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<br />. <br /> <br />l\.) <br />..... <br />co <br />l\) <br /> <br />of the =axioum recoverable ground water reserves in the Region. <br />The rich alluvial aquifers, on the other hand, store only about <br />5 pe=cent of the reserves. Three-fourths of the Region (again, <br />those areas of sedimentary deposition) have a potential well yield <br />of 5 to 50 gpm. Most of the remaining aquifers yield 1 to 10 gpm <br />to walls (Price and Arnow, 1974). <br /> <br />UPPER ~E~ RIVER BASIN (WAU 140401) <br /> <br />Ground water in the Upper Green River Basin (Fig. D.3) is recharged <br />primarily by runoff from the Wind River, Gros Ventre, Uinta, and Wyo- <br />mi~g ~unt3in ranges and by seepage from reservoirs. Ground water is <br />dischar~ed by evaporation, seepage to streams and lakes, transpiration, <br />and vall withdravals. Potential evaporation in the southern part of <br />the basin is up to 10 times greater than annual precipitation, so <br />virtually none of the moisture falling outside of the mountainous <br />areas Haches the ground vater aquifer (lIelder, 1968). As in all <br />aquifer srste~, the rate of recharge decreases as distance from areas <br />of re?leoishment increases. <br /> <br />. <br /> <br />~5t of the grol1~d water in .the Upper Green River Basin is con- <br />fined (~elder, 1968). Artesian formations here are generally pre- <br />Oligoce~e in age. The depth of confined aquifers is generally less <br />than 20J feet, but some well depths are 1,000 to 3,000 feet deep. <br /> <br />The oajor artesian aquifers are the Wasatch Formation and Fort <br />Union.:o~tion, both of which are medi~-grained sandstones) and parts <br />of the Green River Formation (primarily the Tipton and Laney Shale <br />members). The Wasatch Formation is found in a 2S-mile band south of <br />Pinedala, ~7oming, and in the region north of the Washakie Basin. In <br />areal eItent it is the largest of the above-mentioned confined aquifers. <br />Well yields range from I to 688 gpm; quantities greater than 500 gpm <br />might be possible at depths between 2,000 and 5,000 feet (I,Telder, 1968). <br /> <br />3. The tJord "discharge" used in this section denotes water loss or <br />move~aat from an aquifer. The rate of discharge depends primarily on <br />rock ~e~eability (the coefficient of transmissibility), but it would <br />also depend on the rate of ground water recharge and the gradient of <br />the watar table. <br /> <br />4. A confined aquifer is bounded above and below by impermeable rock <br />strata. Generally, wells ta~ confined aquifers below the region of <br />recharge, resulting in a hydrostatic rise of the water (artesian <br />conditio:lS) . <br /> <br />. <br /> <br />D-S <br />