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4. Демидась Г. I. Показники органогенезу i продуктивтсть люцерни поавно! залежно вiд строку ciвби та покривно! культури / Г. I. Демидась. Р. Т. [вановська. В. П. Коваленко, Л. В. Малинка // Корми i кормовиробництво. - Вшниця: 2010. - Вип. 66. - С. 183—188.
5. Виробнича економжа/ За ред. В.П. Галушко. Г. Штрьобеля. Навчальний поибник. - Вiнниця: Нова книга. 2005. - 400 с.
Kozybayevа Farida Esenkozhanovna.,
Dr.Sci.Biol., professor, chief researcher of the Kazakh research institute of soil science and agrochemistry
of name U. U. Uspanova, Kazakhstan, Almaty _ farida_kozybaeva@mail.ru
Beiseyeva Gulzhan Beiseyevna,
doctor of agricultural sciences, manager of department of Ecology of soils of the Kazakh research institute of soil science and agrochemistry of name U.U. Uspanova, Kazakhstan, Almaty beiseeva2009@mail.ru
Azhikina Natalia. Zheksembaevna, research associate of the Kazakh research institute of soil science and agrochemistry of name U. U. Uspanova, Kazakhstan, Almaty Murataliyev Aschat Farchatovich, junior researcher of the Kazakh research institute of soil science and agrochemistry of name U. U. Uspanova, Kazakhstan, Almaty
ASSESSING EFFECT OF ARIDITY ON SOIL TRANSFORMATION OF KAZAKHSTAN'S ARAL SEA REGION AND DEVELOPING OF SCIENTIFIC BASES FOR INCREASE OF BIOLOGICAL PRODUCTIVITY OF SOIL
Козыбаева Ф.Е., доктор биологических наук, профессор, главный научный сотрудник Казахского научно-исследовательского института почвоведения и агрохимии имени У.У. Успанова, Казахстан, Ал-маты
Бейсеева Г. Б., доктор сельскохозяйственных наук, заведующая отделом Экологии почв Казахского научно-исследовательского института почвоведения и агрохимии имени У.У. Успанова, Казахстан, Ал-маты
Ажикина Н. Ж., научный сотрудник Казахского научно-исследовательского института почвоведения и агрохимии имени У.У. Успанова, Казахстан, Алматы
Мураталиев А. Ф. ,младший научный сотрудник Казахского научно-исследовательского института почвоведения и агрохимии имени У.У. Успанова, Казахстан, Алматы
ОЦЕНИТЬ ВЛИЯНИЕ АРИДИЗАЦИИНА ТРАНСФОРМАЦИЮ ПОЧВ КАЗАХСТАНСКОГО ПРИАРАЛЬЯ И РАЗРАБОТАТЬ НАУЧНЫЕ ОСНОВЫ ПОВЫШЕНИЯ ИХ БИОЛОГИЧЕСКОЙ
ПРОДУКТИВНОСТИ
ABSTRACT
The article presents the results of the study of the eastern part of Kazakhstan's Aral Sea region soil cover transformation in terms of human aridity. Trends in the transformation of soils and the soil cover of the Syrdarya modern delta of and the dried bottom of the Aral Sea have identified on the basis of monitoring studies.
АННОТАЦИЯ
В статье представлены результаты исследования почвенного покрова обсохшего дна Аральского моря юго-восточной части Казахстанского Приаралья. В результате усыхания Аральского моря произошли большие изменения в современной дельте Сырдарьи и на обсохшем дне Аральского моря. Изучены состояние почвенного покрова современной дельты Сырдарьи и восточной части обсохшего дна Арала, тенденции изменения почв под влиянием природных и антропогенных факторов, внесены изменения контура почвенных комплексов. Выявлена антропогенная трансформация почвенного покрова в процессе аридизации.
Keywords: Aral Sea, soil transformation, land degradation, soil map.
Ключевые слова: Аральское море, трансформация почв, деградация, почвенная карта
Aral Sea drying up - is one of the most tragic moments of past century. Ecological disaster has covered Kazakhstan's region of Aral Sea, with 85 settlements with total population of 72.0 thousand. Currently, Aral Sea region has the status of ecological disaster zone; it covers an area of 59.6 million hectares. The area of agricultural land is 43.4 million hectares, including 0.6 million hectares of arable land, 42.4 million hectares pastures and 0.4 million hectares of hay-land. The overall decline of social and economic
potential, caused by Aral Sea drying up, is determined by several factors: disturbance of ecological relationships, tension of sanitary-epidemiological situation, desert advancing of vast territory of the Aral Sea region, decreased productivity of agricultural lands, and loss of soil fertility.
The development of irrigation, followed by regulation of rivers flows, increase of water intake and permanent consumption in the upper and middle flows of Syr Darya, resulted in shortage of water resources,
anthropogenous aridization and soil transformation at lower reaches of the river. The most valuable agricultural hydromorphic soils of modern Syr Darya delta were transformed the most. As a result of drying up, large areas of salt marsh were formed on the dried bottom [1].
Region of salt marshes is currently directly adjacent the dried sea bottom, deprived of natural vegetation. It is replaced by a wider strip of seashore-growing, desert crust salt marshes that overgrown by annual alkali grasses (glasswort, sea blite, etc.). For 57 years and over of sea bottom draining, perennial alkali grasses (sarzasan, halostachys, saltwort etc.) were settled on sabulous sea bottom. Plant development is slowing on heavy soils and oppressed species of alkali grass. Territories, which were exposed out of the sea more than 10-15 years ago, formed into desert landscape, soil-cover complex with takyr-like soils and salt marshes. [2]
Takyr soil crust that formed on the surface is the main preventing factor of wind removal of salt dust masses, as well as the vegetation cover (haloxylon forest, tamarisk, sarzasan, perennial alkali grasses).
1. Subject of research and methodology.
The research object is the soil landscape of the dried sea bottom of Aral Sea southeastern part of Kazakhstan region. To assess the current state of agricultural lands and restore transformed soils of Eastern Aral Sea region and further prediction of their changes, following methods were used: cartographic method, comparative geographical method, experimental field studies.
Laboratory and analytical research method that are common in soil science and agricultural chemistry were conducted to determine physical, hydrophysical and chemical soil properties and the elements of nutrient status.
2. Results and discussion
The studies were conducted in the eastern part of the Aral Sea region within Kazaly district of Kyzylor-da region of Kazakhstan. Aral Sea dry up affected the transformation of soil formation of the dried sea border. Soil transformation defined as any form of change in morphologic-genetic characteristics and soil properties, which causing the decrease in fertility and productivity under influence of changes in soil formation factors, as a result of natural and anthropogenic desertification. Nine stages of drying and soil landscape development are allocated, which can be grouped into three stages: 1) Drying stage 1960-1975, absolute dominance of sabulous soils, slight saline. 2) Drying stage 1976-1984, dominance of desert crust salt marshes and swampy meadow dry saline soils, mostly medium loamy, granulometric composition, medium saline. 3) Drying stage 1985-1986, dominance of marshes, seashore growing and crust salt marshes, mostly of heavy granulometric composition, highly saline. Change in environmental conditions of the Aral Sea region, due to the regulation of river flow and Aral Sea dry up had significant influence on delta alluvial soils, which have reduced fertility and biological productivity. Different soil types areas calculation of the Aral Sea region as of 2008 showed that from
the total land area of 1670.5 thousand hectares, predominant soil is saline - 643.3 thousand hectares. Large areas are coastal soils - 311.1 thousand hectares, sandy - 147.6 thousand hectares, gray-brown and saline soils - 146.7 thousand hectares. An indicator of Aral Sea soil desertification is transformation alluvial-meadow saline soils in the alluvial fields of desert, areas of alluvial-meadow and alluvial-meadow riparian are significantly reduced now. Year after year, the saline soil areas has been increased, from 94.5 to 643,3 thousand hectares. Similar trend is observed with sandy soil areas, from 68,3 to 147,6 thousand hectares.
Soil transformation after cessation of rice cultivation takes place according to the following scheme: rice-marsh soils ^-meadow-swampy saline soils ^ swampy-meadow saline soils ^ secondary saline. Three main stages of development of ecological and genetic landscapes of the dried bottom of the Aral Sea and the soil formation steps in desertification process:
1. Desert landscape formation with light soil li-thology, where sandy soils are formed;
2. Landscape formation in severe soil lithology. Takyr soils are formed on heavy bottom deposits.
3. Sor-saline formation. Sor salines are formed on non-draining lagoons of various lithology.
In the condition of Aral Sea East Coast, exposed sea bottom is composed with sandy clay and loams, which are underlay with layered clays and loams that contains 0.4-1.5% of soluble sulfate-chloride and chloride-sulfate salts compositions. Coastal sea marshes are adjoin the seacoast with area width of 2-4 km, lacking of vegetation. This surface, which come out of the sea flooding 1-2 years ago, is the main source of deflation and aerosolic salty dust removal and salinity of surrounding areas. The loop length of the salt removal predominantly in West direction reaches 200-300 km, volume of annual removal - 65 million tons. Recent studies have shown that 8000 tons of salt dust is removed from 1 km2 of dried bottom. Next followed by the wide strip that was dried for 5-6 years, which were overgrown with annual saline (glasswort, sea blite etc.), with low sand dunes that decrease the wind salt dust removal. The area that was exposed more than 10-15 years ago, zonal desert landscapes with takyr soils and saline is formed. With retreat of the sea and coastal salt marshes are transformed into desert crust salt marshes or coastal hy-dromorphic saline soils after 2-3 years. Recent studies showed that in future depending on the lithology of soil, sandy soils or takyr-like soils are formed. With the increase of dried area, coastal marshes and saline soils in the total area of dried bottom of the Aral Sea is reduced.
Dried bottom landscape of the Aral Sea is diverse and it can be distinguish according to genetic properties:
1. Eolian landscape, which is formed by wind activity (sandy ripples, bushy or micro-relief of sandbars). On the sandy areas of the dried bottom, eolian landscape predominates. Very rare vegetation does not prevent deflation of sands. Sand has drawn by the wind, around barriers of bushes of sand vegetation -
y
forms piles (0.5m height) - sandy hillocks. Bushy micro-relief is being formed. Sand bars and ripples are continuously formed and vanish.
2. The erosion-accumulative relief is formed by water. Saline, which are spread as spot shape and saucer shape, are fully covered by the solid salt crust.
3. Subsidence relief. On the dried bottom, area that is bordered by state reserve Barsakelmes, on the large areas so called okpan relief occur - subsidence relief that was formed by cracks. They have crack or shape or ellipse like pits (0.3-0.5 m depth and even deeper 1.5-1.7), sometimes long holes. They can be located on large desiccated and desertificated paths. Micro-relief of biogenic origin - of animal activity (holes emissions, phitogenic bumps is the result of sandy material and dust fixing by plant roots, especially litter across large bushes are very weak saline[3].
The soil cover is formed on the layered saline lake-alluvial and eolian deposits. The formation and development of soil cover, on the studied area, was in close dependence with the Aral Sea fluctuation levels. Large areas of the studied territory are occupied by dross, as residues of ancient riverbeds and dried up lakes, and sands (deflated lake-alluvial deposits).
Within the dried border of the dried bottom, coastal salt marshes and saline, coastal soils with windblown sandy cover and takyr soils are formed. Desert sandy soils are formed in the border of exposure of 10 years drying. Soil formation of the dried strip is determined by the desert climate; it contributes to the rapid transformation and mostly depends on the
lithology of bottom deposits and nature of the coastline [4].
Desert climate determines the overall development of salinization processes. Following arid-nature of exposure contributes its desalinization and soil forming of the zonal type. This trend depends on litho-logical and geomorphological conditions. All soils have a low humus content, relatively small thickness of the humus horizon, low nutrition, and low absorption capacity. In addition, they are characterized by a high carbonate content and salinity. The main sources of soil salinity are saline soil material, and salts that comes from saline groundwater. Types of salinity based on anions - chloride, sulfate-chloride, chloridesulfate; based on cation - magnesium-sodium-calcium. Different hydromorphic and salinity levels of soil have caused wide development of complex soils.
Meadow-marsh soils are formed during transformation of marsh soils because of changes in the hy-drological state, reduced groundwater level to 1.5-2.0 m, which leads to draining, and change in water-air state of soil. However, during rice sowing and restoring moisture conditions of meadow-marsh soil again turn into swamp or rice-swamp. Outside area of flooding in the rice fallows, soils are quickly deserted, groundwater decrease by 3-5 m; as a part of the vegetation cover, on the background of reeds, alkali grasses and agrestal plants are settled, and hence increasing processes of soil salinization. Water-soluble salt distribution in the soil profile is as follows: a small maximum from the surface with a sharp decline of profile
to a minimum.
0-1,5 1,5-11 11-25 25-36 36-46 46-83 83-129 Depth of sampling, cm
Figure 1 - Water-soluble salts distribution in the soil profile of meadow-marsh soil Chemical composition: based on anions chloride - sulfate, based on cation magnesium-sodium-calcium.
mg/eq
25 20 15 10 5 0
1-1
-
- -
■ -П J 1 ■ "П _ „ п-п—п
0-1,5 1,5-11 11-25
25-36
36-46 46-83 83-129 cm
□ НСОэ n °SO4 °a °g °+K
_l_
Figure 2 - The content of soluble salts in meadow-marsh soil
Figure 3 - humus content in meadow-marsh soil
The high humus content in the crust and sub crust horizons - 5.51 - 5.62 %; deeper content is low -0.41-0.48 %.
Salt marshes can be traced along the edge of the water's edge in terms of intensive sea surf, which develop under rare saltwort vegetation (glasswort, sea blite etc.). Groundwater of chloride and some sulfate salinity types, have mineralization of 20-80 g/l, at depth of 0.3 to 3.0 m. The soil materials are layered marine deposits of sand-clay composition. Slight accumulation of salts is observed on the surface of the upper 10 cm layer, going deeper into the soil profile gradual accumulation of salts to the maximum values can be observed, as for second layer. Chemistry salinity type: for anions chloride-sulfate-magnesium, for cation based calcium-sodium. Content of the humus is low - 0.07 % - 0.74 %, which is typical for this kind of soils.
Coastal salt marshes are formed from marsh saline after 2-3 years of drying of bottom deposits at a sufficiently high surface and ground level of moisture. Soil-forming materials are layered lake and marine deposits with predominance of shelly sand and loam. Coastal salt marshes are the youngest soils of the area that are formed on the former sea bottom after the retreat of the sea. Cracked surface with occasional shells and clumps of vegetation. Strong salinity, visible accumulation of salt crystals, rusty, clay spots are formed on the surface of whole soil profile. With the depth, profile hydration increases - lower levels are wet, with bluish coloration becomes yellowish-bluish and brown coloration. Salt distribution of the soil profile is unbalanced: higher concentration is in crust and sub crust layers, with depth concentration decreases.
u
%
0-1 1-2 2-19 19-32 32-58 61-96 96-125
Depth of sampling, cm
Figure 4 - Water-soluble salts distribution in the soil profile of coastal marsh soil
The chemistry of salinity: chloride-sulfate on anions based, and magnesium-calcium-sodium on cation based.
(mg
/eq) 100 -
80 -
60 -
40 -
20 -
0 -
0-1 1-2 2-19 19-32 32-58 61-96 96-125 cm
□ НСО3 □ □ CO4 □ a □ g □ Na+K l
_ 1-1 n
—i- .1. 1. ■ "1- 1-я ■ "tail 1-1 _r-i_ 1-1
Figure 5 - The content of soluble salts in coastal marsh soil
Humus content is higher at crust layer (3.39 %) and sub crust layer (1.24 %), along the entire profile humus content is low - (0.24-0.65 %)
¡3 sP
x Ь
1-2
2-19
19-32
32-58
61-96
96-
Depth of sampling, cm
Figure 6 - Total humus content in coastal salt marsh
125
Dried salt marsh, the area adjacent to the state reserve Barsakelmes, absolute wasteland. Wasteland has flat smooth surface, covered with a dense smooth gray crust of 0.5-1 cm with numerous shells and their residues; and salt sequins, white specks. There are rare phytogenic hillocks of 0.5-0.8m height on the surface, with an underlay of dried seaweed coated with sand. They are occupied with tamarisk of 30-50 cm height. Soil based on profile boils from 10% HCl. Water-soluble salts in the profile are as follows: the maximum concentration is in crust and sub crust horizons, decreasing with depth. The chemistry of salinity: chloride-sulfates on anions based, and magnesium-calcium-sodium on cation based. Humus content is higher at crust layer (0.83 %) and sub crust layer (0.79 %), along the entire profile humus content is low -(0.34-0.65 %)
Coastal soils with windblown sandy cover are formed in the border of sea exposure during formation
of cumulus sands mainly after 9 years of drying and occupied a large area. Windblown sandy cover has capacity of 20-30 cm and 30-50 cm. Formation of mulch sandy layer, reduction of surface evaporation, moisture accumulation in the middle and lower part of the profile (washing mode) contributes to occurrence of xeromesophilic vegetation. Vegetation cover is represented by xeromesophyte, Ceratocarpus, quinoa and perennial shrub and suffrutescent vegetation (tamarisk). Ground water mineralization 50-70 g/l at depth of 1.2-1.5 m. In the surface layer at depth of 40-50 cm horizon of physical draining is formed; hence, the border of capillary fringe is decreased. Groundwater levels of salinization and mineralization are different. The degree of salinity is different from slightly saline on the surface layer to the medium- and strongly saline, depending depth of the profile and it has maximum degree at layer of 29-43 cm and 75-130 cm.
%
0-7 7-17 17-40 40-50 50-80 80-112
Figure 7 - Water-soluble salts content in the profile of coastal soil with windblown sand cover In the upper horizons dominated: on anions based - chloride-sulfate, deeper sulfate-chloride; on cation based
magnesium-sodium-calcium chemistry salinity.
%
%
П il —
1-1 il
-Г " - -г Ш _ — — ï
100
80
60
40
20
0
см
□ НСО3 □ Cl □ SO4 □ Ca □ Mg □ Na ПК
Figure 8 - the content of soluble salts in the coastal soil with windblown sand cover The total humus content is higher in the bottom soil horizons (0.93 %).
y
0,6 0,5 0,4 0,3 0,2 0,1 0
%
-1---г-
0-7 7-17 17-40
40-50
50-80 с cm
□ ryHumus
== (cm)-
Figure 9 - Total humus content in coastal so« w ith windblown sand cover
Takyr-like soils are formed in condition of auto-morphic on young lake-alluvial stratified deposits of different lithological and chemical compositions, which are characterized by evaporating nonleaching water regime. Soil materials is represented by sandy-dusty residually, saline carbonated sand-clay alluvial deposits. Groundwater is deep-seated (5-10 m or more). There are pale gray highly porous crusts on the surface, with capacity of 5-10 cm. The crust is denser and roughly packed in the alkaline soils, and in sandy soil, it is covered with fine-grained sand of varying capacity. The loose packed scaly foliated structural horizon is released under the crust at 5-10 cm depth. Light brown clayey compressed horizon is released at depth of 15-30 cm, which contains carbonates and soluble salts, this horizon is highly compressed in saline alkali soils, and differs by having lumpy and nuci-
form structure with various salts secretions. In takyr saline soils salinity (sulfate-chloride and chloride) is described at a depth of 20-30 cm with salt content of 0.3-1 % and more. Past hydrogenic nature of soil formation can be noticed in takyr soils (decomposed plant deposits, dark-colored marsh layers, clayey and rusty spots etc.). Combined indicators of takyr soils are: low humus of fulvic-acid content, low content of mineral nutrients for plants, low absorption capacity, high alkalinity, alkalinity and residual salinity. Vegetation cover of takyr soil forms open saxaul-wormwood-saltwood groups with low content of ephemers and ephemeroids (sagebrush, anabasis-salsa, tamarisk, peppergrass, blue grass, (Eremopyrum trit-iceum (Gaertn.) Nevski), etc.). The average salinity of takyr soil's upper horizons is differ with depth to a very strong salinity degree.
Figure 10 - Highly soluble salts in the soil profile of takyr soils The chemistry of salinity in the upper horizon 0-9 cm depth: chloride-sulfate mainly sulfate-chloride, and magnesium-calcium-sodium.
%/мг-э 100 90 80 70 60 50 40 30 20 10 0
mg/eq
1
1
I =
гг hr. ■
0-3
3-9
9-32
32-50
50-96
96-118
□ НСОЗ □ cm SO4 □ Ca □ Mg □ Na ПК
см
Figure 11 - Highly soluble salts, water-soluble salts in takyr soils Total humus content increases with depth until 50-96 cm layer (1.04%)
% 1,2 -|-
1
0,8 0,6 0,4 0,2
0-3
3-9
9-32
32-50
50-96
см
□ Гу
Figure 12
3 Conclusions
Long-term monitoring studies of modern Syrdar-ya delta have identified a great diversity of soils and variety of characteristics that are common in the delta of hydromorphic soils. The area is characterized by hydromorphic and automorphic soils: gray-brown soils of outcrops are typically automorphic; takyr soils are currently developing in automorphic conditions, in the recent past they have experienced hydromorphic stage of formation. There is presence of transition soils - from soil hydromorphic stage to automorphic. Currently, the uniqueness and complexity of delta's soil cover can be explained by the peculiar combination of soil formation factors: it is caused by aridity processes against background of an acute shortage of water resources, as a regulated river flow, Syrdarya flood spills were ceased, and the hydrological regime of the delta plains was changed. Desiccation and desertification processes delta is accompanied by the increased salinity of hydromorphic soils. Intensity of salt accumulation in soils of different parts of delta varies depending on the established hydrological con-
Hum
(cm) -
Total humus Co mem in takyr soil
ditions: salinity of 0-100cm layer of meadow soils have risen 2 times, marsh soils - 3 times.
Desertification is associated with reduced fertility of hydromorphic soils and decrease of humus content, total nitrogen. Change of soil fertility is caused by reduction of soil and biogenic runoff, change of vegetation and reduction of biological productivity in the process of changes in the hydrological regime. In the process of desertification, physical, water-physical, and physical-chemical properties are significantly deteriorated.
Increased water flow in the modern delta of the Syrdarya from 3-3.5km3/year to 8-9km3/year has affected only on lake system improvement and some resuscitation (temporary) of hydromorphic soils in the area of 420 thousand hectares. Dried alluvial-meadow, swampy-meadow and meadow-swampy soils are transformed into normal alluvial-meadow and swampy-meadow, meadow-swampy and swampy soils.
The increasing erosion and deflation processes exacerbate critical state of modern Syrdarya delta. Wind erosion is manifested in the form of deflation of
0
sandy and automorphic soils, dust storms and saline deflation; water erosion is shown locally on the slopes of the tertiary outcrops. Anthropogenic factor plays significant role in development of soil deflation: uncontrolled livestock grazing, felling of brushwood, vehicle traffic outside the roads promote intensification of deflationary processes that are changing soil properties, causing degradation.
Soil fertility restoration and preventing of delta soils degradation is related to rational use of water resources. To optimize water regulation dam construction and reconstruction of sewer and irrigation networks are required.
The decline of the Aral Sea level and acute shortage of water resources have dramatically changed the conditions of soil formation on dried territory. At the dried bottom huge massif of different salt marshes were formed (marsh, coastal, crust-salt marshes). The total area of salt marshes has been increased to 746 thousand hectares, but the marsh and a coastal marsh was decreased: marsh and coastal saline soils were transformed in crust-salt marshes and sor salt marshes or coastal hydromorphic saline soils in 2-3 years period.
Studies that were conducted in the eastern part of Aral Sea region on the border of dried bottom of the Aral Sea in 2007 and 2008 showed that in condition of aridity, negative processes development (salinity, aridity, deflation) is still present.
Eolian-deflationary process are developed ubiquitously, but in areas with the groundwater level less than 2m they are developed the most, hence exposing sandy deposits from the surface. Sea-bottom and alluvial deposits are the most exposed towards eolian processing. Dusty sands are the most processed, the less processed are the light sandy loams, and the least processed are heavy loams, loams and clays. To a greater extend deflationary processes are manifested on the dried sea bottom, where active deflation of sandy
massifs are manifested in the form of wind erosion, deflation and removal of sand dust material from the surface of the salt marshes. Bands, pits of wind blowing, phytogenic hills, dunes, sand dunes that are marked with sand wave ripples are formed on such areas. Soil areas with windblown sand cover are increased and the new sand contours with hilly-ridge sands are produced.
Maximum accumulations of salts were observed in soil profile from the coastal area with windblown cover of crust salt marsh. Salt accumulation is decreased with further desiccation of former sea bottom, takyr soil has average level of salinity to a depth of 32 cm, and more deeply, soil is getting highly saline.
Soils of the dried bottom are characterized with low humus content and it has tendency to distribution: increased level in crust and sub crust layers, and a significant reduction and even absence in the rest soil horizons, they are characterized with low availability of gross and mobile forms of nitrogen and phosphorus.
Basic contours of soil complexes that consist of different types of soils and their percentages were changed. Areas of main types of soils were calculated of the territory of modern delta and the Aral Sea dried bottom, i.e. the view Aral Sea dried bottom soil transformation was given, and its orientation in the process of anthropogenic aridity. "Soil map of modern Syrdarya delta and dried bottom of Aral Sea" was mapped, of the Eastern part of Aral Sea region of Kazakhstan in scale of 1:200 000.
Environmental sustainability improvement and biological productivity of anthropogenically degraded soils improvement activities were developed with usage of moisture-retaining hydrogels, adaptogen preparations based on fertilizers and humus substances, that are stimulates plants energy potential with increased rooting effect for the survival of plants under adverse
conditions of desert areas.
References
1. Borovski V. M., Pogrebenski M. A. "Ancient delta of Syrdarya and north Kyzyl-kum" vol.1. Almaty. 1958. - P. 514
2. Borovski V. M., Pogrebenski M. A. "Soil formation of continental deltas and its reclamation". Soil fertility and reclamation in USSR (reports to the VIII international congress of Soil Science). Nauka. 1964. - P. 2128.
3. Kozybaeva F. E., Tomina T. K., Azhikina N. Z. "Soil transformation of the Aral Sea region in arid conditions and increase of environmental sustainability" From: Recent problems of Geobotany. Materials from International Conference dedicated to the memory of the outstanding scientist, the founder of geobotany school of Kazakhstan. Ph. D. Bykov B. A. with his 100th anniversary (Almaty. 11-13 May. 2011). Almaty. 2011. - P. 133139.
4. Borovsky V. M. "Salt accumulation on alluvial plains and development of anthropogenic desertification. Anthropogenic drying up of the Aral Sea region soils." Nauka. 1984. - P.4-37.
