By Richard W. Healy, Bridget R. Scanlon
Figuring out groundwater recharge is key for profitable administration of water assets and modeling fluid and contaminant delivery in the subsurface. This publication presents a severe evaluate of the speculation and assumptions that underlie tools for estimating charges of groundwater recharge. distinct causes of the tools are supplied - permitting readers to use a few of the strategies themselves with no need to refer to extra references. a number of sensible examples spotlight advantages and obstacles of every technique. nearly 900 references let complex practitioners to pursue more information on any procedure. For the 1st time, theoretical and functional concerns for choosing and utilizing tools for estimating groundwater recharge are lined in one quantity with uniform presentation. Hydrogeologists, water-resource experts, civil and agricultural engineers, earth and environmental scientists and agronomists will reap the benefits of this informative and useful publication. it could function the first textual content for a graduate-level path on groundwater recharge or as an accessory textual content for classes on groundwater hydrology or hydrogeology. For the advantage of scholars and teachers, challenge units of various trouble can be found at http://wwwbrr.cr.usgs.gov/projects/GW_Unsat/Recharge_Book/.
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Additional resources for Estimating Groundwater Recharge
Example text
4 Surface flow Estimates of surface-water flow may be needed in recharge studies for predicting direct runoff in the absence of any streamflow gauges or data. A common technique for predicting direct runoff is the US Soil Conservation Service curve number method (Natural Resources Conservation Service, 2004). The dimensionless curve number, CN, is determined on the basis of soil type, land use, and antecedent soil-water content. 37) where P is precipitation (in inches) and S = 1000 / CN – 10. 37) appear in the literature (Garen and Moore, 2005a, b).
When high wind carries warm dry air, and hence energy, into the study area). 32) where s is the slope of the water vapor saturation curve, γ is the psychrometric constant, and Ea is a function of wind speed and water vapor pressure deficit that has taken several forms. 33) where U is the windrun in km/d at a 2 m height and es and ea are saturated and actual vapor pressure, respectively, expressed in kPa. Monteith (1963) modified the Penman equation for vegetated areas to account for the fact that specific humidity at leaf surfaces is usually less than saturation.
2009) made no attempt to do so. Geostatistical techniques such as kriging can account for both measurement error and spatial variability of water-budget components (Journel and Huijbregts, 1978). These techniques are discussed in Chapter 3. Informal, empirical approaches to water budget uncertainty analyses are relatively easy to apply and can provide useful information. A common approach is to assume that the measured value of a component is equal to the true value plus some value of uncertainty.