# Water content

Water content or moisture content is the quantity of water contained in a material, such as soil (called soil moisture), rock, ceramics, crops, or wood. Water content 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. It can be given on a volumetric or mass (gravimetric) basis.

## Definitions

Volumetric water content, θ, is defined mathematically as:

${\displaystyle \theta ={\frac {V_{w}}{V_{\text{wet}}}}}$

where ${\displaystyle V_{w}}$ is the volume of water and ${\displaystyle V_{\text{wet}}=V_{s}+V_{w}+V_{a}}$ is equal to the total volume of the wet material, i.e. of the sum of the volume of solid host material (e.g., soil particles, vegetation tissue) ${\displaystyle V_{s}}$, of water ${\displaystyle V_{w}}$, and of air ${\displaystyle V_{a}}$.

Gravimetric water content[1] is expressed by mass (weight) as follows:

${\displaystyle u={\frac {m_{w}}{m}}}$

where ${\displaystyle m_{w}}$ is the mass of water and ${\displaystyle m}$ is the mass of the substance.

For materials that change in volume with water content, such as coal, the gravimetric water content, u, is expressed in terms of the mass of water per unit mass of the moist specimen (before drying):

${\displaystyle u'={\frac {m_{w}}{m_{\text{wet}}}}}$

However, woodworking, geotechnics and soil science require the gravimetric moisture content to be expressed with respect to the sample's dry weight:

${\displaystyle u''={\frac {m_{w}}{m_{\text{dry}}}}}$

Values are often expressed as a percentage, i.e. u×100%.

To convert gravimetric water content to volumetric water content, multiply the gravimetric water content by the bulk specific gravity ${\displaystyle SG}$ of the material:

${\displaystyle \theta =u\times SG}$.

### Derived quantities

In soil mechanics and petroleum engineering the water saturation or degree of saturation, ${\displaystyle S_{w}}$, is defined as

${\displaystyle S_{w}={\frac {V_{w}}{V_{v}}}={\frac {V_{w}}{V\phi }}={\frac {\theta }{\phi }}}$

where ${\displaystyle \phi =V_{v}/V}$ is the porosity, in terms of the volume of void or pore space ${\displaystyle V_{v}}$ and the total volume of the substance ${\displaystyle V}$. Values of Sw can range from 0 (dry) to 1 (saturated). In reality, Sw never reaches 0 or 1 - these are idealizations for engineering use.

The normalized water content, ${\displaystyle \Theta }$, (also called effective saturation or ${\displaystyle S_{e}}$) is a dimensionless value defined by van Genuchten[2] as:

${\displaystyle \Theta ={\frac {\theta -\theta _{r}}{\theta _{s}-\theta _{r}}}}$

where ${\displaystyle \theta }$ is the volumetric water content; ${\displaystyle \theta _{r}}$ is the residual water content, defined as the water content for which the gradient ${\displaystyle d\theta /dh}$ becomes zero; and, ${\displaystyle \theta _{s}}$ is the saturated water content, which is equivalent to porosity, ${\displaystyle \phi }$.

## Measurement

### Direct methods

Water content can be directly measured using a drying oven.

Gravimetric water content, u, is calculated[3] via the mass of water ${\displaystyle m_{w}}$:

${\displaystyle m_{w}=m_{\text{wet}}-m_{\text{dry}}}$

where ${\displaystyle m_{\text{wet}}}$ and ${\displaystyle m_{\text{dry}}}$ are the masses of the sample before and after drying in the oven. This gives the numerator of u; the denominator is either ${\displaystyle m_{\text{wet}}}$ or ${\displaystyle m_{\text{dry}}}$ (resulting in u' or u", respectively), depending on the discipline.

On the other hand, volumetric water content, θ, is calculated[4] via the volume of water ${\displaystyle V_{w}}$:

${\displaystyle V_{w}={\frac {m_{w}}{\rho _{w}}}}$

where ${\displaystyle \rho _{w}}$ is the density of water. This gives the numerator of θ; the denominator, ${\displaystyle V_{\text{wet}}}$, is the total volume of the wet material, which is fixed by simply filling up a container of known volume (e.g., a tin can) when taking a sample.

For wood, the convention is to report moisture content on oven-dry basis (i.e. generally drying sample in an oven set at 105 deg Celsius for 24 hours). In wood drying, this is an important concept.

### Laboratory methods

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:

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

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

### Soil moisture measurement

In addition to the direct and laboratory methods above, the following options are available.

#### Geophysical methods

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, amplitude domain reflectometry, electrical resistivity tomography, ground penetrating radar (GPR), and others that are sensitive to the physical properties of water .[5] Geophysical sensors are often used to monitor soil moisture continuously in agricultural and scientific applications.

#### Satellite remote sensing method

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 microwave radiation is not sensitive to atmospheric variables, and can penetrate through clouds. Also, microwave signal can penetrate, to a certain extent, the vegetation canopy and retrieve information from ground surface.[6] The data from microwave remote sensing satellites such as WindSat, AMSR-E, RADARSAT, ERS-1-2, Metop/ASCAT, and SMAP are used to estimate surface soil moisture.[7]

## Classification and uses

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 or not depending on the pore size can also be an influence of volume. 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. For a better indication of "free" and "bound" water, the water activity of a material should be considered.

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.

### Earth and agricultural sciences

In soil science, hydrology and agricultural sciences, water content has an important role for groundwater recharge, agriculture, and soil chemistry. Many recent scientific research efforts have aimed toward a predictive-understanding of water content over space and time. Observations have revealed generally that spatial variance in water content tends to increase as overall wetness increases in semiarid regions, to decrease as overall wetness increases in humid regions, and to peak under intermediate wetness conditions in temperate regions .[8]

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)
Conditions
Saturated water content θs 0 0.2–0.5 Fully saturated soil, equivalent to effective porosity
Field capacity θfc −33 0.1–0.35 Soil moisture 2–3 days after a rain or irrigation
Permanent wilting point θpwp or θwp −1500 0.01–0.25 Minimum soil moisture at which a plant wilts
Residual water content θr −∞ 0.001–0.1 Remaining water at high tension

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

θa ≡ θfc − θpwp

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

#### Agriculture

When a soil becomes too dry, plant transpiration drops because the water is 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 or soil cultivation.

#### Groundwater

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. The flow of water through and unsaturated zone in soils often involves a process of fingering, resulting from Saffman–Taylor instability. This results mostly through drainage processes and produces and unstable interface between saturated and unsaturated regions.

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 volumetric 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.

## In aggregates

Generally, an aggregate has four different moisture conditions. They are Oven-dry (OD), Air-dry (AD), Saturated surface dry (SSD) and damp (or wet).[9] Oven-dry and Saturated surface dry can be achieved by experiments in laboratories, while Air-dry and damp (or wet) are aggregates' common conditions in nature.

#### Four Conditions

• Oven-dry (OD) is defined as the condition of an aggregate where there is no moisture within any part of the aggregate. This condition can be achieved in a laboratory by heating the aggregate to 220°F (105°C) for a period of time.[9]
• Air-dry (AD) is defined as the condition of an aggregate in which there are some water or moisture in the pores of the aggregate, while the outer surfaces of it is dry. This is a natural condition of aggregates in summer or in dry regions. In this condition, an aggregate will absorb water from other materials added to the surface of it, which would possibly have some impact on some characters of the aggregate.[9]
• Saturated surface dry (SSD) is defined as the condition of an aggregate in which the surfaces of the particles are "dry" (i.e., they will neither absorb any of the mixing water added; nor will they contribute any of their contained water to the mix[9]), but the inter-particle voids are saturated with water. In this condition aggregates will not affect the free water content of a composite material.[10][11]

The water adsorption by mass (Am) is defined in terms of the mass of saturated-surface-dry (Mssd) sample and the mass of oven dried test sample (Mdry) by the formula:

${\displaystyle A={\frac {M_{ssd}-M_{dry}}{M_{dry}}}}$
• Damp (or wet) is defined as the condition of an aggregate in which water is fully permeated the aggregate through the pores in it, and there is free water in excess of the SSD condition on its surfaces which will become part of the mixing water.[9]

#### Application

Among these four moisture condition of aggregates, saturated surface dry is the condition that has the most applications in laboratory experiments, researches and studies, especially these related to water absorption, composition ratio or shrinkage test in materials like concrete. For many related experiments, a saturated surface dry condition is a premise that must be realize before the experiment. In saturated surface dry condition, the aggregate's water content is in a relatively stable and static situation where it would not be affected by its environment. Therefore, in experiments and tests where aggregates are in saturated surface dry condition, there would be fewer disrupting factors than in other three conditions.[12][13]

## References

1. T. William Lambe & Robert V. Whitman (1969). "Chapter 3: Description of an Assemblage of Particles". Soil Mechanics (First ed.). John Wiley & Sons, Inc. p. 553. ISBN 978-0-471-51192-2.
2. 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. Bibcode:1980SSASJ..44..892V. doi:10.2136/sssaj1980.03615995004400050002x. hdl:10338.dmlcz/141699.
3. Dingman, S.L. (2002). "Chapter 6, Water in soils: infiltration and redistribution". Physical Hydrology (Second ed.). Upper Saddle River, New Jersey: Prentice-Hall, Inc. p. 646. ISBN 978-0-13-099695-4.
4. F. Ozcep; M. Asci; O. Tezel; T. Yas; N. Alpaslan; D. Gundogdu (2005). "Relationships Between Electrical Properties (in Situ) and Water Content (in the Laboratory) of Some Soils in Turkey" (PDF). Geophysical Research Abstracts. 7.
5. Lakhankar, Tarendra; Ghedira, Hosni; Temimi, Marouane; Sengupta, Manajit; Khanbilvardi, Reza; Blake, Reginald (2009). "Non-parametric Methods for Soil Moisture Retrieval from Satellite Remote Sensing Data". Remote Sensing. 1: 3–21. Bibcode:2009RemS....1....3L. doi:10.3390/rs1010003.
6. "Archived copy". Archived from the original on 2007-09-29. Retrieved 2007-08-22.CS1 maint: archived copy as title (link)
7. Lawrence, J. E. & G. M. Hornberger (2007). "Soil moisture variability across climate zones". Geophys. Res. Lett. 34 (L20402): L20402. Bibcode:2007GeoRL..3420402L. doi:10.1029/2007GL031382.
8. "Water-to-Cement Ratio and Aggregate Moisture Corrections". precast.org. Retrieved 2018-11-18.
9. "Aggregate Moisture in Concrete". Concrete Construction. Retrieved 2018-11-08.
10. ftp://ftp.dot.state.tx.us/pub/txdot-info/cst/TMS/400-A_series/pdfs/cnn403.pdf
11. Zaccardi, Y. A. Villagrán; Zega, C. J.; Carrizo, L. E.; Sosa, M. E. (2018-10-01). "Water absorption of fine recycled aggregates: effective determination by a method based on electrical conductivity". Materials and Structures. 51 (5): 127. doi:10.1617/s11527-018-1248-2. ISSN 1871-6873.
12. Kawamura, Masashi; Kasai, Yoshio (2009-05-29). "Determination of saturated surface-dry condition of clay–sand mixed soils for soil–cement concrete construction". Materials and Structures. 43 (4): 571–582. doi:10.1617/s11527-009-9512-0. ISSN 1359-5997.