Groundwater Contaminant Transport Modeling

Introduction Back to Calculation

This groundwater transport calculation simulates one-dimensional (x-direction) transport of a chemical in a confined groundwater aquifer. It is also valid for transport in an unconfined aquifer if the groundwater head gradient (dh/dx) is nearly constant. There are two common boundary conditions for chemical transport: One is a step (i.e. continuous) injection of chemical - the chemical is added at x=0 from time t=0 to t=T. The other common boundary condition is a pulse input where a mass of chemical is added instantaneously at x=0. This groundwater modeling uses the first boundary condition though a pulse input can be simulated by using a short injection time T. The modeling solves for concentration at whatever time and distance is desired by the user.

The groundwater transport calculator includes advection, dispersion, and retardation. Advection is chemical movement via groundwater flow due to the groundwater hydraulic (i.e. head) gradient. Dispersion is the longitudinal (forward and backward) spreading of the contaminant in groundwater. If there were no dispersion, all of the contaminant would travel at the mean chemical velocity. With dispersion, some chemical travels faster and some slower than the mean velocity; the chemical "spreads out." Retardation causes the mean chemical velocity to be slower than the groundwater velocity. If your chemical exhibits no dispersion, set both the dispersivity (a) and diffusion coefficient (D*) to zero. If the chemical is not retarded, then uncheck the retardation check box or use the chemical drop-down menu to select "User enters K_oc" and set K_oc =0.0.

Equations Back to Calculation

Governing Equation and Boundary Conditions
The governing equation for one-dimensional chemical transport in groundwater with advection, dispersion, and retardation is (Van Genuchten and Alves, 1982):

Solution
The solution to the groundwater contaminant transport modeling governing equation and boundary conditions shown above is (Van Genuchten and Alves, 1982):

erfc( ) is called the "complementary error function."  Our groundwater calculation uses the most accurate numerical representation of erfc( ) given in Abramowitz and Stegun (1972, eqn 7.1.26).

Applications Back to Calculation

The following graphs were developed to demonstrate effects of dispersion for trichloroethylene (TCE) in a sandy groundwater aquifer as predicted by the groundwater calculation. The following data were used:
C_o = 10,000 mg/l, d = 1.6 g/cm³, dh/dx = -0.007 m/m, D* = 0,   f_oc = 0.1%,
K = 0.001 cm/s,  K_oc = 100 cm³/g, n = 35%, n_e = 25%.     Click for groundwater variable definitions
Therefore, K_d = 0.1 cm³/g,  R_f  = 1.46,   V_w = 2.8x10^-7 m/s,  and V_c = 1.92x10^-7 m/s.

Two injection durations were used:  T=1,000,000 days in Figure 1 and T=100 days in Figure 2.  For Figure 1, T was selected large enough to simulate an infinite duration injection.  In both figures, the concentration front occurs at  x = V_c t = 16.6 m  when  a=0.   In Figure 2, the trailing edge of the concentration front occurs at  x = V_c( t-T) =14.9 m  when a=0.   a is dispersivity.

Figure 1.  TCE concentration profile at 1000 days for an injection of duration 1,000,000 days

Figure 2.  TCE concentration profile at 1000 days for an injection of duration 100 days.

Variables Back to Calculation

The variables used in the groundwater modeling are:
a = dispersivity [L]. Varies from 0.1 to 100 m. Field and laboratory tests have indicated that a varies with the scale of the test. Large scale groundwater tests have higher a than small lab column tests. An approximate value for a is 0.1 times the scale of your groundwater system (Fetter, 1993). If you are simulating groundwater contaminant transport in a 1 m long laboratory column, then a~0.1 m. However, if you are simulating groundwater transport in a large aquifer greater than 1 km in extent, then use a~100 m.
C = Chemical concentration [M/L³].
C_o = Injected concentration at x=0 [M/L³].
d = Dry bulk density of the groundwater aquifer [M/L³].
dh/dx = Groundwater hydraulic (or head) gradient [L/L]. Since dh/dx is negative, we ask you to enter -dh/dx so that you can enter a positive number for convenience. You determine dh/dx from two head measurements using the equation, dh/dx = (h₂-h₁)/(x₂-x₁).
D = Dispersion coefficient [L²/T]. The equation D=a V_c + D*/n_e is adapted from Ingebritsen and Sanford (1998).
D* = Molecular diffusion coefficient [L²/T]. Varies somewhat for different chemicals but a typical value to use is 1.0x10^-9 m²/s (Fetter, 1993).
f_oc = Organic carbon fraction in soil [%]. (Mass organic carbon per mass soil) x 100%.
K = Hydraulic conductivity of aquifer [L/T].
K_d = Distribution coefficient [L³/M]. Represents chemical partitioning between groundwater and soil.
K_oc = Organic carbon partition coefficient [L³/M]. Represents chemical partitioning between organic carbon and water in soil. Good discussion in Lyman et al. (1982).
n = Total porosity of soil [%]. (Void volume/total volume) x 100%.
n_e = Effective porosity [%]. Porosity through which flow can occur. A thin film of water bound to soil particles by capillary forces does not move through the groundwater aquifer. n_e is always ≤ n.
Pe = Peclet number. Pe=(V_c x ) / D. It is a commonly used dimensionless parameter indicating the relative impact of inertial effects to dispersive effects.
R_f = Retardation factor. R_f =1 if there is no retardation which implies that V_c=V_w. R_f =1 would occur for a conservative tracer; that is, a tracer that does not sorb to the aquifer soil.
t = Time [T]. Time at which C is to be computed.
T = Duration of injection [T]. C_o is injected from t=0 to t=T.
V_c = Mean chemical velocity [L/T].
V_w = Pore water velocity [L/T]. Also known as groundwater velocity.
x = Distance [L]. Distance at which to compute C.

Property Data Back to Calculation

The following are tables of groundwater hydraulic conductivity, total porosity, effective porosity, bulk density, and organic carbon partition coefficient. Groundwater parameter values have been compiled from a variety of sources such as Coduto (1994), Fetter (1993), Freeze and Cherry (1979), Hillel (1982), and Sanders (1998). The values used in the groundwater contaminant transport modeling are typical numbers within the ranges given below.

Table of Soil Properties

Table of Organic Carbon Partition Coefficient, K_oc

Errors Messages Back to Calculation

"Certain inputs must be > 0."  No groundwater computations. C_o , C, d, -dh/dx, K, n, n_e, and T must all be > 0 if entered.

"Certain inputs must be ≥ 0."  No groundwater computations. a, D*, f_oc , K_oc, t, and x must all be ≥ 0 if entered.

"n, n_e , and f_oc must be ≤ 100%."  No groundwater computations. Total porosity, effective porosity, and soil organic carbon cannot exceed 100%.

"n_e must be ≤ n." No groundwater computations. Effective porosity cannot exceed total porosity.

"C_o cannot be determined" or "C_o=∞." C_o not computed. Certain input combinations result in computing erfc(∞), and erfc(∞)=0.0. Therefore, C_o cannot be evaluated or is evaluated as infinity.

"erfc(x,t)=0. Cannot compute C_o", "efrc(x,t-T)=0. Cannot compute C_o", "A(x,t)=0. Cannot compute C_o", or "A(x,t)-A(x,t-T)=0. Cannot compute C_o."   C_o not computed since division by zero occurs.

References Back to Calculation

Abramowitz, M. and I. A. Stegun. 1972. Handbook of Mathematical Functions. Dover Publications, Inc.

Coduto, D. P. 1994. Foundation Design Principles and Practices. Prentice Hall, Inc.

Fetter, C. W. 1993. Contaminant Hydrogeology. Macmillan Pub. Co.

Freeze, R. A. and J. A. Cherry. 1979. Groundwater. Prentice Hall, Inc.

Hillel, D. H. 1982. Introduction to Soil Physics. Academic Press, Inc.

Ingebritsen, S. E. and W. E. Sanford. 1998. Groundwater in Geologic Processes. Cambridge University Press.

Lyman, W. J. Adsorption coefficient for soils and sediments. In Handbook of Chemical Property Estimation Methods. Lyman, W. J., W. F. Reehl, and D. H. Rosenblatt, eds. McGraw-Hill Book Co. 1982. pp. 4-1 thru 4-33.

Sanders, L. L. 1998. A Manual of Field Hydrogeology. Prentice Hall, Inc..

Van Genuchten, M. Th. and W. J. Alves. 1982. Analytical Solutions of the One-Dimensional Convective-Dispersive Solute Transport Equation. United States Department of Agriculture, Agricultural Research Service, Technical Bulletin 1661.