Wiley M.J., Kohler S.L., and P.W. Seelbach. 1997. Reconciling landscape and local views of aquatic communities: lessons from Michigan Trout Streams. Freshwater Biology 37:133-148.
Please contact Dr. Matthew Baker or Dr. Mike Wiley (at the University of Michigan, School of Natural Resources and Environment 430 East University Ann Arbor, MI 48109-1115) or Dr. Paul Seelbach (Institute for Fisheries Research, 212 Museums Annex Building, 1109 North University Ave., Ann Arbor, MI 48109-1084) for additional information on this Darcy Model.
Wiley M.J., Kohler S.L., and P.W. Seelbach. 1997. Reconciling landscape and local views of aquatic communities: lessons from Michigan Trout Streams. Freshwater Biology 37:133-148.
This document explains the development of the various Darcy Models.
Interpreted from the following sources:
Bedient, P.B. and Huber, W.C. 1989. Hydrology and Floodplain Analysis. Addison-Wesley Publishing. Reading, Massachusetts.
Davis, S.N. and DeWiest, R.J. 1966. Hydrogeology. John Wiley and Sons. New York, New York.
Dorr, J.A. and Eschmann, D.F. 1990. The Geology of Michigan. University of Michigan, Ann Arbor.
Dunn, T. and Leopold, L.B. 1978. Water in environmental planning. W.H. Freeman and Co., New York.
Freeze, R.A. and Cherry, J.A. 1979. Groundwater. Prentice-Hall, Inc. Englewood Cliffs, New Jersey.
Todd, D.K. 1976. Groundwater Hydrology. John Wiley and Sons. New York, New York.
Farrand, W.R. and D.L. Bell. 1982. Quaternary Geology of Michigan. State of Michigan Department of Natural Resources, Geological Survey, Map (color).
This model employed a simple neighborhood filter ("buffer algorithm"). Differences between each target DEM cell elevation and the maximum DEM elevation in a circular "buffer" with a 4-km radius were noted as hydraulic slope. These elevation differentials were dividied by the buffer radius for head estimates and multiplied by the conductivity value of each cell. The value of the resulting target pixel represents an estimate of potential groundwater velocity for fluxes from adjacent uplands to the surface of that target cell.
Four-kilometer neighborhoods were used because they represented the greatest distance in a series of observed associations between known major seepage areas and adjacent topographic relief. This model did not incorporate actual water table elevations; DEM neighborhood information was used as a surrogate for maximum proximate water table elevation relative to the focal surface elevation because it was determined that surface topography averaged over broad landscapes provided a constraint on maximum potential flow.
Model output was computed as a velocity value (m day-1) for each 100 m2 grid cell across Lower Michigan. Please refer to the document included in the citation information which contains much greater detail.