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last three years is significantly higher than data between each <br />• pumped sample (see Figure 8-73). This is probably due to some <br />stabilization in water quality in well J1 which causes bailed and <br />pumped samples to yield significantly different water. The <br />pumped samples should better represent average conditions in the <br />aquifer. The COY well conductivity data presented in Figure B-74 <br />shows that the higher precipitation amounts in 1983 and 1984 <br />resulted in much higher conductivity values than after 1984. The <br />conductivity values, except the 1988 value, since 1985 Y~ave shown <br />a slight rise which is reflected in the TDS plot (see Figure B- <br />36). The 1988 value is thought to be low and in error because <br />the DSSUM agrees well with the TDS. Conductivity variations in <br />the alluvial wells and remaining "P" series wells are thought to <br />. be naturally occurring fluctuations due to their distance to <br />active mining and the normally expected wide variations <br />associated with shallow aquifers. <br />Monitoring of well B1-03a was begun in 1987. Water <br />collected from the Third White Sandstone well yielded the <br />conductivities plotted on Figure 8-75. Little change has been <br />seen in well 81-03a and the conductivity plot is similar to the <br />TDS plot. Well Glux-1 was installed in September 1988 in the <br />First White Sandstone to monitor water upgradient of the Lux <br />domestic well. Values of conductivity collected to date are <br />presented on Figure B-76. The field conductivity values for <br />Cottonwood Seep showed little change in 1988 with only the <br />November value slightly lower at 1006 umhos/cm. Field <br />. conductivities for the West Buzzard site for May was 1640 and <br />3-16 <br />