Geohydrology and Water Quality of Stratified-Drift Aquifers in the Lower Merrimack and Coastal River Basins, Southeastern New Hampshire

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Geohydrology and Water Quality of Stratified-Drift Aquifers in the Lower Merrimack and Coastal River Basins, Southeastern New Hampshire Click here to return to USGS publications Geohydrology and Water Quality of Stratified-Drift Aquifers in the Lower Merrimack and Coastal River Basins, Southeastern New Hampshire U.S . GEOLOGICAL SURVEY Water-Resources Investigations Report 91-4025 Prepared in cooperation with the NEW HAMPSHIRE DEPARTMENT OF ENVIRONMENTAL SERVICES WATER RESOURCES DIVISION ponds . Figure 13 shows a typical seismic-reflection parameter differed according to the likely range of profile for a traverse across the western shore of each parameter. Cobbetts Pond in a region of hydrologic connection The results of the analysis of each change in between pond and aquifer. Hydraulic conductivity parameter value are shown in figures 18 and 19 for of the pond bottom was assumed to be 2 ft/d), and an east-west profile along column 44 (fig. 15) . The the thickness of the material was assumed to be 2 ft. profile includes the hypothetical production well of These estimates were based on values calculated for largest simulated discharge (0.135 Mgal/d) and rep- riverbed deposits (Haeni, 1978; de Lima, 1989), and resents an area of the model (column 44, row 11) were assumed to be representative of the pond-bot- where the greatest difference in drawdowns oc- tom hydrology . curred between simulations . The computed per- The final parameter, specific yield, was es- centage changes in storage and leakage and the timated to be 0.2 for this unconfined aquifer and was drawdowns for each simulation are listed for com- assigned to the entire model area. parison in table 5. It should be emphasized that these data represent changes in two of three com- ponents of recharge, aquifer storage, and pond and Application of numerical model river leakage . Not represented is the change in recharge from till and bedrock uplands, which is Five wells were simulated in the model and commonly simulated in numerical ground-water flow pumped at various rates until the limits for draw- models . The superposition technique, however, down were attained at the end of 180 days. Five simplifies the flow regime by simulating the till- wells were needed because the model cells that con- aquifer boundary as "no flow", where additional flow tained the pumped wells went dry if the total dis- is not induced across this boundary. The tabulated charge simulated was distributed among fewer wells. results, therefore, are intended only to show relative The locations of the wells and resultant drawdowns differences in the simulations . are shown in figure 17. The combined pumping rate Aquifer hydraulic-conductivity (Ka) values of the five wells, 0.64 Mgal/d, represents the es- were multiplied by factors of 1 (model standard), 2, timated potential yield of the basin. The potential and 0.5 in three separate simulations . Doubling the yield as used in this report describes the rate at hydraulic conductivity of the aquifer resulted in a which water can be withdrawn from a basin under 32-percent overall reduction in drawdown at conditions of pumping for 180 days without recharge production wells and a decrease in the natural and without having adverse impacts on the water ground-water flow to the ponds . The reduction in resource (see glossary) . drawdown extended generally to a distance of 1,500 ft from well locations, beyond which draw- downs were slightly greater than at corresponding Sensitivity analysis cells in the model standard. Reducing the hydraulic conductivity by 0.5 had A sensitivity analysis of some of the model the greatest effect on drawdown at well locations for parameters was done to show the effect these these simulations . Overall, drawdown increased by parameters have on estimates of potential yield . The 57 percent at production wells, and a greater per- analysis determined the relative importance of input centage of water came from aquifer storage. Draw- data values on calculations of potential yield and downs decreased slightly relative to the model provided a basis for assessing uncertainty in the standard near the till-aquifer boundaries. simulations given the likely range in each value. Pond-bottom conductance (Kb) values were The principal input parameters of aquifer multiplied by factors of 1 (model standard), 10, and hydraulic conductivity, pond-bottom conductance, 0.1 in three separate simulations . These changes specific yield, and duration of pumping were inde resulted in computed heads that were identical to pendently increased and decreased by a constant those of the model standard . No change in the factor throughout the modeled area while other proportions of water derived from the two sources parameters were left unchanged . A reference (table 5) was observed . The insensitivity of the simulation was selected to represent the best es- model shows that pond leakage is not the primary timate of the hydrologic properties of the aquifer . control on the availability of water to the simulated This reference serves as a standard from which sub- production wells, even though one simulated sequent simulations with different input values can production well was within 600 ft of Cobbetts Pond. be compared. The amount of adjustment of each The results are probably a reflection of (1) limited 41 ~° r~/~ rte is 96 / '/ X2°/ l~Y7tl~ Base from U .S . Geological Survey CONTOUR INTERVAL 20 FEET Windham, N.H . 1 :24,000, 1953, photorevised 1985 NATIONAL GEODETIC VERTICAL DATUM OF 1929 0 1 2 KILOMETERS EXPLANATION STRATIFIED DRIFT MODEL BOUNDARY 177771 TILL AND BEDROCK ~~ HYPOTHETICAL PUMPED WELL POND CELLS LINE OF EQUAL DRAWDOWN-Simulated drawdown after pumping 180 days . Contour interval 1 foot Figure 17.--Drawdown resulting from pumping five hypothetical wells completed in the Windham-Cobbetts Pond aquifer after pumping at a combined rate of 0.64 million gallons per day for 180 days . 42 2 MILES 160 J W 158 W J W W 156 mO ¢ - WF 154 W W z w 0 F- 152 F- J W J m 150 F-¢ Wm F- ¢ 148 146 1,500 1,000 500 0 500 1,000 1,500 DISTANCE FROM PUMPED WELL, IN FEET Figure 18.--Effects of varying hydraulic conductivity on results at hypothetical well D from the Windham-Cobbetts Pond model. J W W J W In W O m F- LU W LL Z W F- F- J W J m F- W F- ¢ 1,000 500 0 500 1,000 DISTANCE FROM PUMPED WELL, IN FEET 162 J W DURATION OF PUMPING (t) W t =180 days (Model Standard) J 160 t=90 days W W 158 O m F- W W 156 LL z Lw 0 154 H J W J 152 m F- IY W 150 F- 148 1,500 1,000 500 0 500 1,000 1,b00 DISTANCE FROM PUMPED WELL, IN FEET Figure 19.--Effects of varying specific yield and duration of pumping on results at hypothetical well D from the Windham-Cobb etts Pond model. Table 5.--Summary of aquifer-evaluation results showing sensitivity of model parameters [Mgal/d, million gallons per day; ft, feet; K., horizontal hydraulic conductivity ; Kb, pond- and river-bottom conductance ; Sy, specific yield; t, duration of pumping, in days; --, simulation failure, no values computed] Change in Percentage of Average flux to change in drawdown Percentage difference Model Change in surface Percentage ground-water at production from model standard parameters storage water' of change in flux to sur- wellsz in drawdown at prod- (Mgal/d) (Mgal/d) storage face water (ft) uction wells Windham-Cobbetts Pond aquifer Model 0.60 0.04 94 6 7.6 standard' Ke x 2 .57 .07 90 10 5.2 32 Ka x 0.5 .62 .02 97 3 12 -57 Kb x 10 .60 .04 94 6 7.6 0 Kb x 0.1 .60 .04 94 6 7.6 0 Sy x 0.3 .61 .03 96 4 6.4 16 Sy x 0.1 .57 .07 90 10 10.7 -41 t = 90 .62 .02 97 3 5.7 25 t = 365 .57 .07 89 11 10.3 -36 Kingston-Powwow River aquifer Model .48 3.52 12 88 8 standard 4 Ka x 2 .36 3.64 9 91 4.2 48 Ka x 0.5 Kb x 10 .36 3.64 9 91 7.1 11 Kb x 0.1 1.27 2.73 32 68 11.1 -39 Sy = 0.3 .63 3.37 16 84 7.8 3 Sy = 0.1 .29 3.71 7 93 8.2 -3 t = 90 .75 3.25 19 81 7.6 5 t = 365 .29 3.71 7 93 8.2 -3 1 Includes induced infiltration and ground water captured before it reaches surface-water bodies. 2 Computed (by use of equation 3) as the average drawdown for all production wells in the simulation. 3 Simulation with five wells pumping at a combined discharge of 0.64 Mgal/d. 4 Simulation with eight wells pumping at a combined discharge of 4.0 Mgal/d. Model parameters represent best estimates of the natural system, Ka x 1, Kb x 1, Sy = 0.2, and t = 180 days. 45 ground-water flow in the narrow section of stratified Well-capture area drift that connects Cobbetts Pond to the aquifer and (2) the distance separating the wells from Simpsons pond. Well-capture areas were constructed by use of Specific yield (Sy) was set equal to 0.2 (model the method of superposition and information shown standard), 0.3, and 0 .1 in three separate simulations . in figures 16 and 17. Figure 16 shows the configura Simulated drawdowns were sensitive to small tion of the initial water table and figure 17 shows the changes in the specific yield. An increase in specific drawdown contours constructed from drawdowns yield to 0.3 had a large effect, reducing drawdowns computed from the two-dimensional numerical not only at well locations but also throughout the model .
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