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cm=centimeter, ft=foot, g=gram, gal=U.S. gallon, hr=hour, kg=kilogram, km=kilometer, l=liter, lb=pound, m=meter, mg=milligram, min=minute, mm=millimeter, ppm=part per million (by mass), ppb=part per billion (by mass), s=second, yr=year, ug=microgram
Groundwater topics on this page: Introduction Equations
Definitions Property Data Error Messages References
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This groundwater 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 calculator uses the first boundary condition
though a pulse input can be simulated by using a short injection time T.
The calculator solves for concentration at whatever time and distance is desired by the
The groundwater calculation 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 Koc"
and set Koc =0.0.
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Groundwater 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):
The solution to the 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).
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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:
Co = 10,000 mg/l, d = 1.6 g/cm3, dh/dx = -0.007 m/m, D* =
0, foc = 0.1%,
K = 0.001 cm/s, Koc = 100 cm3/g, n = 35%, ne = 25%.
Click for groundwater variable definitions
Therefore, Kd = 0.1 cm3/g, Rf = 1.46,
Vw = 2.8x10-7 m/s, and Vc = 1.92x10-7
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 = Vc t = 16.6 m when a=0.
In Figure 2, the trailing edge of the concentration front occurs at x = Vc(
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.
Groundwater Variable Definitions Units: [L]=Length, [M]=Mass, [T]=Time
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The variables used in the groundwater calculator 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].
Co = 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 Vc + D*/ne is adapted from Ingebritsen and Sanford
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).
foc = Organic carbon fraction in soil [%].
(Mass organic carbon per mass soil) x 100%.
K = Hydraulic conductivity of aquifer [L/T].
Kd = Distribution coefficient [L3/M].
Represents chemical partitioning between groundwater and soil.
Koc = 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)
ne = 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. ne is always ≤ n.
Pe = Peclet number. Pe=(Vc x ) / D.
It is a commonly used dimensionless parameter indicating the relative impact of inertial
effects to dispersive effects.
Rf = Retardation factor. Rf
=1 if there is no retardation which implies that Vc=Vw.
Rf =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]. Co is
injected from t=0 to t=T.
Vc = Mean chemical velocity [L/T].
Vw = Pore water velocity [L/T]. Also known as
x = Distance [L]. Distance at which to compute C.
Groundwater Property Data
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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 calculation above are typical numbers within the ranges given below.
Table of Soil Properties
||10-9 - 10-6
||10-7 - 10-3
||10-5 - 10-1
||10-1 - 102
Table of Organic Carbon Partition Coefficient, Koc
Error Messages given by groundwater calculation
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"Certain inputs must be > 0." No
groundwater computations. Co , C, d, -dh/dx, K, n, ne, and T
must all be > 0 if entered.
"Certain inputs must be ≥ 0." No
groundwater computations. a, D*, foc , Koc, t,
and x must all be ≥ 0 if entered.
"n, ne , and foc must be ≤ 100%."
No groundwater computations. Total porosity, effective porosity, and soil organic carbon cannot
"ne must be ≤ n." No
groundwater computations. Effective porosity cannot exceed total porosity.
"Co cannot be determined" or
"Co=∞." Co not
computed. Certain input combinations result in computing erfc(∞), and
erfc(∞)=0.0. Therefore, Co cannot be evaluated or is evaluated as infinity.
"erfc(x,t)=0. Cannot compute Co",
"efrc(x,t-T)=0. Cannot compute Co",
"A(x,t)=0. Cannot compute Co", or
"A(x,t)-A(x,t-T)=0. Cannot compute Co."
Co not computed since division by zero occurs.
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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,
Hillel, D. H. 1982. Introduction to Soil Physics. Academic Press,
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,
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.
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Software, Ltd. All rights reserved.
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LMNO Engineering home page (more calculations)
3-D Slug injection with advection and dispersion
Compute gradient from well head measurements
Drawdown for unsteady groundwater flow to pumping well in confined aquifer (Theis calculator)
Transmissivity T=Kb (and K table)