Tyson Research Center

HYDROGEOLOGY OF TYSON RESEARCH CENTER, LONE ELK COUNTY PARK, AND WEST TYSON COUNTY PARK, EASTERN MISSOURI

TVPF Springs
Other Springs
Alluvial Groundwater Wells
Deep Groundwater Wells
Groundwater Geochemistry

LIST OF FIGURES [Figures 1, 2, 3, 4, and 5 appear below in this document]

Fig. 1 Geologic Map of the TVPF area, from Depke (1973)
Fig. 2 Geologic cross section across the TVPF area
Fig. 3 Depth to the top of the St. Peter Sandstone
Fig. 4 Location of perennial springs, intermittent springs, ponds, and karst features at TVPF
Fig. 5 Location of wells used in this report, with indicated DNR identification numbers

LIST OF TABLES [Tables 1, 2 and 3 available as PDF files below in this document]

Robert E. Criss

The Tyson Valley Army Powder Storage Farm is located in a rugged part of the Ozark border that is primarily underlain by Paleozoic carbonate units that dip approximately 1 degree to the northeast. Significant aquifers are the Meramec River alluvium, Mississippian limestone, and the Ordovician carbonates, but the St. Peter Sandstone is the most important source of potable water in the immediate area. Numerous springs emanate from the Burlington-Keokuk Limestone, from near the Fern Glen-Bushburg contact, and from the Kimmswick and Plattin Limestones. Karst features including springs, losing and disappearing streams, leaky lakes, sinkholes and caves are well developed in the Burlington-Keokuk, Kimmswick and Plattin Limestones, demonstrating their high groundwater transmissiviy. Rapid vertical transport of groundwater between the Kimmswick, Decorah and Plattin formations has been reported nearby and likely also occurs in the southern part of Tyson Research Center as suggested by field data. Oxygen isotope and chemical data on various waters in the area are in some cases useful in tracing subsurface flow paths, and strongly suggest links between ponds and lakes in Lone Elk Co. Park and two springs. Field data suggest that TRC Cave and Bluegrass Spring are interconnected. The UTM northing and easting coordinates on the USGS Manchester topographic quadrangle are based on the NAD 27 datum and differ from the newer, widely used NAD 83/WGS 84 datum by being about 212 m lower and 16 m higher.

Location The Tyson Valley Army Powder Storage Farm (TVPF) near Eureka, Missouri is a 2,622 acre area that was a US Army ammunition storage and testing facility during 1941-5 and 1951-61 (Kring and Bailey, 2001). The TVPF has been divided into three parcels representing the Tyson Research Center (TRC) of Washington University, West Tyson Co. Park, and Lone Elk Co. Park. The TVPF lies in the Manchester 7.5 minute quadrangle, occupying Township 44N, Range 4E, and all or parts of Sections 22, 23, 26-29, 32-34. In this report, unless otherwise stated all section numbers refer to this township and range, and the standard notation for water wells (e.g., Miller et al., 1974, p. 7) will be used for sub-locations within an indicated section. As this system is approximate and can cause confusion when section boundaries are irregular, UTM coordinates determined by GPS are also tabulated (see below).

Physiography and Relief. The TVPF lies on the northeastern margin of the Ozarks, and a short distance south of the southern limit of Pleistocene glaciation (Vineyard, 1967). The Burlington escarpment, a cuesta associated with the resistant Burlington Limestone, passes through the middle of TVPF (Depke, 1973), and is partly responsible for the steep local topographic relief. Elevations range from a low of about 395 feet above MSL on the Meramec River to just above 800 feet in Sec. 33Ab, on the boundary road along the western border of TRC.

Geology and Structure. The TVPF area (Fig. 1) lies approximately 5 miles northeast of the House Springs- Eureka anticline, a complex, faulted, northwest-trending structure (Thompson and Robertson, 1993). The structure is clearly exposed in a roadcut on the north side of the Highway W (SR 109) bridge over the Meramec River, approximately 5 miles to the southwest of the area of concern. Despite its proximity the faulted anticline does not disturb the strata in the TVPF area. Dips there are shallow and very uniform, typically 1 degree to the northeast, with a range of 0 to 2 degrees (Depke, 1973). A cross section (Fig. 2) shows this regional dip clearly, while the contour map on the top of the St. Peter Sandstone (Fig. 3) shows the average regional dip to be very close to 1.3 degrees.

Depke (1973) has produced the most accurate geologic map in the area of interest (Fig. 1). Field mapping by Tucker and Criss (1999, unpub.) confirms several details shown by Depke (1973) that are not as accurately represented by Brill (1988) or by HydroGeoLogic (1997, 1999). Examples regarding Brill's map include the position of the Fern Glen-Bushburg contact in upper Tyson Hollow, and the presence of Kimmswick outcrops near the TRC administration building. Similarly, the maps in HydroGeoLogic (1997, 1999) show large areas of Kimmswick Limestone outcrop in upper Tyson Hollow and in its eastern middle tributary that do not exist, as shown by well log 00237A; the large Kimmswick boulders in the creek near Bunker 13 were likely transported to support a bridge and are probably not outcrop. Brill's (1988) map has the advantage of separating the Fern Glen from the Burlington-Keokuk formations. Whitfield (1991) provides a bedrock geological map of the House Springs quadrangle, immediately to the south of TVPF.

Soils. Soils in the TVPF area primarily depend on the nature of the underlying rock strata. The Mississippian Fern Glen and Burlington-Keokuk Limestones underlie the eastern half of TVPF, including all of Lone Elk Co. Park. These limestones weather to reddish residual soils containing abundant chert fragments in permeable clay (Depke, 1973; Lutzen and Rockaway, 1989). This soil type presents particular problems for water retention structures (Lutzen and Rockaway, 1989; Criss et al., 2001), as is the case for Lone Elk Lake as discussed below. Water penetrating through this residual soil can then move rapidly over significant lateral distances through bedrock conduits (Criss et al., 2001).

Developed on the Bushburg Sandstone and the underlying shales are thin residual clay soils that have a tendency to creep (Lutzen and Rockaway, 1989). The Kimmswick, Decorah and Plattin formations are covered by residual, permeable clay soils, while the Joachim Dolomite, mostly exposed in West Tyson Co. Park, is covered by thin soils and sticky clays associated with flaggy bedrock (Lutzen and Rockaway, 1989).

Alluvium. The alluvium along the Meramec River in the TVPF area is 40 to 60 ft. thick, constituted of stratified sand and gravel deposits overlain by silt in overbank areas. Significant gravel dredging formerly occurred in the 1920's, 1950's, and 1970's in Sections 23, 21, and 19, respectively, and is ongoing just south of the Highway W bridge south of Eureka. The alluvial gravels are an important source of groundwater, for example for the golf course to the NW of West Tyson Co. Park, as well as for downstream cities such as Valley Park and Kirkwood (e.g., Miller et al., 1974).

The character of stream banks throughout the Ozarks has changed historically. Prior to European settlement, Ozark streams had many deep pools underlain by silty sediments on top of a gravel bedload. Huge gravel bars aggraded along these streams following the clear-cutting of Ozark forests, which was practically complete by 1910 (Jacobson and Primm, 1997). Such is the condition of the lower Meramec River today, which is lined by bars mostly covered by coarse chert gravels. Even in the 1920's, Lincoln Beach (Sec. 23D; see below) was an excellent sand beach used by thousands of people, but this is not the condition today.

Brief descriptions emphasizing the typical characteristics of the strata that crop out in the TVPF area are given below, from youngest to oldest. Detailed description of these units are provided by Depke (1973, p. 13-96) and Thompson and Robertson (1993). Except for the St. Peter Sandstone, these units all crop out in roaducts along or near I-44 as one proceeds upsection (east and uphill); as well as along the Meramec River as it flows eastward and upsection along the northern boundary of the area of interest. Specific subsectons are provided where the rock units may be easily examined, mostly along I-44. Additional outcrops with indicated formations are indicated on the exposure map in Depke (1973).

Burlington-Keokuk formations (Mississippian; Thickness ~200 ft.) Coarsely crystalline, light gray crinoidal limestone with abundant nodules, beds and masses of white porcellaneous chert. Weathers to terra rossa clay and resistant chert soil residuum. Occurs to the northeast of the Burlington escarpment. A good exposure of the Burlington Limestone occurs on the SE side of the I-44 overpass at the Antire Road exit (Exit 269).

Fern Glen Limestone (Mississippian; Thickness 35-60 ft.) Reddish to yellowish gray, thin bedded to massive, fine to medium grained argillaceous limestone and interbedded shales, with abundant fossils, stylolites and chert. A good exposure of the contact between the lower Fern Glen and the Bushburg Sandstone is on the north side of I-44 (Mile 268.8; see Thompson and Robertson, 1993, p. 148-9.)

Bushburg Sandstone (Devonian; thickness 20-50 ft.) Friable, orangeish-tan, medium grained, massive to cross-bedded sandstone. Thickness variable; deposited on pronounced unconformity. Important and highly distinctive marker bed in the TVPF area. Map unit includes the underlying Glen Park formation and the overlying Bachelor formation (Mississippian), which are thin and discontinuous limestones, shales and sandstones in the TVPF area. Good exposures of the Bushburg are at Bunkers 12, 14, and 49 at TRC, and also at Mile 268.8 (see above).

Kimmswick Limestone (Ordovician; Thickness 65-110 ft.) Light gray, coarsely crystalline, massive, sparsely fossiliferous limestone; Fisherites (formerly, Receptaculites) is diagnostic to the Kimmswick in this area. Cliff former, cavernous in places. Easily distinguished by the abundant, golf-ball sized pits in weathered surfaces. An excellent exposure is in the Mincke Hollow quarry-cave (Sec 28Aa). Depke (1973) includes the thin overlying Maquoketa Shale (Ordovician) in this map unit.

Decorah Group (Ordovician; Thickness 25 ft.) Interbedded greenish-gray shales, limestones and coquinas. Highly fossiliferous in places, with some parting surfaces being almost completely covered with brachiapods and bryozoans. In the lower part of the group are two distinctive, ca. 6-8" thick beds of bentonite that are ~6 feet apart. A fine exposure of the Decorah Group and the underlying upper Plattin Limestone is on the north side of I-44 (Mile 268.2; see Thompson and Robertson, 1993, p. 147-8).

Plattin Limestone (Ordovician; Thickness 110 ft.) Gray, medium bedded to massive, sublithographic limestone, commonly with conchoidal fracture. Abundant burrows produce a mottled surface on fresh exposures, and distinctive, cm-sized pits on weathered surfaces. Fossiliferous in lower section, particularly the thin, dark gray "Establishment Shale" member. Good exposures of the upper and lower parts of the Plattin respectfully occur along I-44 at Mile 268.1 and 267.0; see Thompson and Robertson, 1993, p. 145-8)

Joachim Limestone (Ordovician; Thickness 140 ft.) Yellow-brown to gray, medium to wavy bedded, fine grained, argillaceous dolostone, massive in uppermost part. Basically unfossiliferous except for stromatolitic structures in upper part. A good exposure of stromatolitic structures in the upper Joachim is on the north frontage road at the Lewis Road exit (I-44 Exit 267; see Thompson and Robertson, 1993, p. 145-6).

Karst Features. Besides the springs and losing streams, discussed below, several karst features including caves, sinkholes, and an estavelle occur in the TVPF area (Fig. 4; Table 1). Most of these features are associated with the Kimmswick, Plattin, and Burlington-Keokuk Limestones.

The most extensively developed karst features are located in Section 34C and 34D, in the southern part of TRC and in the lower reaches of Antire and Little Antire Creeks (see "Karst Area", Fig. 4). The features include Mud Cave and TRC Cave developed in Kimmswick Limestone. Downsection in the Plattin Limestone are Bluegrass, Beaumont and Plegge Springs, and a sinkhole and an estavelle near Bluegrass spring. Mud Cave and TRC Cave may be part of the same system, subsequently severed by the erosion of Antire Valley (Owen Sexton, pers. comm., 4/96). Their proximity, similar elevations, and identical rock unit (Table 1) suggest that this is plausible. However, ongoing cave mapping (Osburn and Criss, 2001) indicates that the main passages of both caves have parallel, N60°E trends, and provides no confirmatory evidence for their interconnection. It is possible that the cave systems extend far to the north to sinkholes in Kimmswick Limestone near Mincke Spring, and also to the sinkholes near Bunkers 22 and 50, which are developed in Kimmswick Limestone immediately below the Bushburg Sandstone. TRC Cave has a vertical, sink-type entrance that receives considerable runoff from a gully during rainfall; this water is likely directed downward to the Plattin Limestone to be discharged at Bluegrass Spring, or less likely, at Beaumont Spring (Osburn and Criss, 2001).

Depke (1973, p. 39-41) describes a large "collapse structure" developed in the Plattin, Decorah and Kimmswick formations in Mincke Hollow and its tributaries that extends all the way to the TRC quarry/cave near the northern boundary of TRC; this feature is also shown on the cross section by HydroGeoLogic (1997, 1999). It is possible that a significant, undiscovered and partially collapsed "Bluegrass Cave system" developed in these formations occupies a significant area north of the spring. Direct interconnectivity of the Plattin, Decorah and Kimmswick formations via vertical karst conduits has been described in Jefferson County (Dean and Duley, 1997, p. 125). Ongoing dye tracing experiments (Aley et al., in progress) may prove the interconnectivity of these systems at TRC and of possible downward leakage of water from the Kimmswick Limestone to the Plattin karst system associated with Bluegrass Spring.

Many other karst features, particularly springs and sinkholes, are associated with the Burlington-Keokuk Limestones. These include the spring, sinkhole, and leaky lake at Lone Elk Co. Park, and the springs and the swallow hole in the Williams Creek watershed to the east. Geochemical data suggest that the upper pond in Lone Elk County Park may be leaking through the subsurface to Lone Elk Spring, and that Lone Elk Lake is leaking through the subsurface to Railroad Spring (Fig. 4; see below).

Meramec River. The hydrology of the TVPF area is dominated by the Meramec River, which occupies a 4,000 mi² watershed that originates in the Ozarks. The lower river is well characterized by the USGS gauging station at Eureka (# 07019000; Sec. 32Dd). The average flow is 3260 cfs, though the range in daily mean discharge is huge, from a low of 196 cfs on August 27, 1936 to 175,000 cfs during the destructive flood on August 22, 1915, a range of nearly 1000x (Hauck et al., 1997). Such extreme variations in flow and the flashy character occur because the Meramec is one of the few remaining unimpounded river basins in the United States. The record flood of 1915 occurred in a wet year (49.28") after the clear-cutting of the Ozark forests, when high runoff would be expected.

As it flows eastward along the northern boundary of TVPF, the Meramec River cuts upsection as it cuts downward at an average gradient of about 1.1 ft. per mile (Criss and Wilson, in review). This condition results from the aforementioned, ~1 degree regional dip of the strata to the northeast. Thus, the Joachim Dolomite crops out along the river in Sec. 21, at and north of West Tyson Co. Park, then the river passes through the Plattin, Decorah, and Bushburg formations north of TRC, and then passes into the Fern Glen and Burlington Limestones as it flows along to the north of Lone Elk Co. Park.

Surface Streams. All streams in and near the area of interest, including Tyson Hollow Creek, Mincke Hollow Creek, Antire Creek, Little Antire Creek, Williams Creek to the east, and Keifer and Fishpot Creeks to the north, are losing streams. Discharge along the length of these streams is much less than that expected for their upstream basin areas. All of these streams are intermittent, possibly excepting the lower reaches of Williams, Keifer and Fishpot Creeks. These streams are related to the geologic strata as follows.

Tyson Hollow Creek occupies a broad, north-trending valley in a 1.2 mi² basin that is mostly floored by the Kimmswick Limestone overlain by 30 ft. of alluvial deposits. Valley walls and the floor of its headwaters and tributaries are mostly underlain by the Bushburg Sandstone, while the higher slopes are underlain by the Fern Glen Limestone, and the surrounding ridgetops are capped by the Burlington Limestone and its associated cherty residuum. Several small springs occur near the Bushburg-Fern Glen contact in its headwater tributaries, but of these only Bunker 35 spring is perennial, and these upper tributaries are generally dry. Tyson Hollow Creek flows only rarely, but scattered pools sustained by intergranular flow occur along its lower reaches during much of the year.

Mincke Hollow Creek occupies a narrow valley in a 0.35 mi² basin that is mostly headed in the Kimmswick Limestone, but passes into the Decorah and Plattin formations near its mouth. The surrounding ridgetops are capped by the Burlington Limestone and its associated cherty residuum. Mincke Spring occurs in its upper part, but flow downstream is intermittent.

The principal stream in Lone Elk Co. Park occupies a broad valley in a 0.7 mi² basin that is floored by Mississippian limestone units, principally the Burlington Limestone but including the Fern Glen Limestone near the mouth. An artificial, ~16 acre lake occupies the lower valley.

Above its confluence with Little Antire Creek, Antire Creek occupies a broad, north-trending valley that is mostly floored by the Plattin Limestone. Surrounding ridgetops are capped by Mississippian limestone units. Several significant springs emanate from the Plattin Limestone near its mouth, including Bluegrass Spring.

Little Antire Creek, a major tributary to lower Antire Creek, occupies a broad, north-trending valley in a 3.3 mi² basin that represents one third of the 10.3 mi² Antire Creek basin. Little Antire valley is mostly floored by the Kimmswick Limestone, but passes into the Decorah and Plattin formations near its confluence with Antire Creek, in Antire Valley Co. Park immediately south of TRC. A significant perennial spring emanates from the Kimmswick Limestone at the end of a line of sinkholes in its head, and perennial Beaumont spring issues from Plattin Limestone near its mouth.

Williams Creek occupies a broad, north-trending valley and drains a 9.4 mi² basin that lies mostly east of TVPF. However, some of the western tributaries of Williams Creek are headed in TRC and Lone Elk Co. Park. Practically all of the basin is underlain by Mississippian limestone units. A gauging/water quality station (#07019090) is located near its mouth.

Kiefer and Fishpot Creeks are perennial losing streams located north of the Meramec River, and have watershed areas of 6.6 mi² and 10.9 mi², respectively. Both streams flow to the southeast within Mississippian limestone units. A USGS gauging/water quality station (#07019072) is located in the middle reach of Keifer Creek, just below a significant spring listed in Table 1.

Ponds and Lakes. One lake and several small ponds, all artificial, occur in the Lone Elk and TRC areas. Surprisingly, few of these bodies ever dry up.

Lone Elk Lake is a ~16 acre lake in Sec. 23C that is fed by runoff from intermittent streams in a 0.53 mi² area, as well as by 1 gpm of flow piped in from Lone Elk spring. An earth fill dam along its northern margin that was constructed ca. 1968 (Depke, 1973, p. 156) impounds the lake. The lake is underlain by Burlington Limestone, and has a history of serious leakage that required considerable grouting (Depke, 1973; Jim Emory, pers. comm.). A simple water balance suggests that less than 10% of the runoff that would be supplied by the 0.53 mi² catchment would evaporate from the lake surface. It would appear that significant leakage persists, as is common for lakes developed above the Burlington Limestone (e.g., Criss et al., 2001). Oxygen isotope and field data strongly suggest that the lake is leaking to Railroad Spring.

Two small ponds occur in Lone Elk Co. Park. Spring pond is in Sec. 26Bbb about 100 ft. north of the only significant spring in the park. A larger, upper unnamed pond occupies an area of ~1 acre in Sec. 27Add. Both ponds are underlain by Burlington Limestone residuum.

Railroad Pond, the largest of the TRC lakes, is a ~0.2 acre lake located in a prairie-like area near the mouth of Tyson Hollow (Sec 22Dbb). The pond is fed by runoff from intermittent streams, and is constructed in alluvium overlying the Kimmswick formation.

Two proximal, abandoned sewage lagoons in Sec. 27Acc are located in a tributary of Tyson Hollow Creek, about 800 ft. southeast of the headquarters building. The lagoons are dug in valley alluvium above the Bushburg-Kimmswick contact. The lagoons are entirely covered with algae in summer.

New Pond is located in a mown grassy area in upper Tyson hollow (Sec. 27Cca), and is fed by local runoff. The pond is constructed in alluvium above the Bushburg Sandstone.

Lizard Pen Pond (Sec. 27 Ccd), located near the head of Tyson Valley, is impounded behind an earth fill dam containing two 4' diameter spillway culverts. The pond is geologically situated above the Bushburg-Kimmswick contact. A sinkhole opened up on the east side of the pond in the winter of 1990-91, and the pond has held little or no water since that time (Dave Schilling, pers. comm., 2001). The water retention problems were not corrected by grouting the sinkhole with bentonite.

Salamander Pond is a small, ~ 2 ft deep woodland pond constructed on a high, 770 ft. elevation hilltop in Sec. 27Ddc. The pond is a shallow pit in the residuum of the Burlington Limestone. It is stunning that this pond never dries up, as its catchment area is a very small part of a hilltop. This condition must be attributable to its shady location, which keeps water temperatures about 5°C cooler than grassland ponds, and the fact that the pond is entirely covered by duckweed during most of the summer and fall.

Spring Pond at TRC is located in a grassy area in Sec 33Daa that is underlain by alluvium above Plattin Limestone. The feature is fed by Bluegrass Spring # 2.

Dock Pond, located a few hundred feet to the west of Spring Pond, has severe water retention problems and is commonly dry (Dave Schilling, pers. comm., 2001).

Twin Ponds are two small woodland ponds constructed at a break in slope near a wooded valley in Sec. 34Bbc. The amphitheater-like shape of the valley head above and about 400 ft. north of the ponds is suggestive of groundwater sapping associated with the Bushburg-Fern Glen contact. The ponds are impounded behind small dams constructed above valley alluvium above the Kimmswick Limestone.

TVPF Springs. Several springs occur at TRC, two perennial springs respectively occur within and immediately north of Lone Elk Co. Park, and one wet-weather spring occurs at West Tyson Co. Park (Fig. 4; Table 1). Several other significant springs occur within 2 miles north, south and east of TVPF.

Bluegrass Spring is perennial and located near I-44 near the southern boundary of TRC (Sec. 34Cbb; Fig. 4). The spring issues from a submerged cave in the upper Plattin Limestone, and a small sinkhole occurs about 25 ft. to the west. An autosampling device at Bluegrass Spring takes samples every day, along with continuous measurements of stage, temperature, and electrical conductivity. A weir and a discharge rating curve have been constructed for the site, and indicate that the flow varies from about 0.3 to 6 cfs (Frederickson, 1998). This flow rate indicates that the catchment for Bluegrass Spring must be significant- at least 0.5 mi².

Two springs, one known as Bluegrass Spring #2, occur at the edge of the woods to the west of Bluegrass spring (Sec. 33Daa). One is located in an estavelle, and is generally expressed as a pool about 6 ft. below the ground surface. The other is an intermittent spring in a small isolated group of trees. Both occur in alluvium above the Plattin Limestone.

Mincke Spring is perennial and issues from the base of a small cliff in the Kimmswick Limestone (Sec. 28Daa). Two small sinkholes and a wet weather "upper spring" orifice occur between 75 and 200 feet southeast of the spring.

A small unnamed spring emanates from a cliff in the upper Plattin Limestone along the Burlington Northern railroad tracks, just northeast of the mouth of Mincke Hollow (Sec. 21Ddc).

Bunker 23 and Bunker 25 Springs emanate about 2 feet above the Fern Glen-Bushburg contact in a tributary of Tyson Hollow Creek (Sec. 33Aab and 33Aaa). Both are intermittent, flowing mostly in the winter and early spring.

Lone Elk Spring (Sec. 26 Bbc), the only flowing spring inside Lone Elk Co. Park, emanates from Burlington Limestone. The discharge of about 1 gpm (0.002 cfs) is piped downhill to Lone Elk Lake. The high d¹⁸O value of the spring is unusual and indicates that the water has undergone significant evaporation (e.g., Criss, 1999). The spring may receive a significant fraction of its water via subsurface flow from upper Lone Elk Pond, located 1500 feet to the southwest and 70 feet higher (Fig. 4).

Railroad Spring (Sec. 23 Bcd) emanates from Fern Glen Limestone beneath the railroad immediately north of the northwestern corner of Lone Elk Co. Park. The discharge is a few gpm and has a very high O value of the spring is unusual and indicates that the water has undergone significant evaporation (e.g., Criss, 1999). The spring may receive a significant fraction of its water via subsurface flow from upper Lone Elk Pond, located 1500 feet to the southwest and 70 feet higher (Fig. 4).

Railroad Spring (Sec. 23 Bcd) emanates from Fern Glen Limestone beneath the railroad immediately north of the northwestern corner of Lone Elk Co. Park. The discharge is a few gpm and has a very high d¹⁸O value, again suggesting evaporation. The geochemical data strongly suggest that the spring derives significant water via subsurface flow from Lone Elk Lake (Fig. 4).

The only spring in West Tyson Co. Park is a small unnamed spring in Sec. 29Ada that flows only during wet weather (Tom Hughes, pers. comm.). The spring emanates from alluvium above Plattin Limestone.

Other Springs. Several significant springs lie outside but within 2 miles of TVPF. One with a flow rate of several cfs emanates from the upper Fern Glen formation immediately above the Keifer Creek gauging station (#07019072; Sec. 15Adb). Except for stormflow, this spring probably represents most of the flow in the 3.91 mi² watershed of upper Keifer Creek, as the creek bottom typically has only discontinuous pools above this point. Several other springs discharge from Burlington-Keokuk Limestones along lower Williams Creek (Sec 25A), only to disappear into a swallow hole; additional springs appear downstream in Sec. 24D. Last, Beaumont, Plegge and other springs discharge from the Plattin Limestone in lower Antire Valley and Little Antire Valley, in Sec. 34D immediately south of TRC.

Alluvial Groundwater Wells. Several shallow wells are constructed in the 40 to 60 ft. thick sand and gravel deposits of the Meramec River valley. The alluvial aquifer is used by the cities of Valley Park and Kirkwood, and was formerly used by the abandoned town of Times Beach. Yields as high as 500 to 1500 gpm are possible in Meramec gravel (Miller et al., 1974). The golf course irrigation well in Sec. 20Ddb is 52 ft. deep and has a yield of 400 gpm (Appendix). Miller et al. (1974, p. 39) report that some of the wells in Valley Park and Times Beach have anomalously high TDS and chloride contents that they attribute to upconing of water from underlying bedrock aquifers, particularly when pumping rates are high.

Deep Groundwater Wells. Several deep bedrock wells produce drinking water from the Ozark aquifer (Fig. 5; Table 2). Formerly, several 204 to 450 ft. deep wells at TRC tapped the Kimmswick, Decorah, Plattin and Joachim formations. Yields for all but one of these were 4 gpm or less. The exception is US Ordnance Plant #1, completed to the Joachim Dolomite, which had a yield of 15 gpm, possibly because it intersected a fracture system.

In the TVPF area the most important, consistent source of potable water is the St. Peter Sandstone. The St. Peter Sandstone is tapped by 465 and 540 ft. deep wells at the gatehouse and at the headquarters at TRC, and by 500 and 675 ft. deep wells at the Visitor Center and the maintenance building at Lone Elk Co. Park (Table 2); yields are 30 to 40 gpm. The unit is also tapped by numerous homes, and several new wells are intersecting it every year, for example near the town of Crescent. The St. Peter Sandstone crops out in the Meramec Valley in Sec. 31, in the southwest part of the Manchester quadrangle, which may represent a recharge zone for the aquifer beneath TVPF. However, because of the regional dip, the St. Peter becomes much deeper to the northeast, and is below sea level in eastern Lone Elk Co. Park (Fig. 3). The thickness of the St. Peter Sandstone beneath TVPF is 75 to 125 ft (Appendix; wells at TRC HQ, West Tyson, and Bridgehead).

Because of its proximity to the surface, the St. Peter Sandstone is not used at West Tyson Co. Park. The underlying Powell and Cotter dolostones are tapped instead; the yield is 20 gpm from the 450 ft. deep well. Much deeper formations are tapped by the 1110 foot deep well at the former Bridgehead (Steiny's) Inn, just to the west of TVPF.

Most groundwaters in the TVPF area are dilute with a near-neutral pH and a Ca-Mg-bicarbonate chemistry. Nevertheless, the available data suggest differences in detail that may prove of use in hydrologic tracing (Tables 1, 3). Also, the residence time model of Frederickson and Criss (1999) uses oxygen isotope variations to provide information about subsurface systems and recharge rates.

Groundwaters in the Meramec River alluvium are more dilute than most deep groundwaters, have somewhat higher average d¹⁸O values of about -6.5 per mil, and have somewhat lower pH. Springs issuing from the Burlington Limestone tend to have variable and high d¹⁸O values, suggestive of close communication with the surface and, in the case of Lone Elk and Railroad Springs, of significant contributions from evaporated surface waters. Springs issuing from near the Bushburg-Fern Glen contact are typically more dilute than any other local waters other than rainfall, and typically have the lowest d¹⁸O values of about -7.3 per mil. Springs issuing from the Kimmswick and Plattin Limestones generally have higher salinities (electrical conductivities) than other local, shallow groundwaters and also have rather low but somewhat variable d¹⁸O values. Well waters from the St. Peter Sandstone have moderate salinities, and most have d¹⁸O values of -7.0±0.1. Two well water samples from the Cotter-Powell dolostones have somewhat higher d¹⁸O values of about -6.7, and would be expected to have higher Mg/Ca ratios than shallower groundwaters. The presence of saline waters at greater depths has been suggested in this area (Miller et al., 1974), though high salinities are not produced from the 1,110 ft deep well at Bridgehead (Sec. 32 Dac).

The 1990 Gatehouse Well at TRC (Sec. 34 Aab; ID #0041757A) currently has an anomalously high electrical conductivity of >800 mS that has been confirmed by repeat measurement. This value is significantly higher than that of other recently measured wells completed in the St. Peter, higher than the 520 mS value reported by the USACE (1997) for the gatehouse well in November 1996, and higher than the previous measurements in our data base. The current d¹⁸O values of this well of -7.1 per mil are also lower than those of six previous samples in our database (-6.8 to -6.9) that were collected in 1997 and 1998. Moreover, our attempt to produce water from the old Gatehouse well (# 4A) on July 6, 2001 was unsuccessful. Because the pump was apparently operational as suggested by noise and vibration when turned on, the shallower old well #4A may have been dry and in the cone of depression of the new gatehouse well. All this evidence suggests that drawdown near the gatehouse well is inducing an increased proportion of recharge to be derived from the overlying Plattin and Kimmswick Limestones rather than from the St. Peter Sandstone. As indicated above, waters in the Plattin and Kimmswick Limestones appear to have the requisite characteristics.

Excepting seasonal variability in the springs, and anomalously high temperatures for well waters that are related to surface pipes etc., the temperatures of the deepest well waters tend to be a few degrees higher than those of waters derived from shallower depths. In western St. Louis County and northern Jefferson County, vertical temperature gradients in wells are observed to be about 0.17°C per 100 feet (Fuller, 1981).

A discrepancy was noted between the UTM coordinates (zone 15) of locations measured by GPS and the UTM coordinates indicated by the tic marks on the Manchester 7 1/2' quadrangle published by USGS. In particular, the eastings compare well, but the northings on the map are approximately 200 meters less than those indicated by GPS. In order to determine the source of this discrepancy, GPS measurements have been made of two NGS bench marks in the Manchester quadrangle that are proximal to TVPF, and these may be compared to the map locations and to the coordinates for the bench marks indicated on the NGS web site. The comparisons are as follows:

NGS Benchmark AA8718 at Exit 269

NGS Coordinates (NAD 83) ..... 713704.351 ..... 4265863.184
GPS measurement (NAD 83/WGS 84) ..... 713702 ..... 4265867
USGS Map (NAD 27) ..... 713710 ..... 4265630

NGS Benchmark AA8716 at Exit 267

NGS Coordinates (NAD 83) ..... 710544.672 ..... 4264566.397
GPS measurement (NAD 83/WGS 84) ..... 710543 ..... 4264573
USGS Map (NAD 27) ..... 710570 ..... 4264330

The measurements indicate that the field GPS measurements reported here agree with the tabulated information for the NGS benchmarks to within the estimated position error of < 10 m, but the northings do not agree well with the USGS information. The discrepancy has been linked to a significant difference between the NAD 83 datum, which is identical within 0.0001 meters to the WGS 84 datum (NOAA, 1995), and the NAD 27 datum used to define the tic marks for the published USGS Manchester quadrangle. NOAA (1995) recommends the use of the notation "NAD 83/WGS 84" for horizontal positions, as adopted here. Follow-up calculations performed on the NGS website (NGS, 2001) indicate that for the Manchester quadrangle, the northings on the map will be 212 m lower, and the eastings 16 m higher, than locations based on the newer NAD 83/WGS 84 datum. Similar but not identical discrepancies for other quadrangles in east central Missouri exist and must be computed in each individual case. In this report, all UTM coordinates will refer to my uncorrected, field GPS measurements relative to the NAD 83/WGS 84 datum (NOAA, 1995), which are believed to be accurate to within the indicated average position error of about 10 meters.

In the course of this work several inconsistencies were noted between previous maps and records and actual locations of features. Such is to be expected with any extensive mapping or record-keeping project. The purpose here is not to criticize but to prevent additional confusion. It is hoped that future readers will similarly view any inaccuracies in the present report.

Lincoln Beach appears to be mislocated on the map. Historical photographs on display at Castlewood State Park show the beach was located in Sec. 23D, about a quarter mile to the west of the depicted map location and on the south side of the Meramec River.

The topography of the vertical, ~50 ft. high quarry wall of the TRC quarry/cave is not accurately represented.

TRC Well number 7, at Bunker 22 (DNR # 0000237A) is in Sec 27Ccc, not 27Db. The subsections and collar elevations of a few other wells are corrected in Table 2 by much smaller amounts.

The Tyson Valley Army Powder Storage Farm is primarily underlain by Paleozoic carbonate units that dip approximately 1 degree to the northeast. Karst features including springs, losing streams, leaky lakes, sinkholes and caves are well developed in the Burlington-Keokuk, Kimmswick and Plattin Limestones. Field data demonstrate the high lateral and vertical permeability of these rock units, including the interconnectivity of the Kimmswick, Decorah and Plattin formations via karst conduits. These characteristics could promote contaminant migration, especially for point sources near sinkholes or situated on Burlington residuum, but the downward transport of contaminants all the way to the important St. Peter aquifer is considered unlikely. In some cases, oxygen isotope and chemical data on waters can be used to identify subsurface flow paths. Geochemical data and dye tracing experiments that exploit rainfall events could be used to better define the subsurface paths and rates of shallow groundwater migration.

Fig.1. Geologic Map of the TVPF area, from Depke (1973). Red line shows line of cross section, directed N46.5E. Geologic formations are indicated by the following key:

Figure 1: (larger JPG image - 1,032K)

Figure 2: (larger PDF image - 57K)

Fig. 3. Depth to the top of the St. Peter Sandstone, shown by contours in feet relative to MSL. The St. Peter Sandstone is the most important domestic aquifer in the area, and the sharp change from the Joachim dolostone to the white St. Peter Sandstone is readily recognized by drillers. Contact elevations are indicated in feet next to the location of the water wells (points). Diamonds represent well positions determined by GPS (this study); open triangles are well positions mapped by Depke (1973). Well logs for most of the former and two of the latter are in the Appendix 1. Figure 5 gives well identification numbers. Grid northeast line is the section line of Fig. 2.

Figure 3: (larger PDF image - 33K)

Fig. 4. Location of perennial springs (black diamonds), intermittent springs (open diamonds), ponds (small circles) and karst features (X's) discussed in this report. Arrows depict inferred flowpaths between surface waters and springs. Abbreviations are LP (Lizard Pen pond and sinkhole), E (Estavelle), B (bunker with indicated number). "Karst Area" shown by the heavy dashed line is a zone where many springs, sinkholes and other karst features are developed in the Kimmswick and Plattin Limestones (see text). Data in Table 1.

Figure 4: (larger PDF image - 35K)

Fig. 5. Location of wells used in this report, with indicated DNR identification numbers. Black diamonds are locations determined by GPS (NAD 83/WGS 84), and well records are available for all but two of these. Open triangles represent locations given by Depke (1973). Grid northeast line is the section line of Figure 2. Data in Tables 2 and 3 and Appendix 1.

Figure 5: (larger PDF image - 29K)

Table 1. Springs, Ponds and Karst Features within and near the TVPF area - Table 1 PDF
Table 2. Water well data - Table 2 PDF
Table 3. Geochemical data for well waters - Table 3 PDF

LIST OF APPENDICES

1. NGS benchmark at Antire Road Exit (#269) off I-44
2. NGS benchmark at Lewis Road Exit (#267) off I-44 

Aley, T., Moss, P. and Aley, C., in progress, Groundwater tracing at Tyson (ex.) Powder Farm, Eureka, Missouri.

Brill, K.G., Jr. (1988) Geologic Map of the Manchester Quadrangle, Missouri Division of Geology and Land Survey, Map SL 8805.

Criss, R.E. (1999) Principles of Stable Isotope Distribution, Oxford University Press, NY, 254 p.

Frederickson, G.C. and Criss, R.E. (1999) Isotope hydrology and time constants of the unimpounded Meramec River basin, Missouri. Chem. Geol., v. 157, p. 303-317.

HydroGeoLogic (1997) Draft Final Remedial Investigation Work Plan for the Tyson Valley Powder Farm, Eureka, Missouri. Report for U.S. Army Corps of Engineers.

HydroGeoLogic (1997) Water Well Data Summary Report, Tyson Valley Powder Farm, Eureka, Missouri. Report for U.S. Army Corps of Engineers, 23 p.

HydroGeoLogic (1998) Final Water Well Data Summary Report Addendum, Tyson Valley Powder Farm, Eureka, Missouri. Report for U.S. Army Corps of Engineers.

HydroGeoLogic (1999) Final Data Summary Report, Phase II Remedial Investigation, Tyson Valley Powder Farm, Eureka, Missouri. Report for U.S. Army Corps of Engineers.

Imes, J.L. (1988) Geohydrology and hydrochemistry of the Ozark plateaus aquifer system, in Regional Aquifer Systems of the United States, Aquifers of the Midwestern Area. AWRA Monograph Series no. 13, p. 165-178.

Jacobson, R.B. and Primm, A.T. (1997) Historical land-use changes and potential effects on stream disturbance in the Ozark plateaus, Missouri. U.S. Geological Survey Water Supply Paper 2484, 85 p.

Kring, D. and Bailey, D. (2001) Tyson Valley (ex.) Army Powder Storage Farm, St. Louis, Missouri. EPA Region 7 Fact Sheet, 2 p.

Lutzen, E.E. and Rockaway, J.D., Jr. (1989) Engineering geologic map of St. Louis County, Missouri. Missouri Dept. of Natural Resources, OFM-89-256-EG.

Miller, D.E., Emmett, L.F., Skelton, J., Jeffery, H.G., and Barks, JH. (1974) Water Resources of the St. Louis Area, Missouri. Missouri Geological Survey and Water Resources, Water Resources Report 30, 114 p.

NGS (2001) http://www.ngs.noaa.gov/cgi-bin/utm_getut.prl

NOAA (1995) Use of the "NAD/WGS 84" Datum Tag on Mapping Products. Federal Register, v. 60, no. 157, August 15, 1995 Notices

Osburn, G.R., Criss, R.E., and others (2001) Maps of Mud and TRC Caves, in progress.

Thompson, T.L. and Robertson, C.E. (1993) Guidebook to the geology along Interstate 44 (I-44) in Missouri. Missouri Dept. of Natural Resources, Report of Investigations no. 71, 185 p.

Tucker, R.D. and Criss, R.E. (1999) Map of the Bushburg Sandstone at Tyson Research Center; unpub.

Vandike, J.E. (1995) Surface water resources of Missouri. Missouri Dept. of Natural Resources, Water Resources Report no. 45, 122 p.

Vineyard, J.D. (1967) Physiography; in Mineral and Water resources of Missouri, v. 43, p. 13-15.

Whitfield, J.W. (1991) Bedrock geological map of the House Springs 7 1/2 quadrangle, Jefferson County, Missouri. Missouri Dept. of Natural Resources, OFM-91-263-GMR.

I thank Dave Schilling, Dave Larson, Owen Sexton, Earl Biffle and Jane Walker for sharing their extensive knowledge of TRC. Prof. Robert Tucker and Bob Osburn contributed numerous insights when they helped me teach geological field mapping and cave mapping classes that included several exercises at TRC. Jim Emory and Tom Hughes provided helpful information about Lone Elk and West Tyson County Parks. Evan Kifer at DNR provided many well logs, and Gary Wilson of the USGS provided areas for several basins. I have also benefited from field discussions with Philip Moss and Tom Aley of Ozark Underground Laboratory, and from collaborations with my graduate students Chris Frederickson and Bill Winston.

The Tyson Research Center is located on the Burlington Escarpment which marks the boundary between the Ozark Plateau's Physiographic Province and the Central Lowland Province.

References:

Davis, W. C. (Ed.) 1962. Geology and Soils Manual. Mo. State Highway Comm. Geology and Soils Section, Jefferson City, Mo.

Depke, T. J. 1973. Geology of the Manchester Quadrangle. Unpublished MS dissertation Washington University, St. Louis, Mo.

Lutzen, E. E. & Rockaway, D. H. 1971. Engineering Geology of St. Louis County, Mo..Missouri Geological Survey and Water Resources, Engineering Geology Series #4.

[Contributed by Kenneth G. Brill, Jr.]