Dispersion and Diffusion
Dispersion of solutes in flowing groundwater results in the spreading of a contaminant plume from highly concentrated areas to less concentrated areas. In many groundwater transport models, solute transport is described by the advectiondispersionreaction equation. The dispersion coefficient in this equation is the sum of the molecular diffusion coefficient, the mechanical dispersion coefficient and the macrodispersion effect.
Related Article(s):
CONTRIBUTOR(S):
Key Resource(s):
 Groundwater^{[1]}, Freeze and Cherry, 1979.
 Hydrogeologic Properties of Earth Materials and Principals of Groundwater Flow^{[2]}, Woessner and Poeter, 2020.
Molecular Diffusion
Molecular diffusion is the result of the thermal motion of individual molecules which causes a flux of dissolved solutes from areas of higher concentration to areas of lower concentration (Figure 1). The diffusion coefficient is a proportionality constant between the molar flux due to molecular diffusion and the concentration gradient and is a function of the temperature and molecular weight. In locations where advective flux is low (clayey aquitards and sedimentary rock), diffusion is often the dominant transport mechanism.
The diffusive flux J (M/L^{2}/T) in groundwater is calculated using Fick’s Law:

J = D_{e} dC/dx 

Where:  

is the effective diffusion coefficient and 

is the concentration gradient. 
The effective diffusion coefficient for transport through the porous media, D_{e}, is estimated as:

D_{e} = D_{m} n_{e} δ/Τ 

Where:  

is the diffusion coefficient of the solute in water, 

is the effective porosity (dimensionless), 

is the constrictivity (dimensionless) which reflects the restricted motion of particles in narrow pores^{[4]}, and 

is the tortuosity (dimensionless) which reflects the longer diffusion path in porous media around sediment particles^{[5]}. 
D_{m} is a function of the temperature, fluid viscosity and molecular weight. Values of D_{m} for common groundwater solutes are shown in Table 1.
Aqueous Diffusion Coefficient  Temperature (°C) 
D_{m} (cm^{2}/s) 
Reference 

Acetone  25  1.16x10^{5}  Cussler 1997 
Benzene  20  1.02x10^{5}  Bonoli and Witherspoon 1968 
Carbon dioxide  25  1.92x10^{5}  Cussler 1997 
Carbon tetrachloride  25  9.55x10^{6}  Yaws 1995 
Chloroform  25  1.08x10^{5}  Yaws 1995 
Dichloroethene  25  1.12x10^{5}  Yaws 1995 
1,4Dioxane  25  1.02x10^{5}  Yaws 1995 
Ethane  25  1.52x10^{5}  Witherspoon and Saraf 1965 
Ethylbenzene  20  8.10x10^{6}  Bonoli and Witherspoon 1968 
Ethene  25  1.87x10^{5}  Cussler 1997 
Helium  25  6.28x10^{5}  Cussler 1997 
Hydrogen  25  4.50x10^{5}  Cussler 1997 
Methane  25  1.88x10^{5}  Witherspoon and Saraf 1965 
Nitrogen  25  1.88x10^{5}  Cussler 1997 
Oxygen  25  2.10x10^{5}  Cussler 1997 
Perfluorooctanoic acid (PFOA)  20  4.80x10^{6}  Schaefer et al. 2019 
Perfluorooctane sulfonic acid (PFOS)  20  5.40x10^{6}  Schaefer et al. 2019 
Tetrachloroethene  25  8.99x10^{6}  Yaws 1995 
Toluene  20  8.50x10^{6}  Bonoli and Witherspoon 1968 
Trichloroethene  25  8.16x10^{6}  Rossi et al. 2015 
Vinyl chloride  25  1.34x10^{5}  Yaws 1995 
Mechanical Dispersion
Mechanical dispersion (hydrodynamic dispersion) results from groundwater moving at rates both greater and less than the average linear velocity. This is due to: 1) fluids moving faster through the center of the pores than along the edges, 2) fluids traveling shorter pathways and/or splitting or branching to the sides, and 3) fluids traveling faster through larger pores than through smaller pores^{[6]}. Because the invading solutecontaining water does not travel at the same velocity everywhere, mixing occurs along flow paths. This mixing is called mechanical dispersion and results in distribution of the solute at the advancing edge of flow. The mixing that occurs in the direction of flow is called longitudinal dispersion. Spreading normal to the direction of flow from splitting and branching out to the sides is called transverse dispersion (Figure 2).
Macrodispersion
Macrodispersion is the name given to the plume spreading caused by largescale aquifer heterogeneities and associated spatial variations in advective transport velocity. In some groundwater modeling projects, large values of the macrodispersion coefficient are used as an adjustment factor to help match the apparent largescale spreading of the plume^{[3]}. However, there is limited theoretical support for using large mechanical dispersion coefficients^{[7]}^{[8]}. In transmissive zones, macrodispersion coefficients are often orders of magnitude greater than molecular diffusion coefficients, leading some to conclude that molecular diffusion can be ignored.
Recently, an alternate conceptual model for describing largescale plume spreading in heterogeneous soils has been proposed^{[7]}^{[3]}^{[8]}. In this approach, solute transport in the transmissive zones is reasonably well described by the advectiondispersion equation using relatively small dispersion coefficients representing mechanical dispersion. However, overtime, molecular diffusion slowly transports solutes into lower permeability zones (Figure 3). As the transmissive zones are remediated, these solutes slowly diffuse back out, causing a long extended tail to the flushout curve. This process is controlled by diffusion and the presence of geologic heterogeneity with sharp contrasts between transmissive and low permeability media^{[9]} as discussed in the video shown in Figure 3.
References
 ^ Freeze, A., and Cherry, J., 1979. Groundwater, PrenticeHall, Englewood Cliffs, New Jersey, 604 pages. Free download from Hydrogeologists Without Borders.
 ^ Woessner, W.W., and Poeter, E.P., 2020. Properties of Earth Materials and Principals of Groundwater Flow, The Groundwater Project, Guelph, Ontario, 207 pages. Free download from The Groundwater Project.
 ^ ^{3.0} ^{3.1} ^{3.2} ITRC Integrated DNAPL Site Strategy Team, 2011. Integrated DNAPL Site Strategy. Technical/Regulatory Guidance Document, 209 pgs. Report pdf
 ^ Grathwohl, P., 1998. Diffusion in Natural Porous Media: Contaminant Transport, Sorption/Desorption and Dissolution Kinetics. Kluwer Academic Publishers, Boston. DOI: 10.1007/9781461556831 Available from: Springer.com
 ^ Carey, G.R., McBean, E.A. and Feenstra, S., 2016. Estimating Tortuosity Coefficients Based on Hydraulic Conductivity. Groundwater, 54(4), pp.476487. DOI:10.1111/gwat.12406 Available from: NGWA
 ^ Fetter, C.W., 1994. Applied Hydrogeology: Macmillan College Publishing Company. New York New York. ISBN13:9780130882394
 ^ ^{7.0} ^{7.1} Payne, F.C., Quinnan, J.A. and Potter, S.T., 2008. Remediation hydraulics. CRC Press. ISBN:9781420006841
 ^ ^{8.0} ^{8.1} Hadley, P.W. and Newell, C., 2014. The new potential for understanding groundwater contaminant transport. Groundwater, 52(2), pp.174186. doi:10.1111/gwat.12135
 ^ Sale, T.C., Illangasekare, T., Zimbron, J., Rodriguez, D., Wilkins, B. and Marinelli, F., 2007. AFCEE source zone initiative. Report Prepared for the Air Force Center for Environmental Excellence by Colorado State University and Colorado School of Mines. Report pdf
See Also
 International Water Management Institute Animations
 NAU Lecture Notes on Advective Transport
 MIT Open CourseWare Solute Transport: Advection with Dispersion Video
 Matrix Diffusion Webinar: Technical Challenges and Limitations to Site Closure
 Coursera Matrix Diffusion Online Lecture
 ESTCP Remediation and Matrix Diffusion Webinar
 Matrix Diffusion Movie
 Impact of ClayDNAPL Interactions on Transport and Storage of Chlorinated Solvents in Low Permeability Zones
 Basic Research Addressing Contaminants in Low Permeability Zones
 Prediction of Groundwater Quality Improvement DownGradient of In Situ Permeable Treatment Barriers and Fully Remediated Source Zones
 Determining Source Attenuation History to Support Closure by Natural Attenuation
 Decision Support System for Matrix Diffusion Modeling
 Online Lecture Course  Matrix Diffusion
 Matrix Diffusion Video