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PROPOSED GROUNDWATER REMEDIATION PROTOCOL Data acquired and developed during the placement of soil borings will be used to place wells appropriately for extraction of contaminated groundwater. These wells would serve to remove both non-aqueous phase liquid contamination, should it occur, and groundwater containing significant concentrations of dissolved constituents . The estimated discharge rates, radii of influence and capture for these wells will be calculated ' as shown below. First, a field determination of the hydraulic conductivity "K" will be obtained using the Hvorslev Method (Freeze and Cherry, 1979, p. 340-342 ; Fetter, 1988 , p. 196-199 ) . K= (r2 In MIR] ) 2LT where K= hydraulic conductivity r= radius of the well casing R= radius of the filter pack L= length of the well screen below the static water level T= time for water level to rise 37% of its drop in level due to the removal of water With the Hvorslev Method, the value "K" is derived from measurements made as the water level rises in a well after the ' extraction of a known volume of water . The time "T" is the period required for the water level in the well to recover 370 of the loss of height resulting from the removal of the water ' as determined from a graph of the water level data versus time. The radius of influence and capture "R" will be estimated using the Theis equation (Freeze and Cherry, 1979 , p. 317-319; Fetter, 1988 , p. 164-169 ) as adapted for an unconfined aquifer (after Freeze and Cherry, p. 323 ) . The modified equations are: ( ho-h) = [W(u) ] [ Q/ ( 4 Lz Kb) ] and u= (R2S/4Kbt ) These equations may be rearranged to solve for W(u) and r as : ' W(u ) = [ 4 P Kb (ho-h) /Q] and R= 4uKbt/S where W(u) = well function, as defined by the above equation ' (dimensionless ) K= hydraulic conductivity (m/s ) b= aquifer thickness (m) ' (ho-h) = drawdown at iadzus "R" (m) Q= pump discharge (m /s ) R= radius of influence (m) I . 1