the temperature regime in a particular area, as well as on the amount of precipitation falling during the year.

What is the moisture 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 greater it is, the more humid. 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 mountain 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 tundra, forest-tundra, and temperate. 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 moistening of the territory is already observed (K = 0.3-0.6).

The minimum moisture values ​​are typical for the semi-desert zone (about 0.2-0.3 in total), as well as for (up to 0.1).

Moisture coefficient in Russia

Russia is a huge country, which is characterized by a wide variety of climatic conditions. If we talk about the moisture coefficient, then its values ​​within Russia vary widely from 0.3 to 1.5. The poorest moisture is observed in the Caspian Sea (about 0.3). In the steppe and forest-steppe zone, it is somewhat higher - 0.5-0.8. Maximum moisture is typical for the forest-tundra zone, as well as for the high-mountain regions of the Caucasus, Altai, and the Ural Mountains.

Now you know what the moisture coefficient is. This is a rather important indicator, which 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.

Fuel volatility determines the efficiency of mixture formation and combustion processes in engines, the magnitude of losses during storage and transportation, the possibility of vapor locks in the engine power system, fire and explosion hazard of petroleum products. The rate of fuel evaporation depends on its properties and process conditions. The volatility of fuel characterizes the saturated vapor pressure, diffusion coefficient, heat of vaporization, heat capacity and thermal conductivity.

Determination of saturation vapor pressure

The main indicator of the volatility of a hydrocarbon fuel is the saturated vapor pressure (DAYs) or vapor pressure - this is the pressure that vapor exerts on the vessel walls when the fuel evaporates in a confined space. It characterizes the volatility of gasoline fractions and the starting qualities of the fuel. DNP depends on the chemical and fractional composition of the fuel. As a rule, the more low-boiling hydrocarbons in the fuel, the higher the vapor pressure. DNP also increases with increasing temperature. The use of fuel with high vapor pressure leads to an increased formation of vapor locks in the power system, a decrease in cylinder filling, and a drop in power. In summer grades of gasoline, DNP should not exceed 80 kPa.

Winter grades of gasoline to facilitate starting the engine in the cold season have a higher pressure of 80-100 kPa. In addition, DNP characterizes the physical stability of gasoline.

Saturated vapor pressure of a fuel is determined in various ways: in a metal vessel, using a barometric tube, by comparison with the pressure of a reference liquid, and by a number of other methods.

This indicator is determined by directly measuring the pressure above the liquid at a certain temperature or by the boiling point at a given pressure. In the first case, an equilibrium between vapor and liquid is established in the vessel, which is fixed by the value of the equilibrium pressure with an appropriate device for measuring pressure. In the second case, the set volume of fuel is distilled at atmospheric pressure and the dependence between the amount of distilled product and temperature is fixed, i.e. determine the fractional composition. Saturated vapor pressure can also be determined, in particular, both by the barometric tube method and by the comparative method. Vapor pressure is often determined (GOST 1756-83) by holding the test gasoline for 20 minutes in a sealed container at 38 °C. After a predetermined time, the vapor pressure of the fuel is measured.

When determining the DNP in a metal device, the readings of the pressure measuring device must be corrected, since these readings correspond to the total pressure of saturated vapors of fuel, air and water vapor at the test temperature. Measurements in a barometric tube give values ​​of the true DNP of the fuel, since in this device an equilibrium is established between the liquid and vapor phases containing only fuel vapors. The advantages of the comparative method are its low sensitivity to temperature fluctuations during the measurement process.

Determination of saturated vapor pressure in a metal bomb. The device (Fig. 27.1) consists of a metal bomb 1, water bath 2 and mercury manometer 8. A cylindrical bomb has two chambers: for fuel 10 and larger air. A rubber gasket is placed between the chambers, and they are connected using a threaded connection. The air chamber has a fitting, which is a rubber tube 6 through the gas valve 5 connected to a mercury manometer. The water bath is used to create and maintain a standard temperature; it has an electric heater 1, stirrer 7 and thermometer 4.

To obtain accurate results when determining vapor pressure, it is very important to correctly sample and store the fuel under test so that the loss of light fractions is minimal. A special sampler is used for sampling. 9, which after filling is stored in an ice bath or in a refrigerator.

Rice. 27.1.

• 1 - metal bomb; 2 - water bath; 3 - electric heater;
• 4- thermometer; 5 - gas valve; 6 - rubber tube; 7 - mixer;
• 8 - mercury manometer; 9 - sampler;10 - fuel chamber

Determination of saturated vapor pressure by the barometric tube method. The device consists of a U-tube 1, thermostatic vessel 2, agitators 3, thermometer 4, mercury manometer 8, buffer tank 5 and a vacuum pump (Fig. 27.2). A tee with a three-way valve 7 is installed on the neck of the buffer tank. By switching the three-way valve, you can connect the vacuum pump to the buffer tank, U-tube and mercury pressure gauge or connect it to the atmosphere. All parts of the device are interconnected by rubber tubes. 6.

Rice. 27.2.

• 1- U-shaped tube; 2 - thermostatic vessel; 3 - mixer;4 - thermometer; 5 - buffer capacity; 6 - rubber tubes;
• 7 - three-way valve;8 - mercury manometer

Fill the U-tube with the fuel under test so that it completely fills the elbow with the capillary to the middle of the tube bend. The filled tube is immersed in a thermostatic vessel, connected with a rubber tube to a buffer vessel, and kept at the test temperature. For a short time, the buffer tank is connected to the atmosphere, the vacuum pump is turned on. Under the action of vacuum and vapor pressure of the fuel, the liquid descends in the capillary and rises in the knee with expansion. At the moment of equalization of the levels in both knees of the tube, the readings of the mercury manometer are recorded.

Saturated vapor pressure of fuel ps in Pa is calculated by the formula:

Where r b- barometric pressure, mm Hg. Art.; p and- readings of a mercury manometer, mm Hg. Art.

Determination of the pressure of saturated vapors of fuel by a comparative method. A device for measuring saturated vapor pressure and determining its dependence on temperature by comparison with standards (Fig. 27.3) consists of two flasks 3, thermostatic device 1 and mercury U-shaped manometer 8.

Rice. 27.3.

• 1- thermostatic device;2 - stirrer;3 - conical flask;
• 4- passing crane; 5 - heater; 6 - thermometer;
• 7 - rubber tubes;8 - U-gauge

Glass flasks are closed with ground stoppers with taps 4, which are connected to the pressure gauge with the help of rubber tubes 7.

The thermostatic device is a glass cylindrical vessel filled with water, in which flasks, a stirrer 2, a heater 5 and a thermometer are placed. 6.

A sampler is used to take and store a fuel sample. The test fuel is poured into one of the flasks, the same amount of reference liquid is placed in the other flask - benzene or isooctane for gasoline. The flasks are tightly closed with stoppers with taps, placed in a thermostat with a given temperature and incubated for 5 minutes.

Subsequently, the water is heated in a thermostat and the pressure drop on the pressure gauge is recorded at specified temperature intervals. The value of the saturation vapor pressure of the fuel is calculated as the algebraic sum of the saturation vapor pressure of the reference liquid at a given temperature and the pressure gauge readings. The value of the saturation vapor pressure of reference liquids is given in the reference literature. For benzene, this dependence is shown in Fig. 27.4.

Rice. 27.4.

According to the obtained dependence p s = f(T) build a graph in Ig coordinates ps And /T and determine the values ​​of the coefficients in the empirical formula:

Where L - segment cut off on the y-axis (provided T= 0); IN - tangent of the angle of inclination of a straight line to the abscissa axis.

The relationship between the amount of precipitation and evaporation (or temperature, since evaporation depends on the latter). With excessive moisture, precipitation exceeds evaporation and part of the fallen water is removed from the area by underground and river runoff. With insufficient moisture, precipitation falls less than it can evaporate.[ ...]

Humidity coefficient in the southern part of the zone is 0.25-0.30, in the central part - 0.30-0.35, in the northern part - 0.35-0.45. In the driest years in the summer months, the relative humidity of the air drops sharply. Dry winds are frequent, having 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 waters): K \u003d R / E, where R is the annual amount of precipitation, E is the possible annual evaporation. Expressed in %.[ ...]

The boundaries between the moisture series are marked by the values ​​of the Vysotsky moisture coefficient. So, for example, the hydroseries O is a series of balanced moisture. Rows SB and B are limited by moisture coefficients of 0.60 and 0.99. The moisture coefficient of the steppe zone is in the range of 0.5-1.0. Accordingly, the range of chernozem-steppe soils is located in the hydroseries of CO and O.[ ...]

In the eastern regions of precipitation is even less - 200-300 mm. The moisture coefficient in different parts of the zone from south to north ranges from 0.25 to 0.45. The water regime is non-flushing.[ ...]

The ratio of the annual precipitation to the annual evaporation is called the moisture coefficient (KU). In different natural zones, the KU ranges from 3 to OD.[ ...]

The modulus of elasticity of dry-method boards is 3650 MPa on average. Assuming moisture coefficients of 0.7 and operating conditions of 0.9, we get B = 0.9-0.7-3650 = 2300 MPa.[ ...]

Of the agro-climatic indicators, the most closely related to productivity are the sum of temperatures > 10 ° С, the moisture coefficient (according to Vysotsky-Ivanov), in some cases the hydrothermal coefficient (according to Selyaninov), the degree of continental climate.[ ...]

Evaporation in the landscapes of the dry and desert steppe significantly exceeds the amount of precipitation, the moisture coefficient is about 0.33-0.5. strong winds further dry out the soil and cause vigorous erosion.[ ...]

Possessing relative radiation-thermal homogeneity, the type of climate - and, accordingly, the climatic zone - is divided into subtypes according to the conditions of moisture: humid, dry, semi-dry. In the humid subtype, the Dokuchaev-Vysotsky moistening coefficient is greater than 1 (precipitation is greater than evaporation), in the semi-dry - from 1 to 0.5, in the dry - less than 0.5. The ranges of subtypes form climatic zones in the latitudinal direction, climatic regions in the meridional direction.[ ...]

Of the characteristics of the water regime, the most important are the average annual precipitation, their fluctuation, seasonal distribution, moisture coefficient or hydrothermal coefficient, the presence of dry periods, their duration and frequency, frequency, depth, the time of establishment and destruction of snow cover, seasonal dynamics of air humidity, the presence dry winds, dust storms and other favorable 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: annual precipitation, soil moisture coefficient, average annual air temperature, average long-term temperatures in January and July, the sum of average daily air temperatures for a period with temperatures above 10 ° C, 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 (humidity coefficient of N. N. Ivanov) or between precipitation and the radiation balance of the earth's surface (dryness index of M. I. Budyko), or between precipitation and sums of temperatures (hydrothermal coefficient of G. T. Selyaninov) .[ ...]

When compiling the table, I. I. Karmanov found correlations between yields and soil properties and with three agro-climatic indicators (the sum of temperatures for the growing season, the moisture coefficient according to Vysotsky-Ivanov and the coefficient of continentality) and built empirical formulas for calculations. Since the bonitet scores for low and high levels of farming were calculated according to independent hundred-point systems, the previously used concept of the yield price of a point (in kg/ha) was introduced. Table 113 shows the change in the degree of growth in yields during the transition from low to high intensity of agriculture for the main types of soils in the agricultural zone of the USSR and for the five main provincial sectors.[ ...]

The completeness of the use of the incoming solar energy on 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. Under arid conditions, with small values ​​of the moisture coefficient, the degree of use of solar energy for soil formation is very small. 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 completeness of energy use increases much more slowly than the increase in landscape moisture. The completeness of the use of solar energy in soil formation does not reach one.[ ...]

To create optimal conditions for growth and development 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, to create 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.[ ... ]

Thermal and water balances play a decisive role in the formation of landscape biota. A partial solution gives the moisture balance - the difference between precipitation and evaporation over a certain period of time. Both precipitation and evaporation are measured in millimeters, but the second value here represents the heat balance, since the potential (maximum) evaporation in a given place depends primarily on thermal conditions. In forest zones and tundra, the moisture balance is positive (precipitation exceeds evaporation), in steppes and deserts it is 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 over a known period of time. To the north of the forest-steppe, the moisture coefficient is higher than one, to the south it is less than one.[ ...]

To the south of the northern taiga, there is enough heat everywhere to form a powerful biostrome, but here another controlling factor of its development comes into force - the ratio of heat and moisture. His maximum development with forest landscapes, the biostrome reaches an optimal ratio of heat and moisture in places where the Vysotsky-Ivanov moisture coefficient and M. I. Budyko's radiation index of dryness are close to unity.[ ...]

The differences are due to the geographical and climatic unevenness of precipitation. There are places on the planet where not a drop of moisture falls (the Aswan region), and places where it rains almost incessantly, giving a huge annual rainfall - up to 12,500 mm (the Cherrapunji region in India). 60% of the world's population lives in areas with a moisture coefficient less than one.[ ...]

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, annual amplitude of fluctuations in soil and air temperature, frost-free period, radiation balance, precipitation (monthly average, annual average, for warm and cold periods), degree of continentality, evaporation, moisture coefficient, dryness radiation index, etc. In addition to those listed indicators, there are a number of parameters characterizing precipitation and wind speed, which determine the manifestation of water and wind erosion.[ ...]

IN last years a soil-ecological assessment has been developed and is widely used (Shishov, Durmanov, Karmanov et al., 1991). The technique makes it possible to determine the soil-ecological indicators and soil quality ratings 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, rubble, etc.), average humus content, agrochemical indicators(coefficients for the content of nutrients, soil acidity, etc.), climatic indicators (sum of temperatures, moisture coefficients, etc.). They also calculate the final indicators (soil, agrochemical, climatic) and, in general, the final soil-ecological index.[ ...]

In practice, the nature of the water regime is determined by the ratio between the amount of precipitation according to average long-term data and evaporation per year. Evaporation is the maximum amount of moisture that can be evaporated from an open water surface or from the surface of a permanently waterlogged soil in the data. climatic conditions for a certain period of time, expressed in mm. The ratio of the annual precipitation to the annual evaporation is called the moisture coefficient (KU). In various natural zones, CU ranges from 3 to 0.1.

Exercise 1.

Calculate the moisture coefficient for the points indicated in the table, determine in which natural zones they are located and what kind of moisture is typical for them.

The moisture coefficient is determined by the formula:

K - moisture coefficient in the form of a fraction or in%; P is the amount of precipitation in mm; Em - volatility in mm. According to N.N. Ivanov, the moisture coefficient for the forest zone is 1.0-1.5; forest-steppe 0.6 - 1.0; steppes 0.3 - 0.6; semi-deserts 0.1 - 0.3; desert less than 0.1.

Moisture characteristics by natural zones

For an approximate assessment of moisture conditions, a scale is used: 2.0 - excessive moisture, 1.0-2.0 - satisfactory moisture, 1.0-0.5 - arid, insufficient moisture, 0.5 - dry

For 1 item:

K = 520/610 K = 0.85

Arid, insufficient moisture, natural zone - forest-steppe.

For 2 items:

K = 110/1340 K = 0.082

Dry, insufficient moisture, natural zone - desert.

For 3 items:

K = 450/820 K = 0.54

Arid, insufficient moisture, natural zone - steppe.

For 4 items:

K = 220/1100 K = 0.2

Dry, insufficient moisture, natural zone - semi-desert.

Task 2.

Calculate the moisture coefficient for the Vologda Oblast, if the average annual precipitation is 700 mm, evaporation is 450 mm. Make a conclusion about the nature of moisture in the area. Consider how moisture will change in various conditions hilly terrain.

Moisture coefficient (according to N. N. Ivanov) is determined by the formula:

where, K - moisture coefficient in the form of a fraction or in%; P is the amount of precipitation in mm; Em - volatility in mm.

K = 700/450 K = 1.55

Conclusion: In the Vologda region, located in the natural zone - taiga, moisture is excessive, because. moisture factor is greater than 1.

Humidification in different conditions of a hilly terrain will change, it depends on: the geographical latitude of the area, the area occupied, the proximity of the ocean, the height of the relief, the moisture coefficient, the underlying surface, and the exposure of the slopes.

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