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minutes of strolling around a given stream reach, you should have been able to identify the cool spots in the water at the streambed corresponding to localized zones of groundwater discharge On large scales, similar surveys can be made using thermometers trailed from boats, or even by airborne thermal imaging If you can t wait until summer to identify groundwater discharge zones, you can always take a walk on a cold winter s day and identify groundwater discharge zones from the occurrence of unfrozen patches (sometimes emitting steam into the frosty air) along otherwise icedup stream channels Airborne visual surveys can also be useful under such winter conditions At the next level of sophistication, it is possible to quantify groundwater discharge rates by making a series of spot gagings (ie one-off measurements) of stream ow at a number of points along a channel (eg Pettyjohn 1985a).

The increase in ow between each gaging point and its downstream neighbor is called the transmission gain (GT), and it is calculated by subtracting the upstream ow (Qu) from the downstream ow (Qd) In the absence of stream tributary in ows or arti cial discharges, GT simply equals the amount of groundwater entering the channel between the two points If the transmission gain is divided by the distance between the two measurement points, a speci c gain value is obtained, typically in units of m3/s per km length of stream channel Alternatively, speci c gain can be de ned as the transmission gain divided by the area of the streambed (As) between the two stations, so that the value obtained will be in units of m3/s per m2 of streambed (or similar).

You can add more than one light to your file by clicking the Light icon at the bottom of the preview pane. You can also take advantage of some of the presets by choosing one from the Style drop-down menu. You can see three examples of these presets in Figure 14.29. You can also save your own light settings as a style.

(As can be readily estimated by multiplying the distance between neighboring gauging points by the average channel width in that reach) If observation boreholes are present in the adjoining aquifer, so that the gradient (i) of the water table towards the river can be determined, then it is even possible to estimate the mean transmissivity (T) of that aquifer using the following simple formula, derived from Darcy s Law: T = GT / (i As) (51).

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