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The void volume within a porous medium. Porosity is its fraction of bulk volume; saturation specifies which fluids occupy that void volume.

Pore velocity is the fluid velocity averaged over pore volume relative to the solid framework. For uniform porosity $\varphi$, full saturation and all pores participating, $\mathbf{v}=\mathbf{q}/\varphi$, with Darcy velocity $\mathbf{q}$ defined per bulk area. The identity follows from volume averaging: extending the relative fluid velocity by zero in the solid gives a bulk average equal to the pore fraction times the pore-volume average. It does not assert that every local passage has open area $\varphi A$ or identical speed.

In a uniform advective model, travel over length $L$ takes $L/v=\varphi L/q$. If some pore volume is inaccessible to transport, the corresponding estimate uses effective porosity ${\varphi }_e$ and $v=q/{\varphi }_e$. A connected but nearly stagnant passage can exchange solute slowly, so even this mean does not describe all arrival times. Flux-weighted residence time in a porous layer explains one precise averaging convention.^[ref]

Porosity is the fraction of a representative bulk material volume occupied by voids:It is dimensionless and measures storage space. A sample with bulk volume $1.0\mathrm{L}$ and pore volume $0.25\mathrm{L}$ has porosity $\varphi =0.25=25\%$. If all its pores are saturated by one liquid, the liquid occupies $0.25\mathrm{L}$; partial fluid saturation $s$ instead gives liquid volume $s\varphi V_{\mathrm{bulk}}$.

Porosity and permeability of a porous medium answer different questions: how much fluid fits, and how easily it flows. Isolated bubbles or cavities can contribute to total porosity while providing no throughgoing path. Even connected passages may be narrow enough to transmit very little discharge. In the simple fully participating saturated model, Darcy velocity is $\varphi$ times pore velocity; changing porosity at a stipulated fixed Darcy flux changes ideal advective travel time, but porosity alone cannot predict the Darcy flux.

A shallow buoyant porous gravity current in a deep aquifer with uniform imposed Darcy velocity $U$ obeys $\varphi h_t+(Uh-K_{b}h{h}_x{)}_x=0$ away from sources, where $K_b=k\Delta \rho g/\mu$. Here $k$ is permeability of a porous medium, $\varphi$ is porosity, and $\mu$ is dynamic viscosity. The pore-fluid drift speed is $u=U/\varphi$, and the gravity diffusion coefficient multiplying $(h{h}_x{)}_x$ is $a=K_b/\varphi$. The sharp-interface model neglects capillary trapping and dissolution.

Porous-media flow is fluid motion through the interconnected voids of a porous medium, such as a sand bed, a rock or a filter. Individual passages can be tiny and tortuous, yet their combined discharge can be predicted without resolving every passage. Darcy law supplies this bulk description when viscous resistance dominates pore-scale inertia; porosity measures how much space stores fluid, while permeability of a porous medium measures how readily that space transmits it.

The basic fully saturated model assumes one Newtonian fluid fills the connected pore space of a stationary solid framework, with incompressible flow, a small pore-scale Reynolds number, and averaging volumes large compared with individual pores but small compared with macroscopic variations. These are assumptions of the model developed below, rather than a claim that Darcy law describes every porous-media flow. Two-phase porous-media flow and poroelastic aquifers require additional constitutive and storage information.

For a first calculation, see Darcy flow through a homogeneous slab: a pressure drop determines the discharge, but porosity determines the corresponding pore velocity. Layered porous permeability then shows how geometry alone can make the bulk response anisotropic.

A porous medium is a solid framework containing connected voids in which a fluid can reside and flow. Its porosity is the void fraction; its permeability of a porous medium measures the ease of pressure-driven flow through the connected pores. The averaged Darcy flux is measured per total cross-sectional area, whereas the pore velocity is that flux divided by porosity. Not every material with voids has connected permeable pores.

A growing ice-filled sphere expels liquid because ice is less dense than water. With porosity $\varphi$, $ϵ=1-{\rho }_s/\rho$, and pressure-induced freezing-point depression $T_i=T_m-\gamma p_i$, the Darcy velocity gives $p_i=\mu \varphi ϵa\dot{a}/\Pi$. Quasi-steady spherical thermal conduction gives $\varphi {\rho }_{s}La\dot{a}=k(T_i-T_{\infty })$. Hence $a\dot{a}=k(T_m-T_{\infty })/[\varphi {\rho }_{s}L(1+\Lambda )]$, where $\Lambda =k\gamma \mu ϵ/(\Pi {\rho }_{s}L)$. The interface approaches the far-field temperature at low permeability of a porous medium, while its pressure tends to a finite equilibrium value.

Without transverse exchange, a particle chosen uniformly from pore volume samples each streamline's transit time with resident-volume weight. This differs from the flux-weighted residence time in a porous layer, which samples at the inlet proportionally to $v$. For constant porosity and a linear positive velocity $v=v_0+(v_1-v_0)y/H$, the two means are $L\log (v_1/v_0)/(v_1-v_0)$ and $2L/(v_0+v_1)$, respectively. Their limits agree for uniform velocity.

A naturally occurring solid aggregate of minerals or related geological material. Its composition, porosity, cracks and fluid content affect seismic wave speeds and magnetic susceptibility.

A sedimentary rock composed predominantly of sand-sized grains. Cementation, porosity, pore fluid and effective stress strongly affect its seismic velocity.

With permeability of a porous medium $k(z)=k_0(1+\beta z)$, the Dupuit approximation givesHere $\varphi$ is porosity and $R$ is recharge. The low-height limit has mobility proportional to $h$, whereas large heights have mobility proportional to $h^2$. This changes both the forced filling similarity for power-law diffusion and the separable draining profile for power-law diffusion.

With constant porosity $P$ and $X=x\tan \theta$, $Y=y\tan \theta$, a translating frame $\xi =X-T$, $\eta =Y$ has area Jacobian determinant $dxdy={\cot }^2\theta d\xi d\eta$. Actual fluid volume is $P\iint hdxdy$, proving the displayed normalization. Replacing the cotangent factor by a tangent factor is incompatible with these coordinates except at a slope of $\pi /4$.