Darcy's law

Darcy's law is a constitutive equation that describes the flow of a fluid through a porous medium. The law was formulated by Henry Darcy based on the results of experiments^[1] on the flow of water through beds of sand, forming the basis of hydrogeology, a branch of earth sciences.

Background

Although Darcy's law (an expression of Newton's second law) was determined experimentally by Darcy, it has since been derived from the Navier-Stokes equations via homogenization.^[2] It is analogous to Fourier's law in the field of heat conduction, Ohm's law in the field of electrical networks, or Fick's law in diffusion theory.

One application of Darcy's law is to analyze water flow through an aquifer; Darcy's law along with the equation of conservation of mass are equivalent to the groundwater flow equation, one of the basic relationships of hydrogeology. Darcy's law is also used to describe oil, water, and gas flows through petroleum reservoirs.

Description

Diagram showing definitions and directions for Darcy's law.

Darcy's law, as refined by Morris Muskat, at constant elevation is a simple proportional relationship between the instantaneous discharge rate through a porous medium, the viscosity of the fluid and the pressure drop over a given distance.

Q=-{\frac {\kappa A\left(p_{\mathrm {b} }-p_{\mathrm {a} }\right)}{\mu L}}\,.

The total discharge, $Q$ (units of volume per time, e.g., m³/s) is equal to the product of the intrinsic permeability of the medium, $κ$ (m²), the cross-sectional area to flow, $A$ (units of area, e.g., m²), and the total pressure drop $p b - p a$ (pascals), all divided by the viscosity, $μ$ (Pa·s) and the length over which the pressure drop is taking place ( $L$ ). The negative sign is needed because fluid flows from high pressure to low pressure. Note that the elevation head must be taken into account if the inlet and outlet are at different elevations. If the change in pressure is negative (where $p a > p b$ ), then the flow will be in the positive $x$ direction. Dividing both sides of the equation by the area and using more general notation leads

q=-{\frac {\kappa }{\mu }}\nabla p\,,

where $q$ is the flux (discharge per unit area, with units of length per time, m/s) and $\nabla p$ is the pressure gradient vector (Pa/m). This value of flux, often referred to as the Darcy flux, is not the velocity which the fluid traveling through the pores is experiencing. The fluid velocity ( $v$ ) is related to the Darcy flux ( $q$ ) by the porosity ( $φ$ ). The flux is divided by porosity to account for the fact that only a fraction of the total formation volume is available for flow. The fluid velocity would be the velocity a conservative tracer would experience if carried by the fluid through the formation.

v={\frac {q}{\phi }}\,.

Darcy's law is a simple mathematical statement which neatly summarizes several familiar properties that groundwater flowing in aquifers exhibits, including:

if there is no pressure gradient over a distance, no flow occurs (these are hydrostatic conditions),
if there is a pressure gradient, flow will occur from high pressure towards low pressure (opposite the direction of increasing gradient — hence the negative sign in Darcy's law),
the greater the pressure gradient (through the same formation material), the greater the discharge rate, and
the discharge rate of fluid will often be different — through different formation materials (or even through the same material, in a different direction) — even if the same pressure gradient exists in both cases.

A graphical illustration of the use of the steady-state groundwater flow equation (based on Darcy's law and the conservation of mass) is in the construction of flownets, to quantify the amount of groundwater flowing under a dam.

Darcy's law is only valid for slow, viscous flow; fortunately, most groundwater flow cases fall in this category. Typically any flow with a Reynolds number less than one is clearly laminar, and it would be valid to apply Darcy's law. Experimental tests have shown that flow regimes with Reynolds numbers up to 10 may still be Darcian, as in the case of groundwater flow. The Reynolds number (a dimensionless parameter) for porous media flow is typically expressed as

\mathrm {Re} ={\frac {\rho vd_{30}}{\mu }}\,,

where $ρ$ is the density of water (units of mass per volume), $v$ is the specific discharge (not the pore velocity — with units of length per time), $d 30$ is a representative grain diameter for the porous media (often taken as the 30% passing size from a grain size analysis using sieves — with units of length), and $μ$ is the viscosity of the fluid.

Derivation

For stationary, creeping, incompressible flow, i.e. $D (ρu i) / Dt \approx 0$ , the Navier–Stokes equation simplifies to the Stokes equation:

\mu \nabla ^{2}u_{i}+\rho g_{i}-\partial _{i}p=0\,,

where $μ$ is the viscosity, $u i$ is the velocity in the $i$ direction, $g i$ is the gravity component in the $i$ direction and $p$ is the pressure. Assuming the viscous resisting force is linear with the velocity we may write:

-\left(\kappa _{ij}\right)^{-1}\mu \phi u_{j}+\rho g_{i}-\partial _{i}p=0\,,

where $φ$ is the porosity, and $κ ij$ is the second order permeability tensor. This gives the velocity in the $n$ direction,

\kappa _{ni}\left(\kappa _{ij}\right)^{-1}u_{j}=\delta _{nj}u_{j}=u_{n}=-{\frac {\kappa _{ni}}{\phi \mu }}\left(\partial _{i}p-\rho g_{i}\right)\,,

which gives Darcy's law for the volumetric flux density in the $n$ direction,

q_{n}=-{\frac {\kappa _{ni}}{\mu }}\left(\partial _{i}p-\rho g_{i}\right)\,.

In isotropic porous media the off-diagonal elements in the permeability tensor are zero, $κ ij = 0$ for $i \neq j$ and the diagonal elements are identical, $κ ii = κ$ , and the common form is obtained

{\boldsymbol {q}}=-{\frac {\kappa }{\mu }}\left({\boldsymbol {\nabla }}p-\rho {\boldsymbol {g}}\right)\,.

Additional forms of Darcy's law

Darcy's law for short time scales

For very short time scales, a time derivative of flux may be added to Darcy's law, which results in valid solutions at very small times (in heat transfer, this is called the modified form of Fourier's law),

\tau {\frac {\partial q}{\partial t}}+q=-\kappa \nabla h\,,

where $τ$ is a very small time constant which causes this equation to reduce to the normal form of Darcy's law at "normal" times (> nanoseconds). The main reason for doing this is that the regular groundwater flow equation (diffusion equation) leads to singularities at constant head boundaries at very small times. This form is more mathematically rigorous, but leads to a hyperbolic groundwater flow equation, which is more difficult to solve and is only useful at very small times, typically out of the realm of practical use.

Brinkman form of Darcy's law

Another extension to the traditional form of Darcy's law is the Brinkman term, which is used to account for transitional flow between boundaries (introduced by Brinkman in 1949^[3]),

\beta \nabla ^{2}q+q=-{\frac {\kappa }{\mu }}\nabla p\,,

where $β$ is an effective viscosity term. This correction term accounts for flow through medium where the grains of the media are porous themselves, but is difficult to use, and is typically neglected.

Darcy's law in petroleum engineering

Another derivation of Darcy's law is used extensively in petroleum engineering to determine the flow through permeable media — the most simple of which is for a one-dimensional, homogeneous rock formation with a fluid of constant viscosity.

Q={\frac {\kappa A}{\mu }}\left({\frac {\partial p}{\partial x}}\right)\,,

where $Q$ is the flowrate of the formation (in units of volume per unit time), $k$ is the permeability of the formation (typically in millidarcys), $A$ is the cross-sectional area of the formation, $μ$ is the viscosity of the fluid (typically in units of centipoise). $\partial p / \partial x$ represents the pressure change per unit length of the formation. This equation can also be solved for permeability and is used to measure it, forcing a fluid of known viscosity through a core of a known length and area, and measuring the pressure drop across the length of the core.

Darcy–Forchheimer law

For flows in porous media with Reynolds numbers greater than about 1 to 10, inertial effects can also become significant. Sometimes an inertial term is added to the Darcy's equation, known as Forchheimer term. This term is able to account for the non-linear behavior of the pressure difference vs flow data.^[4]

{\frac {\partial p}{\partial x}}=-{\frac {\mu }{\kappa }}q-{\frac {\rho }{\kappa _{1}}}q^{2}\,,

where the additional term $κ 1$ is known as inertial permeability.

Darcy's law for gases in fine media (Knudsen diffusion or Klinkenberg effect)

For gas flow in small characteristic dimensions (e.g., very fine sand, nanoporous structures etc.), the particle-wall interactions become more frequent, giving rise to additional wall friction (Knudsen friction). For a flow in this region, where both viscous and Knudsen friction are present, a new formulation needs to be used. Knudsen presented a semi-empirical model for flow in transition regime based on his experiments on small capillaries.^[5]^[6] For a porous medium, the Knudsen equation can be given as ^[6]

N=-\left({\frac {\kappa }{\mu }}{\frac {p_{a}+p_{b}}{2}}+D_{\mathrm {K} }^{\mathrm {eff} }\right){\frac {1}{R_{\mathrm {g} }T}}{\frac {p_{\mathrm {b} }-p_{\mathrm {a} }}{L}}\,,

where $N$ is the molar flux, $R g$ is the gas constant, $T$ is the temperature, $D eff K$ is the effective Knudsen diffusivity of the porous media. The model can also be derived from the first-principle-based binary friction model (BFM).^[7]^[8] The differential equation of transition flow in porous media based on BFM is given as^[7]

{\frac {\partial p}{\partial x}}=-R_{\mathrm {g} }T\left({\frac {\kappa p}{\mu }}+D_{\mathrm {K} }\right)^{-1}N\,.

This equation is valid for capillaries as well as porous media. The terminology of the Knudsen effect and Knudsen diffusivity is more common in mechanical and chemical engineering. In geological and petrochemical engineering, this effect is known as the Klinkenberg effect. Using the definition of molar flux, the above equation can be rewritten as

{\frac {\partial p}{\partial x}}=-R_{\mathrm {g} }T\left({\frac {\kappa p}{\mu }}+D_{\mathrm {K} }\right)^{-1}{\dfrac {p}{R_{\mathrm {g} }T}}q\,.

This equation can be rearranged into the following equation

q=-{\frac {\kappa }{\mu }}\left(1+{\frac {D_{\mathrm {K} }\mu }{\kappa }}{\frac {1}{p}}\right){\frac {\partial p}{\partial x}}\,.

Comparing this equation with conventional Darcy's law, a new formulation can be given as

q=-{\frac {\kappa ^{\mathrm {eff} }}{\mu }}{\frac {\partial p}{\partial x}}\,,

where

\kappa ^{\mathrm {eff} }=\kappa \left(1+{\frac {D_{\mathrm {K} }\mu }{\kappa }}{\frac {1}{p}}\right)\,.

This is equivalent to the effective permeability formulation proposed by Klinkenberg:^[9]

\kappa ^{\mathrm {eff} }=\kappa \left(1+{\frac {b}{p}}\right)\,.

where $b$ is known as the Klinkenberg parameter, which depends on the gas and the porous medium structure. This is quite evident if we compare the above formulations. The Klinkenberg parameter $b$ is dependent on permeability, Knudsen diffusivity and viscosity (i.e., both gas and porous medium properties).

Validity of Darcy's law

Darcy's law is valid for laminar flow through sediments. In fine-grained sediments, the dimensions of interstices are small and thus flow is laminar. Coarse-grained sediments also behave similarly but in very coarse-grained sediments the flow may be turbulent.^[10] Hence Darcy's law is not always valid in such sediments. For flow through commercial pipes, the flow is laminar when Reynolds number is less than 2000, but in some sediments it has been found that flow is laminar when the value of Reynolds number is less than 1.^[11]

References

↑ Darcy, H. (1856). Les fontaines publiques de la ville de Dijon. Paris: Dalmont.
↑ Whitaker, S. (1986). "Flow in porous media I: A theoretical derivation of Darcy's law". Transport in Porous Media. 1: 3–25. doi:10.1007/BF01036523.
↑ Brinkman, H. C. (1949). "A calculation of the viscous force exerted by a flowing fluid on a dense swarm of particles". Applied Scientific Research. 1: 27–34. doi:10.1007/BF02120313.
↑ Bejan, A. (1984). Convection Heat Transfer. John Wiley & Sons.
↑ Cunningham, R. E.; Williams, R. J. J. (1980). Diffusion in Gases and Porous Media. New York: Plenum Press.
1 2 Carrigy, N.; Pant, L. M.; Mitra, S. K.; Secanell, M. (2013). "Knudsen diffusivity and permeability of pemfc microporous coated gas diffusion layers for different polytetrafluoroethylene loadings". Journal of the Electrochemical Society. 160: F81–89. doi:10.1149/2.036302jes.
1 2 Pant, L. M.; Mitra, S. K.; Secanell, M. (2012). "Absolute permeability and Knudsen diffusivity measurements in PEMFC gas diffusion layers and micro porous layers". Journal of Power Sources. 206: 153–160. doi:10.1016/j.jpowsour.2012.01.099.
↑ Kerkhof, P. (1996). "A modified Maxwell-Stefan model for transport through inert membranes: The binary friction model". Chemical Engineering Journal and the Biochemical Engineering Journal. 64: 319–343. doi:10.1016/S0923-0467(96)03134-X.
↑ Klinkenberg, L. J. (1941). "The permeability of porous media to liquids and gases". Drilling and Production Practice. American Petroleum Institute. pp. 200–213.
↑ Jin, Y.; Uth, M.-F.; Kuznetsov, A. V.; Herwig, H. (2 February 2015). "Numerical investigation of the possibility of macroscopic turbulence in porous media: a direct numerical simulation study". Journal of Fluid Mechanics. 766: 76–103. Bibcode:2015JFM...766...76J. doi:10.1017/jfm.2015.9.
↑ Arora, K. R. (1989). Soil Mechanics and Foundation Engineering. Standard Publishers.

This article is issued from Wikipedia - version of the 12/1/2016. The text is available under the Creative Commons Attribution/Share Alike but additional terms may apply for the media files.