Void ratio

The void ratio (${\displaystyle e}$) of a mixture of solids and fluids (gases and liquids), or of a porous composite material such as concrete, is the ratio of the volume of the voids (${\displaystyle V_{V}}$) filled by the fluids to the volume of all the solids (${\displaystyle V_{S}}$). It is a dimensionless quantity in materials science and in soil science, and is closely related to the porosity (often noted as ${\displaystyle \phi }$, or ${\displaystyle {\eta }}$, depending on the convention), the ratio of the volume of voids (${\displaystyle V_{V}}$) to the total (or bulk) volume (${\displaystyle V_{T}}$), as follows:

${\displaystyle e={\frac {V_{V}}{V_{S}}}={\frac {V_{V}}{V_{T}-V_{V}}}={\frac {\phi }{1-\phi }}}$

in which, for idealized porous media with a rigid and undeformable skeleton structure (i.e., without variation of total volume (${\displaystyle V_{T}}$) when the water content of the sample changes (no expansion or swelling with the wetting of the sample); nor contraction or shrinking effect after drying of the sample), the total (or bulk) volume (${\displaystyle V_{T}}$) of an ideal porous material is the sum of the volume of the solids (${\displaystyle V_{S}}$) and the volume of voids (${\displaystyle V_{V}}$):

${\displaystyle V_{T}=V_{S}+V_{V}}$

(in a rock, or in a soil, this also assumes that the solid grains and the pore fluid are clearly separated, so swelling clay minerals such as smectite, montmorillonite, or bentonite containing bound water in their interlayer space are not considered here.)

and

${\displaystyle \phi ={\frac {V_{V}}{V_{T}}}={\frac {V_{V}}{V_{S}+V_{V}}}={\frac {e}{1+e}}}$

where ${\displaystyle e}$ is the void ratio, ${\displaystyle \phi }$ is the porosity, V_V is the volume of void-space (gases and liquids), V_S is the volume of solids, and V_T is the total (or bulk) volume. This figure is relevant in composites, in mining (particular with regard to the properties of tailings), and in soil science. In geotechnical engineering, it is considered one of the state variables of soils and represented by the symbol ${\displaystyle e}$. ^{[1] [2]}

Note that in geotechnical engineering, the symbol ${\displaystyle \phi }$ usually represents the angle of shearing resistance, a shear strength (soil) parameter. Because of this, in soil science and geotechnics, these two equations are usually presented using ${\displaystyle {\eta }}$ for porosity: ^{[3] [4]}

${\displaystyle e={\frac {V_{V}}{V_{S}}}={\frac {V_{V}}{V_{T}-V_{V}}}={\frac {n}{1-{\eta }}}}$

and

${\displaystyle {\eta }={\frac {V_{V}}{V_{T}}}={\frac {V_{V}}{V_{S}+V_{V}}}={\frac {e}{1+e}}}$

where ${\displaystyle e}$ is the void ratio, ${\displaystyle {\eta }}$ is the porosity, V_V is the volume of void-space (air and water), V_S is the volume of solids, and V_T is the total (or bulk) volume. ^[5]

Applications in soil sciences and geomechanics

• Control of the volume change tendency. Suppose the void ratio is high (loose soils). Under loading, voids in the soil skeleton tend to decrease (shrinkage), increasing the contact between adjacent particles and modifying the soil effective stress. The opposite situation, i. e. when the void ratio is relatively small (dense soils), indicates that the volume of the soil is vulnerable to increase (swelling) under unloading – the smectite (montmorillonite, bentonite) partially dry clay particles present in an unsaturated soil can swell due to their hydration after contact with water (when the saturated/unsaturated conditions fluctuate in a soil).
• Control of the fluid hydraulic conductivity (ability of water movement through the soil). Loose soils show a high hydraulic conductivity, while dense soils are less permeable.
• Particle movement. Small, unbound particles can move relatively quickly through the larger open voids in loose soil. In contrast, in dense soil, finer particles cannot freely pass the smaller pores, which leads to the clogging of the porosity.

See also

• Pore space in soil
• Void (composites)

References

1. Lambe, T. William & Robert V. Whitman. Soil Mechanics. Wiley, 1991; p. 29. ISBN   978-0-471-51192-2
2. Santamarina, J. Carlos, Katherine A. Klein, & Moheb A. Fam. Soils and Waves: Particulate Materials Behavior, Characterization and Process Monitoring. Wiley, 2001; pp. 35-36 & 51-53. ISBN   978-0-471-49058-6
3. Pearson, F. J. (1999). "What is the porosity of a mudrock? In: Aplin, A.C., Fleet, A.J. & Macquaker, J.H.S. (Ed.). Muds and mudstones: Physical and fluid flow properties". Geological Society, London, Special Publications. 158 (1): 9–21. doi:10.1144/GSL.SP.1999.158.01.02. ISSN   0305-8719.
4. Pearson, F. J.; Fernández, A. M.; Gaboriau, H.; Waber, H. N.; Bath, A. (2003). "Annex 10: Porosity and Water Content of Mont Terri Claystones. In: Mont Terri Project – Geochemistry of Water in the Opalinus Clay Formation at the Mont Terri Rock Laboratory" . Retrieved 2024-06-09.
5. Craig, R. F. Craig's Soil Mechanics. London: Spon, 2004, p.18. ISBN   0-203-49410-5.

Further reading

• Bates, R.L.; Jackson, J.A. (1987-10-15). Glossary of Geology, Third Edition – American Geological Institute, Alexandria. Amazon.com: Books 9780913312896. American Geological Institute. ISBN   0913312894.