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<br />. <br /> <br />. <br /> <br />'::::l <br />:::> <br />~ <br />Q) <br />co <br /> <br />7, Identify areas where additional quantities of ground water might be stored <br />unde rground, <br /> <br />8, Provide a means of predicting water availability in different areas of the <br />Arkansas Valley under varying conditions of surface-water delivery and <br />ground-water pumpage, <br /> <br />BASIC ASSUMPTIONS CONCERNING THE AQUIFER IN <br />THE ARKANSAS VALLEY <br /> <br />1. Alluvium not hydraulically connected to bedrock (may be changed in some <br />reaches) <br /> <br />2, Alluvium has finite boundaries exc!"pt where indicated, <br /> <br />3, Alluvium hydraulically connected with river (hydraulic connection may not <br />be complete when water table is below river bed) <br /> <br />4, Water in alluvium under water-table conditions <br /> <br />5, Recharge is from applied irrigation water, precipitation, canal seepage, <br />tributary underflow, and sometimes from the river <br /> <br />6, Discharge is by ground-water return flow, ground-water pumpage, evapo- <br />transpiration, and ground-water underflow into Kansas <br /> <br />7, Water can be salvaged from evapotranspiration by lowering water table <br /> <br />8, Evapotranspiration losses are small where depth to water greater than 10 feet <br /> <br />9, Soil moisture is constant from year to year <br /> <br />1 0, Change in transmissibility caused by changes in saturated thickness and <br />permeability can be averaged or modeled (lower part of aquifer is coarser <br />and more permeable) <br /> <br />1 1. Storage coefficient varies with depth but can be averaged (aquifer grades from <br />coarse on bottom to fine at top) <br /> <br />12, Changes in head cannot be predicted near pumped wells because transmiss- <br />ibility decreases due to pumping <br /> <br />- 4- <br />