ML21341A484
| ML21341A484 | |
| Person / Time | |
|---|---|
| Site: | Consolidated Interim Storage Facility |
| Issue date: | 11/22/2021 |
| From: | Consolidated Interim Storage Facility |
| To: | Office of Nuclear Reactor Regulation, Office of Nuclear Material Safety and Safeguards |
| Shared Package | |
| ML21341A497 | List: |
| References | |
| E-59638 | |
| Download: ML21341A484 (63) | |
Text
{{#Wiki_filter:OCCURRENCE OF GYPSUM AT THE WCS SITE Outcrops of the Dockum Group in the RCRA landfill at the WCS site contain minor amounts of gypsum. Gypsum appears to be confined to a ~20 ft thick horizon roughly 30 ft below the caliche caprock and is absent from this horizon where calcic alteration has penetrated the upper Dockum surface. The gypsum horizon does not occur throughout the RCRA landfill excavation and is limited to the southern-most outcrops. Gypsum is contained within burrowed, mottled red, silty to sandy mudstone displaying blocky fabrics consistent with paleosol formation and pedogenic movement of clays. Slickensides are also common within the mudstone. Dockum Group cores from the site area show little evidence of gypsum to depths of up to 270 ft, indicating that the gypsum occurs only locally. The gypsum displays a variety of morphologies including fibrous antitaxial veins, lenticular gypsum rosettes, and passive pore-filling cements in fractures. In the following, we discuss describe each of these gypsum morphologies and then comment on its origin. GYPSUM MORPHOLOGIES Poorly preserved, discontinuous, arcuate to planar, subvertical to subhorizontal, antitaxial gypsum-filled veins occur within the gypsum-bearing interval at the WCS site (Figure 1). Crystals within the veins are blocky and are primarily oriented perpendicular to the edge of the vein, indicating that minimum principle stresses were oriented subvertically when the veins formed (e.g., Durney and Ramsay, 1973; Ramsay, 1980). Gypsum crystals within the veins appear to be partly corroded or fluted and may show local overgrowths or recrystallization (Figure 2), indicating a complex fluid history since the veins first formed. Medial lines, 69
commonly associated with antitaxial veins, are poorly preserved due to gypsum dissolution, overgrowth, and possible recrystallization. At the WCS site, lenticular gypsum rosettes occur in elongated zones along some fractures, in cylindrical zones (possible rizoliths) (Figure 3), and as irregular masses (Figure 4). Gypsum crystals range up to ~1 cm and contain inclusions of the mudstone host rock. The morphology of the gypsum crystals provides some information about their origin. Lenticular gypsum crystals form from alkaline fluids (pH >7.5) in the presence of soluble organic materials at relatively high temperatures (greater than ~ 35° C) (e.g., Cody, 1979; Cody and Cody, 1988). Lenticular penetration twins observed at the WCS site also require the presence of high concentrations of terrestrial humic substances in the pore fluids (Cody and Cody, 1988). Large (several cm), interlocking gypsum crystals occupy some fractures at the WCS site (Figure 5). Some crystals contain small inclusions of mudstone, while the surfaces of other crystals are lenticular. The large crystal size indicates that most of this gypsum grew passively into and filled existing void space associated with fractures. Limited displacive and incorporative growth may have occurred as the crystals began to encroach on the boundary of previously open fractures. DISCUSSION Widespread occurrences of antitaxial gypsum veins have been attributed to stresses induced by large-scale processes such as unloading (Holt and Powers, 1990 a, b; El Tabakh et al, 1998) and collapse due to regional-scale dissolution (Gustavson et al., 1994). The limited vertical and areal extent of gypsum at the WCS site, however, eliminates unloading and dissolution as a potential cause of the gypsum veins found at the site. Because the veins are typically small in 70
length (< 1 m), discontinuous, subvertical, and often arcuate, they likely developed below the water table in response to localized stress conditions within ductile Dockum mudstones. Under these conditions fracturing is not required to produce antitaxial gypsum veins, as the force of crystallization is sufficient to open the space required by the vein, and the orientation of veins and their fibers reflect local stress conditions (e.g., Means and Li, 2001; Elburg et al., 2002; Hilgers and Urai, 2005). Furthermore, it is difficult to maintain open fractures within a water-saturated mudstone. The original fibrous texture of the veins has been altered by recrystallization and overgrowth, and later gypsum undersaturated fluids dissolved and corroded vein fibers. Because other forms of gypsum are also present within the same limited area, it is likely that these veins developed within the same hydrologic environment as the other forms of gypsum present at the site. This does not represent a new concept as syndepositional gypsum veins have been reported elsewhere (e.g., Holt and Powers, 1990 a,b; Aref and Morsy, 2000). The forms of gypsum present at the WCS site reveal additional information about the hydrologic system in which they formed. Crystal habits suggest that lenticular gypsum rosettes at the WCS site formed displacively in soft sediments containing warm and alkaline groundwater with high amounts of humic substances (e.g., Cody and Cody, 1988), requiring the decomposition of large amounts of plant matter. The lenticular habit of some of the passive pore-filling crystals suggests that they are coeval with the rosettes and also formed in warm, alkaline, humic-rich groundwater. The limited extent of gypsum and its proximity to the caliche caprock at the WCS site suggest that hydrologic environments that formed gypsum were also of limited vertical and areal extent. Because abundant humic substances are required to form lenticular gypsum rosettes, the gypsum formed in a shallow, phreatic aquifer in a warm climate with abundant vegetation. 71
These conditions suggest that the gypsum likely developed beneath or at the margins of a small saline lake or wetland. The source of dissolved gypsum within the groundwater need not be the deep evaporites that occur over 1,500 ft below the gypsum horizon. Low permeability mudstones separate deeper Dockum aquifers from the gypsum horizon, and current groundwater age dating (Darling, 2006) supports hydrologic separation. During the Triassic and throughout most of the Cenozoic, eastward-draining fluvial systems associated with the Dockum Group and Ogallala Formation crossed evaporite-bearing rocks exposed west and northwest of the WCS site. Groundwaters associated with these fluvial systems were likely to be enriched in dissolved gypsum. Sulfate may also have been derived from sulfide minerals within the Dockum group mudstones (e.g., Joeckel et al., 2005), atmospheric sulfer (e.g., Dultz and Kühn, 2005), Cretaceous seawater, or shallow saline groundwaters associated with saline lakes (e.g., Wood and Jones, 1990). Gypsum at the WCS site could not have formed in the Holocene. The relationship to pedogenic carbonate indicates gypsum formed earlier than the calcretes. The OAG interval at the WCS RCRA landfill currently contains no groundwater. Nearby, the pH of groundwater in two samples from the OAG aquifer is 7.36 and 7.15 (Darling, 2006), too low to generate lenticular crystals (Cody and Cody, 1988). Furthermore, OAG waters are undersaturated with respect to gypsum, and the vegetative cover cannot provide sufficient humic substances to generate gypsum rosettes. The gypsum horizon predates the development of the caprock caliche. Gypsum is absent where calcic alteration associated with the caliche caprock has penetrated the upper Dockum surface. The caprock developed on a long stable topography. In the vicinity of topographically low areas, downward percolating fluids dissolved gypsum, reducing the areal extent of the 72
gypsum horizon. The gypsum horizon was preserved in topographically high areas where gypsum was beyond the depth of high amounts of infiltrating precipitation. Some etching and corrosion of gypsum veins likely occurred during the development of the caprock. In the vicinity of the WCS site, conditions suitable for the development of warm, alkaline, saline lakes or wetlands bounded by vegetated environments have existed several times prior to the development of the caprock. Dockum mudstone textures observed at the WCS site are consistent with a wetland or a shallow lacustrine environment, and the Dockum environment was sufficiently warm to produce lenticular gypsum. Abundant burrowing attests to significant biological activity, and soil textures suggest subaerial exposure and the presence of plants. During the accumulation of the Dockum, fluvial systems drained evaporite terrains west and northwest of the site (McGowen et al., 1979). Groundwaters associated with these systems were likely sufficiently alkaline and saline to lead to localized gypsum accumulation in the vicinity of wetlands and lakes. These conditions persisted after Dockum deposition. Eastward drainage of evaporite terrains likely continued after Dockum deposition until the accumulation of the Antlers Formation during the Cretaceous. While this period of time is dominated by net erosion, localized wetlands or saline lakes capable of accumulating the WCS gypsum may have developed. During the Cenozoic, eastward drainage over evaporite terrains again resumed, and localized wetlands or saline lakes could have formed.
SUMMARY
There are three major summary points from this examination of gypsum occurrences at the WCS site and a review of literature: 73
- Because the gypsum is limited in areal extent and occurs within a limited horizon near the upper surface of the Dockum redbeds, the occurrence of gypsum cannot be related to large-scale processes such as unloading or dissolution of underlying evaporites.
- Antitaxial gypsum vein morphologies suggest that the veins developed in response to localized stress conditions.
- Gypsum morphologies indicate formation in shallow, warm, alkaline groundwaters. The most likely setting and time of formation is syndepositional, as sulfate, organic activity, and warm temperatures should have been present at and near the surface; other possible periods of exposure or near-exposure occurred between Dockum deposition and the deposition of the Cretaceous Antlers Formation and in the Cenozoic prior to the accumulation of the caprock.
REFERENCES Aref, M. A., and M. A. Morsy, 2000, Polygonal shrinkage cracks filled with gypsum in the Upper Eocene, Fayum, Egypt, Sedimentology of Egypt, vol. 8, p. 89-103. Cody, R. D., 1979, Lenticular gypsum: Occurrences in nature, and experimental determinations of effects of soluble green plant material on its formation, Journal of Sedimentary Petrology, vol. 49, no. 3, p. 1015-1028. Cody, R. D., and A. M. Cody, 1988, Gypsum nucleation and crystal morphology in analog saline terrestrial environments, Journal of Sedimentary Petrology, vol. 58, no. 2, p. 247-255. Darling, B. K., 2006, Letter report on findings related to the age-dating of groundwater at a proposed treatment and disposal facility for low-level radioactive waste, Andrews County, Texas, unpublished report, LBG-Guyton Associates, Lafayette, LA. 74
Durney, D. W. and Ramsay, J. G., 1973, Incremental strains measured by sysntectonic crystal growths, in Gravity and Tectonics, K.A. de Jong and R. Scholten (eds), John Wiley and Sons, New York, p. 67-96. Dultz, S. and P. Kühn, 2005, Occurrence, formation, and micromorphology of gypsum in soils from the Central-German Chernozem region, Geoderma, vol. 129, p. 230-250. El Tabakh, M., B. C. Schreiber, and J. K. Warren, Origin of fibrous gypsum in the Newark Rift Basin, Eastern North America, Journal of Sedimentary Research, vol. 68, no. 1, p. 88-99. Elburg, M. A., P. D. Bons, J. Foden, and C. W. Passchier, 2002, in Deformation mechanisms, rheology and tectionics: Current status and future perspectives, S. de Meer, M. R. Drury, J. H. P. de Bresser, and G. M. Pennock (eds), Geological Society, London, Special Publications, vol. 2000, p. 103-118. Gustavson, T. C., S. D. Hovorka, and A. R. Dutton, 1994, Origin of satin spar veins in evaporite basins, Journal of Sedimentary Research, vol. 64, no. 1, p. 88-94. Hilgers, C., and J. L. Urai, 2005, On the arrangement of solid inclusions in fibrous veins and the role of the crack-seal mechanism, Journal of Structural Geology, vol. 27, p. 481-494. Holt, R.M., and D. W. Powers, 1990a, Geotechnical activities in the air intake shaft (AIS): DOE/WIPP 90 051, US Department of Energy, Carlsbad, NM. Holt, R.M., and D. W. Powers, 1990b, The Late Permian Dewey Lake Formation at the Waste Isolation Pilot Plant, in Geological and Hydrological Studies of Evaporites in the Northern Delaware Basin for the Waste Isolation Pilot Plant (WIPP), D.W. Powers, R. M. Holt, R. L. Beauheim, and N. Rempe, (eds) Guidebook 14, Geological Society of America (Dallas Geological Society), p. 45-78. Joeckel, R. M., B. J. Ang Clement, L. R. VanFleet Bates, 2005, Sulfate-mineral crusts from pyrite weathering and acid rock drainage in the Dakota Formation and Graneros Shale, Jefferson County, Nebraska, Chemical Geology, 2005, vol. 215, p. 433-452. McGowen, J. H., G. E. Granata, and S. J. Seni, 1979, Depositional framework of the lower Dockum Group (Triassic) Texas Panhandle, Report of Technical Investigations No. 97, Bureau of Economic Geology, The University of Texas at Austin, 60 p. 75
Means, W. D., and T. Li, 2001, A laboratory simulation of fibrous veins: Some first observations, Journal of Structural Geology, vol. 23, p. 857-863. Ramsay, J. G., 1980, The crack-seal mechanism of rock deformation, Nature, vol. 284, p. 135-139. Wood, W. W. and B. F. Jones, 1990, Origin of solutes in saline lakes and springs on the southern High Plains of Texas and New Mexico, in Geologic framework and regional hydrology; upper Cenozoic Blackwater Draw and Ogallala Formations, Great Plains, T. C. Gustavson (ed), proceedings of the Symposium on geology and geohydrology of the Tertiary Ogallala Formation (Group) and Quaternary Blackwater Draw Formation, Lubbock, TX, p. 193 - 208. 76
APPENDIX A FIGURES 77
Figure 1. Antitaxial gypsum veins found in the WCS RCRA landfill are discontinuous and display planar (P) and arcuate (A) morphologies. 78
Figure 2. Gypsum crystals within antitaxial veins appear to be partly corroded or fluted and show local overgrowths and possible recrystallization. Figure 3. Rosettes of gypsum crystals display lenticular crystal habits. This example occurs in a roughly cylindrical zone and could be a rizolith. 79
Figure 4. Some lenticular gypsum rosettes occur in irregular masses within the host mudstone. Figure 5. This gypsum fracture filling from the WCS site displays large interlocking crystals with lenticular surfaces. Note that some wall rock mudstone has been incorporated within the crystals, especially along crystal boundaries. 80
APPENDIX B BASIC STRATIGRAPHIC DATA FROM OIL AND GAS WELLS AT AND AROUND THE WCS SITE 81
Stratigraphic Data at WCS Site (Figures 14-19) Depth Data Elevation Data Thickness Data (ft below reference elevation) (ftamsl) (ft) c 0
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APPENDIX C BASIC STRATIGRAPHIC DATA FROM OIL AND GAS WELLS ACROSS A SECTION OF THE MESCALERO RIDGE, NM 84
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29406 19 34 23 1980N 1980W 637580 3612988 3817 1794 2101 307 2023 1 f1t:i 29299 19 34 23 1980N 660E 638378 3613002 3832 1804 211 0 306 2028 1722 30839 19 34 24 1650S 2310W 639295 3612516 3812 1805 2105 300 2007 1707 24413 19 34 24 1980N 760E 639955 3613031 3840 1803 2100 297 2037 1740 24390 19 34 24 330S 1700E 639681 3612121 3794 1799 2108 309 1995 1686 2393 19 34 24 660N 660E 639980 3613434 3862 1802 2100 298 2060 1762 23502 19 34 24 660S 660W 638794 3612205 3794 1804 211 0 306 1990 1684 28571 19 34 24 760S 2080E 639563 3612249 3814 181 5 2123 308 1999 1691 21369 19 34 25 1980S 660W 638812 3610999 3753 1814 2120 306 1939 1633 25101 19 34 25 1670N 2310E 639504 3611508 3775 1795 211 0 315 1980 1665 20889 19 34 25 1780N 1980W 639210 3611469 3771 1806 2117 311 1965 1654 25123 19 34 25 1800N 990E 639908 3611476 3772 1804 2113 309 1968 1659 22967 19 34 25 1980S 660E 640016 3611020 37()2 1803 2120 317 1959 1642 21098 19 34 25 2130N 760W 638837 3611356 3775 1808 2122 314 1967 1653 24868 19 34 25 330N 1650W 639102 3611909 3788 1807 211 3 306 1981 1675 23708 19 34 25 610S 1880W 639191 3610588 3745 1815 2132 317 1930 1613 27896 19 34 25 660N 1980W 639204 3611811 3798 1815 2120 305 1983 1678 02394 19 34 25 660N 660W 638800 3611803 3779 1800 211 0 310 1979 1669 02396 19 34 25 660S 1980W 639222 3610604 3743 181 3 2126 313 1930 1617 02395 19 34 25 660S 660E 640022 3610618 3746 1808 2128 320 1938 1618 24069 19 34 25 760N 760E 639973 3611794 3786 1802 2108 306 1984 1678 24867 19 34 25 990N 1980E 639601 3611718 3781 1801 211 0 309 1980 1671 21745 19 34 25 990S 1650W 639119 3610703 3737 1807 2123 316 1930 1614 21370 19 34 25 990S 400W 638736 3610696 3741 1817 2130 313 1924 161 1 22081 19 34 26 1650S 1980W 637609 3610878 3751 1805 2122 317 1946 1629 36196 19 34 28 1980S 660W 633984 3610919 3714 1695 2032 337 2019 1682 32003 19 34 32 2310N 1980E 633195 3609597 3680 1512 1840 328 2168 1840 32783 19 34 34 19805 1980E 636418 3609349 3696 1677 2020 343 2019 1676 20096 19 34 36 660S 330E 640147 3609010 3702 1830 2153 323 1872 1549 20144 19 35 6 19808 660E 641585 3617492 3898 1830 2106 276 2068 1792 20322 19 35 6 1980S 1980E 639806 3617492 3900 1822 2096 274 2078 1804 20590 19 35 6 860N 660E 641557 3618217 3924 1840 211 0 270 2084 1814 21171 19 35 6 560S 1880E 641213 3617059 3921 1850 2134 284 2071 1787 39842 19 35 6 660S 660W 640393 3617038 3950 1859 2140 281 2091 1810 29945 19 35 18 1780S 660E 641623 3614203 3919 1870 2159 289 2049 1760 29041 19 35 18 660N 1980W 640813 3615023 3949 1869 2159 290 2080 1790 03169 19 35 19 990S 660W 640400 3612349 3829 1808 2111 303 2021 1718 03168 19 35 19 6605 660E 643242 3613873 3802 1808 211 0 302 1994 1692 33762 19 35 30 9905 700E 641678 3610736 3758 1808 2122 314 1950 1636 24034 19 35 30 20908 760E 641659 3611071 3778 1810 2120 310 1968 1658 23987 19 35 30 1980S 1980W 640881 3611010 3752 1810 2122 312 1942 1630 03259 19 35 30 2310N 330E 641757 3611332 3768 1800 2105 305 1968 1663 03260 19 35 30 660S 1980E 641288 3610635 3752 1812 2124 312 1940 1628 03256 19 35 30 330S 990W 640579 3610507 3738 1796 211 5 319 1942 1623 03258 19 35 30 1980S 660E 641690 3611038 3757 1803 211 5 312 1954 IO'+L UTM (NAD27) coordinates were calculated from the nearest section comer. 86
APPENDIX D BASIC STRATIGRAPHIC DATA FROM OIL AND GAS WELLS ACROSS A SECTION OF MONUMENT DRAW, NM (T21S, R37E) 87
Basic Drillhole Data from T21S, R37E for Figures 29-31
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~ ~ 0 0 0 0 0 ltl ffl ~ c~ Q) ..... I- I- Q) ~ Q) '+- Q) '+- :::J -Q) '+-
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<( ~ t- O::'. Cl) LL-= LL 0 :::::i :::::i O::'. w 0 0 0 0 t- O'.'. w 0 w 0 34937 21 37 1 990s 2430w 676917 3597578 3527 1538 1744 206 1989 1783 34411 21 37 2 3800s 1200w 674926 3598426 3498 1389 1590 201 2109 1908 06373 21 37 2 660s 1980w 675164 3597469 3473 1349 1554 205 2124 1919 37725 21 37 3 330s 330w 673048 3597335 3476 1282 1489 207 2194 1987 35734 21 37 3 1300s 1980e 673956 3597664 3477 1305 1513 208 2172 1964 37727 21 37 3 1940s 1760w 673483 3597825 3437 1257 1460 203 2180 1977 06388 21 37 3 1980s 660w 673148 3597838 3450 1275 1495 220 2175 1955 35354 21 37 3 3448n 1576w 673389 3598560 3469 1299 1522 223 2170 1947 35225 21 37 3 3240s 1839w 673508 3598222 3458 1283 1490 207 2175 1968 35352 21 37 3 2310n 990w 673211 3598907 3488 1310 1520 210 2178 1968 06386 21 37 3 1582n 330w 673010 3599129 3490 1320 1527 207 2170 1963 35224 21 37 4 3196s 426e 672817 3598208 3450 1280 1490 210 2170 1960 35768 21 37 4 330s 1980e 672343 3597335 3477 1276 1493 217 2201 1984 37983 21 37 4 2630s 2310e 672243 3598036 3483 1303 1517 214 2180 1966 37463 21 37 4 2310s 350e 672840 3597938 3481 1293 1503 210 2188 1978 36314 21 37 4 130s 1270e 672560 3597274 3479 1273 1496 223 2206 1983 36141 21 37 4 2460s 990e 672645 3597984 3479 1299 1511 212 2180 1968 35341 21 37 4 3630n 810e 672662 3598505 3428 1265 1480 215 2163 1948 35557 21 37 4 1050n 150e 672863 3599291 3483 1330 1542 212 2153 1941 34737 21 37 4 2620n 116e 672874 3598812 3483 1306 1516 210 2177 1967 06400 21 37 4 1582n 990e 672607 3599129 3486 1320 1529 209 2166 1957 35493 21 37 4 3168s 1650e 672444 3598200 3473 1304 1520 216 2169 1953 34738 21 37 4 3810s 200e 672886 3598395 3445 1257 1470 213 2188 1975 35351 21 37 4 2310n 810e 672662 3598907 3463 1304 1515 211 2159 1948 06397 21 37 4 1980s 660e 672746 3597838 3483 1295 1506 21 1 2188 1977 36811 21 37 4 3480s 1650e 672444 3598295 3480 1296 1514 218 2184 1966 06399 21 37 4 4620s 660e 672746 3598642 3465 1282 1494 212 2183 1971 35895 21 37 4 330s 2050w 671968 3597302 3478 1295 1512 217 2183 1966 06389 21 37 4 660s 660w 671544 3597402 3498 1304 1524 220 2194 1974 35875 21 37 4 330s 760w 671575 3597302 3501 1303 1523 220 2198 1978 12759 21 37 4 1980s 1980w 671947 3597805 3487 1293 1513 220 2194 1974 37236 21 37 5 3630n 330e 671192 3598481 3488 1326 1549 223 2162 1939 27954 21 37 7 330n 660e 669540 3597073 3538 1347 1577 230 2191 1961 21621 21 37 8 1980n 1980e 670739 3596597 3548 1330 1552 222 2218 1996 35350 21 37 9 1980s 330e 672882 3596220 3487 1292 1502 21 0 2195 1985 06445 21 37 9 660n 585e 672769 3597033 3480 1274 1484 210 2206 1996 37028 21 37 10 2375s 505e 674440 3596376 3446 1265 1471 206 2181 1975 37026 21 37 10 330n 330e 674459 3597167 3457 1296 1502 206 2161 1955 35905 21 37 10 550n 740e 674334 3597100 3449 1285 1486 201 2164 1963 35637 21 37 10 704n 2208e 673887 3597053 3431 1277 1475 198 2154 1956 35545 21 37 10 1470n 1350e 674149 3596820 3426 1250 1450 200 2176 1976 34367 21 37 10 42n 2334e 673849 3597255 3427 1455 1972 37876 21 37 10 2360n 1650e 674057 3596549 3447 1260 1460 200 2187 1987 06553 21 37 12 660s 2310e 677097 3595907 3463 1460 1670 210 2003 1793 23953 21 37 18 660s 330e 669686 3594159 3509 1230 1443 213 2279 2066 21035 21 37 19 990n 884w 668478 3593627 3533 1257 1472 215 2276 2061 23494 21 37 30 1650s 660w 668461 3591214 3527 1199 1424 225 2328 2103 24084 21 37 30 660s 1820w 668815 3590912 3518 1200 1424 224 2318 2094 24120 21 37 31 330n 330w 668361 3590610 3523 1184 1405 221 2339 2118 Value in red indicates a ground-level elevation obtained from a topographic map. UTM (NAD27) coordinates were calculated from the map values of the nearest section comer.
88
APPENDIX E ELECTRONIC FILES OF GEOPHYSICAL LOGS OF DRILLHOLES AT AND NEAR THE WCS SITE 89
A CD-ROM is attached to the report with electronic files of geophysical logs from drillholes in the vicinity of the WCS site. These files are in TIFF format and are best viewed with software such as Quick View Plus because of the length of each log. There are no markings of stratigraphic contacts on these logs from this study. The files from the CD-ROM have been converted to PDFs and follow this page. 90}}