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Soil moisture is the water held between soil particles in the root zone (rhizosphere) of plants, generally in the top 200 cm of soil. Water storage in the soil profile is extremely important for agriculture, especially in locations that rely on rainfall for cultivating plants.
Water retention curve is the relationship between the water content, θ, and the soil water potential, ψ. This curve is characteristic for different types of soil, and is also called the soil moisture characteristic . It is used to predict the soil water storage, water supply to the plants ( field capacity) and soil aggregate stability.
Pores (the spaces that exist between soil particles) provide for the passage and/or retention of gasses and moisture within the soil profile.The soil's ability to retain water is strongly related to particle size; water molecules hold more tightly to the fine particles of a clay soil than to coarser particles of a sandy soil, so clays generally retain more water. [2]
For a confined aquifer or aquitard, storativity is the vertically integrated specific storage value. Specific storage is the volume of water released from one unit volume of the aquifer under one unit decline in head. This is related to both the compressibility of the aquifer and the compressibility of the water itself.
Available water capacity. Available water capacity is the amount of water that can be stored in a soil profile and be available for growing crops. [1] It is also known as available water content ( AWC ), profile available water ( PAW) [2] or total available water ( TAW ). The concept, put forward by Frank Veihmeyer and Arthur Hendrickson, [3 ...
Water balance in a basin. A general water balance equation is: [ 5] P = Q + ET + ΔS. where. P is precipitation. Q is streamflow. ET is evapotranspiration. ΔS is the change in storage (in soil or the bedrock / groundwater) This equation uses the principles of conservation of mass in a closed system, whereby any water entering a system (via ...
Richards equation. The Richards equation represents the movement of water in unsaturated soils, and is attributed to Lorenzo A. Richards who published the equation in 1931. [ 1] It is a quasilinear partial differential equation; its analytical solution is often limited to specific initial and boundary conditions. [ 2]
Field capacity. Field capacity is the amount of soil moisture or water content held in the soil after excess water has drained away and the rate of downward movement has decreased. This usually takes place two to three days after rain or irrigation in pervious soils of uniform structure and texture. The physical definition of field capacity ...
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