Water content

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Soil composition

Water content or moisture content is the quantity of water contained in a material, such as soil (called soil moisture), rock, ceramics, or wood on a volumetric or gravimetric basis. The property is used in a wide range of scientific and technical areas, and is expressed as a ratio, which can range from 0 (completely dry) to the value of the materials' porosity at saturation.

Volumetric water content, θ, is defined mathematically as:

$\theta = \frac{V_w}{V_b}$

where $V w$ is the volume of water and $V b$ (or $V s$ for soil) is the bulk material volume. Water content may also be based on its mass or weight, thus the gravimetric water content is defined as:

$u = \frac{m_w}{m_b}$

where $m w$ is the mass of water and $m b$ (or $m s$ for soil) is the bulk material mass.

To convert gravimetric water content to volumetric water, multiply the gravimetric water content by the bulk density of the material.

In petroleum engineering, the term water saturation, $S w$ is used, defined as

$S_w = \frac{V_w}{V_b\phi} = \frac{\theta}{\phi}$

where $φ$ is the porosity.

1 Measurement
2 Classification and uses
- 2.1 Earth and agricultural sciences
3 See also
4 References

Volumetric water content can be directly measured using a known volume of the material, and a drying oven. Volumetric water content, θ, is calculated^[1] using:

$\theta = \frac{m_{\text{wet}}-m_{\text{dry}}}{\rho_w \cdot V_b}$

where

m wet

and

m dry

are the masses of the sample before and after drying in the oven;

ρ w

is the density of water; and

V b

is the volume of the sample before drying the sample

For materials that change in volume with water content, such as wood, the water content, u, is expressed in terms of the mass of water per unit mass of the moist specimen:

$u = \frac{m_{\text{wet}} - m_{\text{dry}}}{m_{\text{wet}}}$

However, geotechnics requires the moisture content to be expressed as a percentage of the sample's dry weight i.e. % mosisture content = $u * 100$

Where

$u = \frac{m_{\text{wet}} - m_{\text{dry}}}{m_{\text{dry}}}$

Main article: Moisture analysis

Other methods that determine water content of a sample include chemical titrations (for example the Karl Fischer titration), determining mass loss on heating (perhaps in the presence of an inert gas), or after freeze drying. In the food industry the Dean-Stark method is also commonly used.

From the Annual Book of ASTM (American Society for Testing and Materials) Standards, the total evaporable moisture content in Aggregate (C 566) can be calculated with the formula:

$p = \frac{W-D}{D}$

where $p$ is the fraction of total evaporable moisture content of sample, $W$ is the mass of the original sample, and $D$ is mass of dried sample.

There are several geophysical methods available that can approximate in situ soil water content. These methods include: time-domain reflectometry (TDR), neutron probe, frequency domain sensor, capacitance probe, electrical resistivity tomography, and others that are sensitive to the physical properties of water. Geophysical sensors are often used to monitor soil moisture continuously in agricultural and scientific applications.

Satellite microwave remote sensing is used to estimate soil moisture based on the large contrast between the dielectric properties of wet and dry soil. The data from microwave remote sensing satellite such as: WindSat, AMSR-E, RADARSAT, ERS-1-2 are used to estimate surface soil moisture [1].

Moisture may be present as adsorbed moisture at internal surfaces and as capillary condensed water in small pores. At low relative humidities, moisture consists mainly of adsorbed water. At higher relative humidities, liquid water becomes more and more important, depending on the pore size. In wood-based materials, however, almost all water is adsorbed at humidities below 98% RH.

In biological applications there can also be a distinction between physisorbed water and free water — the physisorbed water being that closely associated with and relatively difficult to remove from a biological material. The method used to determine water content may affect whether water present in this form is accounted for.

Water molecules may also be present in materials closely associated with individual molecules, as "water of crystallization", or as water molecules which are static components of protein structure.

In soil science, hydrology and agricultural sciences, water content has an important role for groundwater recharge, agriculture, and soil chemistry. Recent research has aimed toward a predictive-understanding of water content over space and time. In general, observations have revealed that spatial variance tends to increase as water content increases in semiarid regions, to decrease as water content increases in humid regions, and to peak at intermediate water contents in temperature regions ^[2] .

There are four standard water contents that are routinely measured and used, which are described in the following table:

Name	Notation	Suction pressure (J/kg or kPa)	Typical water content (vol/vol)	Description
Saturated water content	θ_s	0	0.2–0.5	Fully saturated water, equivalent to effective porosity
Field capacity	θ_fc	−33	0.1–0.35	Soil moisture after 2–3 days after a rain or irrigation
Permanent wilting point	θ_pwp or θ_wp	−1500	0.01–0.25	minimum soil moisture at which a plant wilts
Residual water content	θ_r	−∞	0.001–0.1	Remaining water at high tension

And lastly the available water content, θ_a, which is equivalent to:

θ_a ≡ θ_fc − θ_pwp

which can range between 0.1 in gravel and 0.3 in peat.

When a soil gets too dry, plant transpiration drops because the water is becoming increasingly bound to the soil particles by suction. Below the wilting point plants are no longer able to extract water. At this point they wilt and cease transpiring altogether. Conditions where soil is too dry to maintain reliable plant growth is referred to as agricultural drought, and is a particular focus of irrigation management. Such conditions are common in arid and semi-arid environments.

Some agriculture professionals are beginning to use environmental measurements such as soil moisture to schedule irrigation. This method is referred to as "Smart Irrigation."

In saturated groundwater aquifers, all available pore spaces are filled with water (volumetric water content = porosity). Above a capillary fringe, pore spaces have air in them too.

Most soils have a water content less than porosity, which is the definition of unsaturated conditions, and they make up the subject of vadose zone hydrogeology. The capillary fringe of the water table is the dividing line between saturated and unsaturated conditions. Water content in the capillary fringe decreases with increasing distance above the phreatic surface.

One of the main complications which arises in studying the vadose zone, is the fact that the unsaturated hydraulic conductivity is a function of the water content of the material. As a material dries out, the connected wet pathways through the media become smaller, the hydraulic conductivity decreasing with lower water content in a very non-linear fashion.

A water retention curve is the relationship between water content and the water potential of the porous medium. It is characteristic for different types of porous medium. Due to hysteresis, different wetting and drying curves may be distinguished.

The normalized water content, $Θ$ , (also called effective saturation or $S e$ ) is a dimensionless value defined by van Genuchten^[3] as:

$\Theta = \frac{\theta - \theta_r}{\theta_s-\theta_r}$

where $θ$ is the volumetric water content; $θ r$ is the residual water content, defined as the water content for which the gradient $d θ / d h$ becomes zero; and, $θ s$ is the saturated water content.

^ Dingman, S.L. (2002). "Chapter 6, Water in soils: infiltration and redistribution", Physical Hydrology, Second Edition, Upper Saddle River, New Jersey: Prentice-Hall, Inc., 646 pp. ISBN 0-13-099695-5.
^ Lawrence, J. E., and G. M. Hornberger (2007). "Soil moisture variability across climate zones". Geophys. Res. Lett. 34 (L20402, doi:10.1029/2007GL031382).
^ van Genuchten, M.Th. (1980). "A closed-form equation for predicting the hydraulic conductivity of unsaturated soils". Soil Science Society of America Journal 44 (5): 892–898.

v • d • e Physical aquifer properties used in hydrogeology
hydraulic head · hydraulic conductivity · storativity · porosity · water content

v • d • e Topics in geotechnical engineering
Soils	Clay · Silt · Sand · Gravel · Peat
Soil properties	Hydraulic conductivity · Water content · Void ratio · Bulk density · Thixotropy · Reynolds' dilatancy · Angle of repose · Cohesion · Porosity · Permeability · Specific storage
Soil mechanics	Effective stress · Pore water pressure · Shear strength · Overburden pressure · Consolidation · Soil compaction · Soil classification · Shear wave
Geotechnical investigation	Cone penetration test · Standard penetration test · Exploration geophysics · Monitoring well · Borehole
Laboratory tests	Atterberg limits · California bearing ratio · Direct shear test · Hydrometer · Proctor compaction test · R-value · Sieve analysis · Triaxial shear test · Hydraulic conductivity tests · Water content tests
Foundations	Bearing capacity · Shallow foundation · Deep foundation · Dynamic load testing · Wave equation analysis · Crosshole sonic logging
Retaining walls	Lateral earth pressure · Mechanically stabilized earth · Soil nailing · Tieback · Gabion · Slurry wall
Slope stability	Mass wasting · Landslide
Earthquakes	Soil liquefaction · Response spectrum · Seismic hazard · Ground-structure interaction
Geosynthetics	Geotextile · Geomembranes · Geosynthetic clay liner

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Water content

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Water content

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