DOI: 10.2478/v10025-012-0034-8 © Polish Academy of Sciences, Committee for Land Reclamation JOURNAL OF WATER AND LAND DEVELOPMENT and Environmental Engineering in Agriculture, 2012 J. Water Land Dev. 2012, No. 17 (VII–XII): 61–67 © Institute of Technology and Life Science, 2012 PL ISSN 1429–7426 Available (PDF): www.itep.edu.pl/wydawnictwo; http://versita.com/jwld/ Received 16.11.2011 Reviewed 16.11.2012 Accepted 26.11.2012 Water and physical characteristics A – study design B – data collection of irrigated soils C – statistical analysis D – data interpretation E – manuscript preparation in the Massif of Mugan-Salyan F – literature search Mustafa Gilman MUSTAFAYEV ABCDEF Institute of Soil Science and Agrochemistry of ANAS, Baku, Azerbaijan, AZ 1073 M. Arif-5; tel. 99412 39-97-16, e-mail: [email protected] For citation: Mustafayev M.G. 2012. Water and physical characteristics of irrigated soils in the Massif of Mugan-Salyan. Journal of Water and Land Development. No. 17 p. 61–67 Abstract Detailed information about the water and physical properties of irrigated soils in the Massif of Mugan- -Salyan is given in the paper. Results of the study showed differences in the soil properties. The field water ca- pacity of soil in the zone was 25.32–30.30% or 1.26–1.56 g·cm–3, particle density was 2.53–2.88 g·cm–3, porosity – 44.16–54.20%; clay content – 22.54–70.10% and the velocity of soaking the soil with water ranged between 9.24 and 55.84 cm·h–1. Such variability of the indices points to a need for reclamation measures in the soils. Key words: bulk density, soaking velocity, soil density, soil porosity, soil texture, water and physical properties INTRODUCTION that physical soil characteristics directly affect the growth and development of plants. The main problem As a result of the agrarian reforms, state and of this study was to analyse changes in the water and commune farms were liquidated and agricultural physical properties of arable soils in the massif zone lands were distributed among private farmers. At pre- and to propose reclamation measures for their im- sent the farmers begin their good practices and their provement. soils are used under sowing. It is obvious that collec- tor-drainage systems and technical state of the irriga- STUDY OBJECT AND METHODS tion canals are poor and consequently the reclamation status of soils becomes worse and worse due to the Eight sampling sites characteristic for the Mu- neglect in the transitional period. That's why it is nec- gan-Salyan Massif were selected. The soils of the dis- essary to provide the development of agricultural sys- trict were formed on alluvial rocks created as an effect tem according to the contemporary requirements, to of the activity of the Kur River. Material carried by increase the rationality of the irrigation-drainage net- the Kur River formed silt deposits which periodically works, to improve reclamation status of soils, to es- filled its river bed. Then river waters raised and tablish their fertility and to carry out measures appro- flooded the surroundings resulting in the coverage of priate for the new conditions. The chance of using flooded lands by silty deposits. A lot of soils covering subsoil waters for irrigation is limited and the main the zone possess alluvial character. It can be ex- sources of water remain the Kur and Araz Rivers. Wa- plained by the characters of soil forming rocks. The ter and physical features of soils are not stable, they clayey profile of the soil in some areas show that the change continuously in the effect of both natural con- same soils developed on delluvial-alluvial heaps on ditions and agro-technical measures. The studies show debris cone of the Kur River and of other small rivers. © Polish Academy Sciences (PAN) in Warsaw, 2012; © Institute of Technology and Life Science (ITP) in Falenty, 2012 62 M.G. MUSTAFAYEV A lot of soil forming rocks are rich in salts and car- were executed. Field water capacity, water soaking bonates; that’s why developed soils are saline to ability, soil structure, bulk density, particle density a different degree. and porosity belong to the main water and physical Climate of this zone is semi-desert of dry and features of any soil. steppe type (the summer is moderately hot). This type Field water capacity was measured in selected of climate is characterised by low humidity, moderate sampling sites 2×2 m. Blocks 70 cm wide and 35 cm winter and dry and hot summer. The coldest months high were drawn around the selected square-shaped are January and February and the hottest months are areas. The iron frame of a size of 1×1 m and a height July and August. Dry and hot summer of this zone of 20 cm was pressed into the soil to a depth of no influences plant cover and soil forming processes less than 10 cm in the middle of the square. Two [EYUBOV 1968; SHIKHLINSKY 1969]. Mean monthly squares were thus sampled: the inner square called an temperature of the hottest month is 26.1–26.5°C, that account square and the outer square called the protec- of the coldest month is 1.8–2.5°C. Annual rainfall tive one. After the squares were ready, water was varies between 187 and 309 mm in the region. Gener- poured into both squares at the same time. Pouring ally, maximum rainfall is observed in the spring water into the little squares was continued till filling months and minimum – in the summer. The average the porosities of the account soil layer with water. yearly relative air humidity varies from 72.3 to After the soil became saturated totally with water, the 75.0%. Maximum relative air humidity is observed in two little squares were covered with a pellicle to pre- the winter and minimum – in the summer months. vent from water evaporation. Two-three days after That's why agricultural plants need irrigation in the covering, the soil samples were taken every 10 cm till summer months. The dry climate affects soil cover, 1 m depth in three repetitions from the middle of the too. Thus, natural vegetation develops poorly there little square (from within the iron frame) and soil which is the reason for low accumulation of humus moisture was determined by a thermostat-gravimetric materials in the soil. Secondary salinization occurs in method. The little squares were covered tightly after places where the subsoil water is near the soil surface each moisture measurement. Moisture measurements because evaporation is very intensive on hot summer in the soil samples were continued till obtaining the days. The level of subsoil water is different and de- same moisture of a given layer for three consecutive pends on land relief. The time when the subsoil wa- days. This stabilized moisture was assumed the field ters are near the surface is May–June, from the end of water capacity of the soil. June water level begins to decline. October is consid- ered a time when the subsoil waters are the deepest. RESULTS AND DISCUSSION The subsoil waters are not present in north and north- west parts of the region [BABAYEV 2005; BEHBUDOV SOAKING VELOCITY OF WATER INTO THE SOIL 1977]. Studies on the subsoil waters showed that their total slope followed the inclination of land surface. A velocity of water soaking was determined in The level of subsoil waters was noted to rise along the order to characterize soil permeability. To determine Kur River and big irrigation canals which was the the soaking velocity of water, the formulas by A.N. evidence for the effect of surface flows on subsoil Kostyakov were used and the indices obtained from water table. Besides, the rise of subsoil water level is the field works according to methods described observed in the areas affected by mud-volcano waters. above. Obtained velocity of water soaking was used Shallow subsoil waters stretch as a strip along the to attribute a soil to the type of water soaking group. Caspian Sea shore. The calculation followed A.N. Kostyakov's [KOSTYA- The main soil features were taken into consid- KOV 1960] equations: eration while selecting sampling sites. The study on the water and physical characteristics were performed K K = o (1) under field and laboratory conditions. Field water ca- or t a pacity, bulk density and the velocity of water soaking into the soil were determined in the field and in the where: laboratory. Soil structure and particle density were Kor – velocity of water soaking into the soil ex- –1 measured under laboratory conditions using soil sam- pressed in mm·min ; ples taken from little squares in the sampling sites. Ko – an average velocity of water soaking the soil –1 Soil porosity was calculated from the determined bulk for the first minute, mm·min . and particle densities. K The characteristic areas were distinguished to K = 1 (2) analyse changes in the water and physical characteris- o 1− a tics of soils salinized to a different degree (weak, me- where: dium and strong). The soil samples were taken from K1 – an average soaking velocity of water at the the same places and appropriate chemical analyses end of the first minute, mm·min–1. © PAN in Warsaw, 2012; © ITP in Falenty, 2012; J. Water Land Dev. No. 17 (VII–XII) Water and physical characteristics of irrigated soils in the Massif of Mugan-Salyan 63 a those of the mean soaking velocity less than 5.0 cm·h–1, 1 = d tKK 2 (3) moderately permeable soils had the velocity between 5.0 and 15 cm·h–1 and highly permeable – above 15.0 where: –1 –1 cm·h .