Hydrology and model study of the proposed Prosperity Reservoir, Center Creek Basin, southwestern Missouri
<p>A dam and reservoir have been proposed for construction on Center Creek, Jasper County, in southwestern Missouri. Ground-water levels in the hills…
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/ AD-A089 782 HYDROLOGY AND MODEL STUDY OF THE PROPOSED PROSPERITY RESERVOIR, CENTER CREEK BASIN, SOUTHWESTERN MISSOURI E. J. Harvey, et al U. S. Geological Survey Rolla, Missouri June 1980 QE U58w no.80-7 U.S. DEPARTMENT OF COMMERCE National Technical Information Service
XIBRARY OCT 05 19a1 guresu of Reclamation Denver, Colorado
Bureau Of Reclamation Denver Library
HYDROLOGY AND MOIEL STUDY OF THE PROPOSED PROSPERITY RESERVOIR, CENTER CREEK BASIN, SOUTHWESTER MISSOURI eleraifflElliE0
owe : ' to' U. S. GEOLOGICAL SURVEY Wottr-Rescurces Investigations 8O-7 Prepared hi cooperation with U. S. Army Corps of En's 5ISTRI3UTION sTATEmarr A Approved for pubto releano; aution Unlimited
1. REPORT NO. 1 3. Reciprient's Acc,p7sicr No. REPORT DOCUMENTATION 4. Title and Subtitle 1 5. Report Date HYDROLOGY AND MODEL STUDY OF THE PROPOSED PROSPERITY RESERVOIR, dune 1980 CENTER CREEK BASIN, SOUTHWESTERN MISSOURI 7. Authors) 8. Performing Organization Rept. No. E. J. Harvey and L. F. Emmett A :19. Performing Organization Name and Address 10. Project/Task/Work Unit No. U.S. Geological Survey. Water Resources Division 11. Contract(C) or Grant(G) No. 1400 Independence Road, Mail Stop 200 Rolla, Missouri 65401 (C) (G) 12. Sponsoring Organization Name and Address 13. Type of Report & Period Covered U.S. Geological Survey, Water Resources Division Final 1400 Independence Road, Mail Stop 200 Rolla, Missouri 65401 15. Supplementary Notes Prepared in cooperation with U.S. Army Corps of Engineers , .16. Abstract (Limit: 200 words) A reservoir has been proposed on Center Creek, Jasper County, southwestern Missouri Ground-water levels in the limestone uplands adjacent to the reservoir will rise when the impoundment is completed. The site is a few miles upstream from the Oronogo-Duenweg belt in the Tri-State zinc district. Grove Creek joins Center Creek downstream from the reservoir separating it from the mining belt. A model study indicates water-level rises varying from about 20 feet near the reservoir to 0.5 to 1.0 foot in the southern part of the Grove Creek drainage basin. A significant rise in the water table adjacent to the reservoir could increase mine-water discharge if Grove Creek is not an effective drain. However, it is probable that Grove Creek is an effective drain, and that higher ground-water levels in the reservoir area will increase ground-water discharge to Grove Creek, and in turn, Center Creek. The increase in ground-water discharge to Grove Creek will have the beneficial effect of diluting mine-water discharge from the Oronogo-Duenweg belt during periods of low flow. 17. Document Analysis a. Descriptors *Missouri, *Mine drainage, *Multiple-purpose reservoirs, *Karst, Ground water, *Hydrologic model, Underground streams, Limestone. b. Identifiers/Open-Ended Terms Tri-State Mining District, Oronogo-Duenweg Belt, Springfield Plateau, Center Creek, Jasper County. c. COSATI Field/Group 18. Availability Statement 119. Security Class (This Report) 21. No. of Pages No restriction on distribution UNCLASSIFIED 20. Security Class (This Page) 22. Price UNCLASSIFIED See ANSI—Z39.18) See Instructions on Reverse OPTIONAL FORM 27 (Formerly NTIS-35) Department of Comn
HYDROLOGY AND MODEL STUDY OF THE PROPOSED PROSPERITY RESERVOIR, CENTER CREEK BASIN, SOUTHWESTERN MISSOURI BY E. J. HARVEY AND L. F. EMMETT U.S. GEOLOGICAL SURVEY Water-Resources Investigations 80-7 Prepared in cooperation with U.S. Army Corps of Engineers June 1980
UNITED STATES DEPARTMENT OF THE INTERIOR CECIL D. ANDRUS, Secretary GEOLOGICAL SURVEY H. William Menard, Director For additional information write to: ' U.S. Geological Survey 1400 Independence Road Mail Stop 200 Rolla, Missouri 65401
CONTENTS Page Conversion factors Abstract Introduction Earlier work Hydrogeologic setting Transmissivity variation d Well construction Well yields Potentiometric mapping Grove Creek Quality of water Digital simulation model Finite-difference grid Boundary conditions and hydraulic stresses Aquifer properties Calibration of the model Summary and conclusions References cited ILLUSTRATIONS Figure 1. Map of Center Creek basin showing location of proposed reservoir, mine dumps, springs, and sinkholes 2. Geologic map of Jasper, Lawrence, and Newton Counties, Missouri. Geology from State geologic map of Missouri (Anderson, 1979) 3. Longitudinal geologic section of Spring River, Center Creek, and Turkey Creek basins, Missouri 4. Geologic cross sections in the vicinity of proposed Prosperity Reservoir 5. Map showing distribution of Pennsylvanian rocks in the Joplin area 6. Map showing brecciated zones and mines in a part of the Joplin District, Missouri
ILLUSTRATIONS Page Figure 7. Map showing well locations, depths, and water-level altitudes in sec. 7, T. 27 N., R. 31 W., Jasper County, Missouri 8. Map showing yields of wells completed in the Mississippian limestone in southwest Missouri 9. Potentiometric map of Mississippian limestone aquifer in Center Creek basin and contiguous parts of Spring River and Shoal Creek basins, Missouri, 1978. (Contour interval, 25 ft) 10. Potentiometric map of proposed Prosperity Reservoir area in Center Creek basin, Missouri, 1965. (Contour interval, 25 ft) 11. Potentiometric map of proposed Prosperity Reservoir area in Center Creek basin, 1978. (Contour interval, 10 ft) 12. Map showing wells sampled in 1965, 1976, and 1978, and springs sampled in 1978 in Spring River, Center Creek and Shoal Creek drainage basins, Missouri Map showing variation in nitrate content in water from wells in Mississippian limestone 14. Map showing observed and computed head change (1965-78) for the Oronogo-Duenweg area, and projected head change that may occur due to Prosperity Reservoir 15. Graph showing simulation of hydrograph Graph showing computed increase in storage due to construction of Prosperity Reservoir
TABLES Table 1. Generalized section of geologic formations in the Joplin area, Missouri v--
2. Water-quality data for wells and springs in Center Creek basin, Missouri 3. Comparison of analyses of water samples collected in 1965, 1976, and 1978 from Mississippian wells in the Joplin area, Missouri 4. Summary of mine discharges represented in the model Page
CONVERSION FACTORS For use of those readers who may prefer to use metric units rather than inch-pound units, the conversion factors for the terms used in this report are listed below. Multiply inch-pound units foot (ft) square foot per day (ft2/s) foot per second (ft/s) cubic foot per second (ft3/s) gallon per minute (gal/min) inch (in.) mile (mi) square mile (mil) By 3.048)(10 To obtain SI units meter (m) square meter per day (m2d) meter per second (m/s) cubic meter per second (m3/s) cubic meter per day (m3/d) millimeter (mm) kilometer (km) square kilometer (km2)
Hydrology and Model Study of the Proposed Prosperity Reservoir, Center Creek Basin, Southwestern Missouri By E. J. Harvey and L. F. Emmett ABSTRACT A dam and reservoir have been proposed for construction on Center Creek, Jasper County, in southwestern Missouri. Ground-water levels in the hills adjacent to the reservoir will rise when the impoundment is completed. One of the problems is that the proposed site of Prosperity Reservoir is a few miles upstream from the lead-zinc mining area known as the Oronogo-Duenweg belt. In this belt transmissivities are variable but appear to be higher than they are in the immediate area of the reservoir. Grove Creek lies down-gradient from the reservoir area and separates it from the mining belt. A model study indicates that inflow from the proposed reservoir to the water table could cause water level rises varying from about 20 feet near the reservoir to 0.5 to 1.0 foot in the southern part of Grove Creek drainage basin. These rises will cause significant changes to the natural ground-water flow system. Increased ground-water elevations in the reservoir area could result in increased ground-water gradients and discharge to Grove and Center Creeks. The increase in ground-water discharge to Grove Creek, and in turn Center Creek, will have the beneficial effect of diluting mine-water discharge from the OronogoDuenweg belt during periods of low flow. However, if Grove Creek does not act as an effective drain and if conduits extend beneath Grove Creek to transfer the increased water available to the Oronogo-Duenweg belt, the flow regimen could change in the mining belt west of Grove Creek increasing mine-water discharge to Center Creek downstream from the reservoir. Bedrock in the area is Mississippian limestone, the deeply solutioned formation that contained the ore deposits. The limestone in the mining
district was greatly altered by solution prior to ore deposition while the limestone in the area of the reservoir was altered less. The extent of the alteration is related to the aquifer characteristics in that high and low values of transmissivity and storage coefficient correspond to greatly altered brecciated rocks in the mining district and less altered, less brecciated rocks in the reservoir area, respectively. The authors suggest that an ancestral east-flowing White River drained the area about Joplin in Late Mississippian time. This is based on the configuration of the contact between Meramecian and Osagean rocks of Mississippian age. A high topographic area existed in the region about Joplin in which the water table stood 200 feet below the land surface when sinkholes and caverns of that depth were formed. The large number of Pennsylvanian-filled sinkholes in the Joplin area and the smaller number to the east suggest a higher land surface to the west than that to the east. The distribution of paleokarst sinkholes supports the conclusion based on the configuration of the Meramecian-Osagean contact. INTRODUCTION The work was undertaken at the request of the Corps of Engineers to describe the hydrology of the Mississippian aquifer, to assess the possible effect of a change in the ground-water regimen on the old Oronogo-Duenweg lead-zinc mining belt downstream from the proposed site of the Prosperity Reservoir, and to determine whether Grove Creek is an effective drain for the area east of the creek. This report includes a general description of the geology and hydrology of the Mississippian limestone aquifer in the Center Creek basin and contiguous areas,. and a detailed description of those features in the area of the proposed Prosperity Reservoir near Joplin, Mo. Figure 1 shows the Center Creek basin, the location of the proposed reservoir, Center Creek and adjacent basins and Oronogo and Duenweg, the principal center of mining in Missouri. The Joplin area as it is used in this report includes the area of Center and Turkey Creek basins from the Kansas line to the proposed reservoir area. The report includes results of a model study that shows rises in ground-water levels in the hills adjacent to the reservoir. The authors found the residents and landowners very helpful and friendly in supplying information about their water wells and their water supplies, and in allowing water-level measurements to be made. EARLIER WORK Much has been written about the lead-zinc deposits, their origin, and history of mining. It was not possible in the short time available for this
94° Od EXPLANATION Mine Dump Modern Sinkhole Proposed Reservoir ow Spring Drainage Divide ci) OKLAHOMA tM Monett ( SCALE ' fi t ' 10 Miles 16 kilometer! Base from U.S. Geological Survey in cooperation with Project Area the State of Missouri, I: 500,000 , 1971. 0:0 Figure I.-- Map of Center Creek basin showing location of proposed reservoir, mine dumps, and sinkholes.
study to review the literature adequately for historical information on the changes in ground-water and surface-water regimes in the area through a hundred years. A study (Feder and others, 1969) was made in 1963-65 of the hydrology of the Oronogo-Duenweg mining belt and the areas adjacent to it on the west. Later, a second study was made (Barks, 1977) to determine the nature of additions of metals from the Oronogo-Duenweg belt to Center Creek. The most comprehensive report available describing the Mississippian aquifer is the Joplin District Folio by Smith and Siebenthal (1907). Although their purpose was to describe the geologic history of the prepa ration of the rocks for mineralization and the occurrence of minerals in the deposits, the information and interpretation presented aid our present understanding of the hydrology. Brockie and others (1968, p. 400-430) have an extensive bibliography in their paper on the area. HYDROGEOLOGIC SETTING The geologic section for the area is given in table 1, the same as that used in Feder and others (1969), and Barks (1977). Most of the Mississippian section is limestone while the Cambrian-Ordovician section is dolomite. In Feder's report (1969, p. 7), he refers to the Mississippian limestone section as the shallow aquifer and the Cambrian-Ordovician dolomite section as the deep aquifer. In this report the shallow aquifer is called the Mississippian limestone. The emphasis in this report is on this aquifer. Basically, the rock section consists of small areas of Pennsylvanian sandstone and shale in outcrop surrounded by Mississippian limestone that is exposed over the remainder of the area. Below the Pennsylvanian the section consists of an average of 300 ft of Mississippian limestone separated from the underlying 1,400-ft thick section of Cambrian-Ordovician dolomite and sandstone by the 20- to 30-ft thick Lower Mississippian Kinderhookina Series which contains shale beds of the Northview Formation, the principal con fining bed between the Mississippian limestone and the Cotter Dolomite. Underlying the Cambrian-Ordovician section are Precambrian igneous and metamorphic rocks. Figure 2 shows the areal geology of the region. The main area of Pennsylvanian rocks is northwest of the project area. Outliers of Pennsylvanian rocks are scattered over the entire area becoming less frequent to the southeast. Many small deposits of shale and sandstone occur in sinkholes and cavern fillings in much of Jasper and Lawrence Counties, evidence of the development of an ancient karst topography.
Table 1.--Generalized section of geologic formations in the Joplin area, Missouri (from Feder and others, 1969) [The stratigraphic nomenclature generally follows that of the U.S. Geological Survey and the Missouri Geological Survey; however, there are some variations from the current usage of the U.S. Geological Survey.; Stratigraphic Thickness ?hysical Character Depth to Top of Water-bearing Character Unit Feet Formation, Feet , Alluvium Unconsolidated silt, Outcrop Yields small supplies for domestic 1 sand, and gravel and stock use i a rg. g 0 z o az 75 Lu Z PENNSYLVANIAN Desmolneslan 0-100+ Shales and sandstones with beds of coal Outcrop Yields little water to shallow dug wells Ca g . e ; o Carterville Formation Limestones, shales, and siltstones; generally found Outcrop to 50 Does not yield water to wells U filling depressions in underlying rocks Warsaw Dense limestone with Outcrop to 150 Yields little water except in Formation soma chart isolated solution channels E Burlington Dense cherty limeOutcrop to 300 Yields little water where massive, and Keokuk stone, sometimes but can yield over 100 gpm in Limestones mineralized with brecciated areas. zinc and lead Solution channels may yield large Shallow Aquifer supplies Generally yields adequate supply for domestic and stock use, rarely over 50 gpm. Supplies many springs Generally yields adequate domeutic MISSISSIPPIAN Elsey 30+ Fine-grained, very Outcrop to 450 Formation cherty limestone; sometimes all chert and mineralized with g zinc and lead :., Reeds Spring Dark, very cherty, Outcrop to 500 o . Formation argillaceous limeor stock supply. Supplies many stone; sometimes springs mineralized with zinc and lead Pier'Bon Cherty dolomitic Yield. very small quantities of water Formation limestone in upper portion; silty dolomite in lower portion Northview Shale or shaly lima125-625 Confining bed Formation stone; absent in parts of the area Compton Shaly limestone Generally does not yield water Formation Bachelor Sandstone Does noc yield water to wells Formation uoplootpepulm Chattanooga Fissile, black, Confining bed Z Shale carbonaceous shale;
absent throughout most of area Cotter 200± Cherty dolomite; ' Yields small quantities of water Dolomite some sandstone beds Jefferson City 200± Cherty dolomite Yields small quantities of water Z Dolomite Upper Lower ti
et Roubidoux 175± Cherty dolomite 550-1,000 Generally yields good supply of Formation and several water; moat suppliea between 50-150 sandstone beds gpm Gasconade 300+ Cherty limestone 700-1,l50 Yields small suppliea of water Dolomite and dolomite; sandstone bed at bottom of formation sr Eminence and 200+ Dolomite with druay chert 1,000-1,450 a. Generally yields good supply of water, Potosi Dolomites in lower 50 feet : especially from lower portion; between 50-400 gpm z Derby-Doerun, 150± Silty dolomites; some 1,200-1,650 Yields mall quantities of water ti Davis and siltstones and shales Bonneterre Formations cm as a undifferentiated Lamotte Sandstone Quartzose sandstone 1,350-1,750 Yields vary considerably. Formation may be absent over Precambrian highs PRECAMBRIAN Granites and rhyolites 1,350-1,850 Generally does not yield water
94" Od SCALE 10 miles O ie) o,s,..0 O 16 kilometers /0 0...11 ok -rAz g Air."1: Carthag
River Webb City Center Mt. Verno PROPOSED RESE RVOIRrSarcoxie Oil 3 7° Fault
Ma ‘PWA
EXPLANATION PENNSYLVANIAN Cherokee Group Neosho , Carterville Formation Meramecion Series MISSISSIPPIAN Osagean Series Kinderhookian Series ORDOVICIAN Cotter and Jefferson City Dolomites U, up thrown side V— Fault D, downthrown side Contact (dashed where inferred) Figure 2.-- Geologic map of Jasper, Lawrence, and Newton Counties, Missouri. Geology from State geologic map of Missouri (Anderson, 1979)
While figure 2 shows the areal distribution of the outcropping geologic formations, the cross section (figure 3) shows the general attitude of the principal units involved in the discussion, and figure 4 shows in greater detail the attitude and thicknesses of the Mississippian formations. The average dip of the rocks is 4° northwest. The cross sections also show the re'ation of the potentiometric surfaces of the Mississippian limestone and the Cambrian-Ordovician dolomite section. In table 1 the Elsey Formation is listed and replaces the Grand Falls Formation, the name used in figure 4. Grand Falls Formation and Elsey Formation are not exact equivalents (Robertson, 1968, p. 7). Although the name Grand Falls has been retired from common usage in favor of Elsey, logs used in the cross section show Grand Falls because these wells were logged many years ago on the basis of studies of insoluble residue. Rather than relog the wells, it was expedient to use the old terminology in the cross sections for this report. Similarly, the name Fern Glen Limestone appears in many of the logs and the cross sections (fig. 4) and is the approximate equivalent of the Pierson Formation given in table 1 (Howe, 1961, p. 59-63). Devonian rocks represented in southwest Missouri by the Chattanooga Shale are not recognized in logs in the project area. Where recognized to the south, the Chattanooga is generally 5-10 ft thick. The Cambrian-Ordovician section of dolomite and sandstone is present everywhere in the subsurface, is about 1,400 ft thick, and is the source of water for many of the towns, rural households, and industries. The main part of the section is dolomite, sandstone is minor, and the only shale (Davis Formation) of any consequence as a confining bed is near the bottom of the section. Most large-capacity wells do not penetrate the Davis Formation. Most domestic wells completed in the Cambrian-Ordovician section stop in the upper part of the section 100 or so feet below the Mississippian, whereas industrial and municipal wells, which generally have higher yields, penetrate all or most of the section. Dissolution of limestone has greatly influenced the geomorphic history and hydrology of the area over a long period extending back to the time when the limestone was deposited. It is evident in the distribution of Pennsyl vanian rock in the Mississippian outcrop area near Joplin where sinkholes were formed principally at the close of deposition of the limestone. The sinkholes were filled by sandstone, shale, and coal of Pennsylvanian age. Across Jasper County east into Lawrence County, sinkholes filled with Pennsylvanian rock occur, but are few in comparison to the many in the Joplin area. They are shown in the Joplin District Folio by Smith and Siebenthal (1907), on the geologic maps showing mining and mineralized areas (Missouri Geological Survey and Water Resources, 1922), and on the Lawrence County geologic map by Rutledge (1929). Their abundance in the Joplin area and their relative scarcity east of Grove Creek attest to
TURKEY CREEK BASIN CENTER CREEK BASIN --- SPRING RIVER BASIN GOO - t3 &EV — I CENTER COE. CaL - 1I51119S1 AN 5USEACL TO AO ID 30.6 B plogo40ww, TO 326 eon MISSISSIPPIAN ORDOVICIAN TOGO TO 4G TO 660 TO NO a .0. EXPLANATION ,.„ LOWER ORDOVICIAN PaIS rept A.L1. TIOME.T 14. BUlotrACE o TO Ms ctraerraZtAl=".= . to est TO GOO TO GOO TO GTO UPPER CAMBRIAN HORIZONTAL SCALE a TOTAL DEPTH OF 11 HOLE BELOW LAND SURFACE gl* LOCAT ION MAP a VERTICAL SCALE Greatly Etogoratod TO GO Figure 3.-- Longitudinal geologic section of Spring River, Center Creek, and Turkey Creek basins, Missouri
A l g 1200 a' ,-Ordovician '3 1200 (-Mississippian Potentiometric E Potenfiometric Surface Surface Compton ORDOVIIA EXPLANATIO Cotter- Jefferson City Dolomites T.D. 1250 ft. Casing T.D. 815 ft Mine T.D. 805 ft. T.D. 1865 ft. T. D. Potentiometric Total Depth Paten tiometric B aE Surface Mississippian Potentiometric datum of 1929. a) CD Surface Keokuk-Burlington Limestor-irxt,agelhiRkft..Ngh. cp Compton Nor thview ORDOVICIAN Casing-1 T.D. 1402 ft. Cotter - Jefferson City Dolomites T.D. 1473 ft. 852 ft. Z T'D' C C E
.co= 'a 117) CI rdovician 0 , — Center Creek - 4- 1200 (-)() 0 Surface a)2 Potentiometric /- Mississippian Potentiometric Cr o, su o c -o a.) / Sur face o)
0 c7) a 0 z 4C7riCv.
a) 1000
. /7Gran Compton / (17 ORDOVICIAN
// ,, Cotter- Jefferson City Dolomites Nor thview T.D. 852 ft. T.D. 1.228 ft. Casing- 1 Orono q.
Carthage T. D. 1335 ft. T.D. 1415 ft. O 1mile
94° 00' A O I kilometer Horizontal Scale U) Creek Vertical Scale: Greatly Exagerated ,.Joplin U) Duenweg Diamond 37° 00' OKLAHOMA C' EII A George Washington Carver National Monument 10 miles 16 kilometers SCALE Figure 4.-- Geologic cross - sections in the vicinity of proposed Prosperity Reservoir
the different levels of dissolution activity in the area at the time of their formation. The distribution of modern unfilled sinkholes on the Springfield Plateau and on the Salem Plateau to the east parallels the ancient distribution of Pennsylvanian-filled sinkholes, a paleokarst. Great clusters of ancient sinkholes (paleokarst) are surrounded by areas of few or no sinkholes just as clusters of modern sinkholes are surrounded by areas devoid of them. Sinkholes are the surface evidence for an underground drainage system where permeability can be expected to be relatively great. In the Joplin mining district the system of caverns developed by solution is the locus of mineral deposits. These have been described in great detail by Smith and Siebenthal (1907), and others. Modern unfilled sinkholes are uncommon in the Joplin area. New (1956-72) 71/2-minute, 1:24,000 scale topographic maps having a contour interval of 10 ft have been examined for sinkholes. The distribution is shown in figure 1. The few that are found in the Shoal Creek-Center Creek-Spring River basins seem to lie along northwest trends that cross the three basins. Approaching the Pennyslvanian outcrop the number of modern sinkholes diminishes showing that the Pennsylvanian forms a protective cover retarding limestone solution since the deposition of the Pennsylvanian. This distribution contrasts with that which existed in Late Mississippian time when the Pennsylvanian cover did not exist and solution was active prior to ore deposition (Smith and Siebenthal, 1907, p. 8). The geologic history of the Mississippian and Pennsylvanian Periods influenced the development of permeable areas in the Mississippian limestone in which the proposed Prosperity Reservoir is located. The events of most importance to the development of the present hydrologic properties of the limestone extend from the Mississippian Period into the Pennsylvanian Period. At the close of Meramecian deposition in Late Mississippian time drain age may have been to the east through an ancestral White River that perhaps rose in Kansas and Oklahoma. The river eroded the limestone of the Meramecian and Osagean Series leaving the fluted appearance of the Meramecian-Osagean contact somewhat as we see it today. (See fig. 2). The Hrainage system established by the ancestral White River has practically disappeared, replaced by the present (1979) system discharging to the west. The Meramecian-Osagean contact is a vestige of the earlier system. During this period the Joplin area was topographically higher than the area to the east. In the area around Joplin, karst topography began to develop. Sinkholes became abundant. Submergence followed this erosion interval and the Carterville Formation of the Chesterian Series was deposited. Emergence from the sea at the close of the Mississippian resulted in the removal of most of the Carterville and
only those deposits protected in sinkholes and a few scattered outcrops remain as evidence. Smith and Siebenthal (1907, p. 5) report that remnants of the Carterville Formation at depths of 200 ft in sinkholes are evidence of the depth to which solution was active and that the water table must have been close to that depth (Smith and Siebenthal, 1907, p. 8). Erosion contimed well into the Pennsylvanian Period. Submergence occurred again in the Pennsylvanian Period. The area was inundated from the west and layers of sand, clay, coal, and a minor amount of limestone were laid down. Sediments were deposited along trends which marked lines of connected sinkholes, similar to the lost rivers of modern cave regions (Smith and Siebenthal, 1907, p. 7). Valleys developed before Pennsylvanian time when drainage was toward the east or southeast and later toward the northwest were filled with Pennsylvanian sediment following the epeirogenic movements referred to by Smith and Siebenthal. Grove Creek lies near the eastern margin of the area so severely affected by underground solution. This is also shown by the contrast in abundance of Pennsylvanian-filled sinkholes in the west and comparative paucity in the east. Figure 5 shows the distribution of Pennsylvanian sedimentary rocks in a part of southwest Missouri. The map was adapted from the geologic map in the Joplin District Folio (Smith and Siebenthal, 1907), the geologic map of Lawrence County and parts of Jasper and Newton Counties (Rutledge, 1929), and a geologic map of the Granby area (Buckley, 1906). Some areas of exposure of Pennsylvanian rocks are outliers, but many of the small circular outcrops are in sinkholes. The long linear outcrops are in collapsed valleys. Only field examination can determine which deposits east of Grove Creek are sinkhole exposures and which are merely outliers. Features of karst topography in addition to sinkholes indicative of limestone solution are springs, caves, and losing streams. The large increases in springflow to Spring River, Center Creek, and Shoal Creek are principally in Lawrence and Barry Counties (fig. 2) in the eastern parts of the three basins (Harvey and Maxwell, 1965; Feder and others, 1969). Yet, in this eastern area where springs are plentiful and moderately large, wells in the Mississippian limestone as a rule yield little more than enough for a domestic water supply. In the west, near Joplin, springs are very few and very small. Yet, the chance of obtaining more than 100 gal/min in the Joplin area is considerably enhanced, as several such wells exist, while none is known farther to the east. Thus the spring development is a later one, while the contrast in well yields is the result of paleokarst develop ment. Grove Creek and the area in which the proposed reservoir is situated lies near the boundary of the great, ancient karst development of the mining district. It has some of the characteristics of a modern karst. Grove Creek
94° 15' 940 45' I 37° 15' 37°15' I O Creek e- 4,.., v, 4,0 , , t e t. 6 ,Vz*": . % 0e .„ cb e e a .11 g ‘1". 0 a
,it PROSPERIT f 44z4 % -; '. RESERVOIR 37° 00 37° 00' 94° 45' Base from Joplin District, Mo-Ka. Adapted from Smith & Siebenthal, 1906 94° 15' SCALE EXPLANATION 5miles 8 kilometers Pennsylvanian Rocks Figure 5.-- Distribution of Pennsylvanian rocks in the Joplin area
is a losing stream in its upper reaches. (See the tabulation of flow estimates in a later section of the report.) Scotland Spring (fig. 1) situated on Grove Creek is supplied by a network of conduits in the limestone extending to the east and south. Grove Creek changes at Scotland Spring from a losing to a gaining stream and perennial flow continues to the mouth. If all the water disappearing in the losing reach reappears in Scotland Spring, then Grove Creek can be considered an effective drain despite its upstream losing reach. The longitudinal profile (fig. 3) extends from the Chesapeake fault zone in Lawrence County to the state line. The Northview Formation which occurs near the base of the Mississippian limestone is 5 to 10 ft thick and is reported in most of the well logs used in the section. The profile of the potentiometric surface of the Cambrian-Ordovician section lies as much as 200 ft below the water table or potentiometric surface of the Mississippian limestone. In this longitudinal section as in the cross sections, the potentiometric surface of the Mississippian limestone follows the topography, whereas the potentiometric surface of the Cambrian-Ordovician has a more uniform westward slope. At Spring River in Lawrence County and near Sarcoxie the two potenti ometric surfaces are coincident. This suggests that in these two areas local recharge to the Cambrian-Ordovician aquifers occurs despite the presence of the Northview Formation. The potentiometric surface in the Mississippian limestone slopes with some irregularity from east to west and intersects Spring River and Center Creek at several places, and Grove Creek. From a point west of Spring River the surface slopes uniformly west to Sarcoxie. Comparison of the profile with the potentiometric map (see fig. 9) shows that the profile approximately parallels contours on the potentiometric map and the map shows that ground water movement is toward Spring River north of the divide. Because of the perspective the profile does not correctly portray the local direction of ground-water movement. Three cross sections of Center Creek basin compare the hydrology of the Mississippian limestone and the Cambrian-Ordovicain section (fig. 4). The prominent features of the three sections are the following: 1. There is always a separation between the water table of the Mississippian limestone and the potentiometric surface of the Cambrian-Ordovician section and it varies from 50 ft on the south to as much as 200 ft on the north. The proximity of the two surfaces in some parts of the area as indicated on the cross sections may be due in part to the local absence of the Northview Formation. In the absence of the retarding effect of the shale, vertical leakage from the Mississippian limestone to the Cambrian-Ordovician aquifer is less impeded. Pumping from the Cambrian-Ordovician aquifer at such centers as Carthage and Webb City increases the difference.
2. The water table of the Mississippian limestone follows the topo graphy whereas the potentiometric surface of the Cambrian-Ordovician does not. The Mississippian grossly exhibits a water-table condition; the Cambrian-Ordovician exhibits an artesian condition. 3. The general direction of ground-water movement in both the Missis sippian and Cambrian-Ordovician is toward the north and the west. 4. The Mississippian limestone water table is uniform while following the topography in the two sections (AA' and BB') upstream from the Oronogo-Duenweg belt and uneven in the mining belt (CC'). The irregularity in the mining belt is the result of local recharge and bonding of water behind collapses in the abandoned mine workings. Transmissivity Variation An overlay of the mines and breccia areas (fig. 6) shows their distrib ution in the Joplin district. The areas of widespread brecciation and mineralization were outlined as areas of high transmissivity for the model. The Oronogo-Duenweg belt is such an area. Areas devoid of brecciation or with significantly less brecciation were assigned a low transmissivity value. In a general way, the variation in well yield corresponds with the distrib ution of breccia areas. While the mines represent a completely altered flow system, the mines" are not continuously connected from south to north. In the north the mines are more connected than they are in the south. However, the breccia areas are more extensive and more continuous than the mines and they would tend to serve as an avenue for the lateral movement of water between mines. The breccia areas are not continuous throughout the belt and are more discontin uous toward the south than toward the north. If the areas between the breccia areas are dense limestone, locally called "lime bars," then three components make up the flow system: (1) the mines, (2) the breccia areas, and (3) the lime bars. The mines should have an extremely high transmissivity, perhaps close to infinity. Rock falls in caved areas will reduce the transmissivity. Breccia areas will have a variable transmissivity depending on the amount of secondary silicification and dolomitization of the limestone and chert breccia. If the voids were completely filled by secondary minerals, the tranmissivity would be low. On the other hand, if the voids were not filled the transmissivity could be high. The lime bars are limestone with fractures and bedding planes more or less opened by dissolution. If not altered by dissolution, the transmissivity can be extremely small. If opened, the transmissivity can be somewhat more.
Adapted from Missouri Geological Survey, 1942. LOCATION MAP SCALE EXPLANATION 4 Miles 34.Or Brecciated Zone Kilometers 0° Mine Workings er ICI mats 5 d kdometar Figure 6.-- Brecciated zones and mines in a part of the Joplin District, Missouri
WELL CONSTRUCTION Weathering of the limestone varies greatly in short distances. The availability of water at shallow depth also varies in short distances. A well drilled 270 ft deep at A (fig. 7) in sec. 7, T. 27 N., R. 31 W., about 3 mi southeast of the proposed reservoir was abandoned because of mud- and water-filled pockets. A new site was selected 15 ft east of the abandoned site (B, fig. 7) where 156 ft of casing was set in the completed well and the total depth was 323 ft. This well stopped in the Ordovician. Two wells at C (fig. 7) stopped at 159 and 118 ft with 45 and 52 ft of casing, respectively. Figure 7 shows well depths and altitudes of water levels in the wells measured in the spring of 1978. These wells illustrate three conditions: An open section supplying adequate water from the main body of the limestone, which has a normal weathered section (wells at C); a weathered section yielding insufficient water (well at A); and a weathered section through the entire thickness of the limestone requiring drilling to the Ordovician (well at B). The location of section 7 is shown in figure It appears that in many parts of the area investigated, even in an area of 1 mil or less, conditions in the limestone are so heterogeneous and weathering.may be so deep that it is necessary to drill into the underlying Ordovician. On the other hand, in places a well can be made at less than 100 ft or 150 to 250 ft in the limestone. In some instances no well can be made in the limestone because it is tight (as at B, fig. 7). Yet, even though weathering to great depths may occur in proximity to hard, tight areas, enough wells completed in the Mississippian exist so that a potentiometric surface can be mapped. Water in the Mississippian is probably confined in many places, but unconfined throughout most of the area. Rather extensive areas of several square miles exist in the uplands where all of the wells range from 150 to 200 ft deep. In the Center Creek basin, many of the wells required only a minimum depth of casing, 20 ft. Some required an abnormally great depth of casing, 100 to 200 ft. Apparently when abnormally long lengths of casing are required, the wells are in recharge areas. These may be at joint inter sections where solution has progressed far. WELL YIELDS Yields of wells completed in Mississippian limestone range from nearly zero to 400 gal/min according to owners' and drillers' records. Figure 8 shows the distribution of values across a large part of southwest Missouri extending from Springfield to McDonald County. Wells drilled to the Cambrian-Ordovician aquifer but open in the Mississippian are not included. The following table presents the ranges, median, and average values of the yields by areas.
Number Block (fig. 8) Description of values Range (gal/min) Median (gal/min) Average (gal/min) East of Chesapeake Fault Chesapeake-Pierce City fault block (mainly Lawrence County) Joplin-Sarcoxie area (Jasper and northern Newton Counties) South of Pierce City Fault 1/2-130 On the basis of the variation in well yield a higher value for transmissivity was assigned in the model analysis in parts of Jasper County than that in the area to the east. Brecciated limestone often associated with zinc has higher permeability where the voids have not been filled with secondary minerals (jasperoid, dolomite, and sulfides). The field inventory which supplemented data from the log file showed that even in the area around Joplin where it is possible to obtain 100 gal/min or more of water from the limestone, limestone of very low permeability exists in which little or no water was obtained. POTENTIOMETRIC MAPPING Three potentiometric maps are included in the report. Figure 9 is a map of the entire Center Creek basin and contiguous areas in the Spring River and Shoal Creek basins. All water levels measured and reported are shown on the map. A 25-ft contour interval was used, which generalized variations in slopes of the potentiometric surface.
el 100 A B 2709)(323 175M 118 Co' — Sec. 7 SCALE 1000 ft. 300 meters no s it 1035 NOTE: EXPLANATION See figure II for location with respect Depth of well 1035 Altitude of water level, March, April, 1978 to the reservoir. MISSISSIPPIAN WELL 444 Depth of well — 7- - - Altitude of .water level, March, April, 1978 ORDOVICIAN WELL Figure 7.-- Well locations, depths and water-level altitudes in section 7, T. 27 R. 31 W., Jasper County, Missouri
- R-33-W I R-2I-W I
BARTON1 JASPER so z DADE I
cn N I '45 '20 Carthage
*20 '15
GREENE Springfield .1 °I5 . .13 30 to '..,
V...5".2 .22 15. 2 30 .2 *35"
16. ' 2 5., 3 16 *30 14, p .P 3' 0. rt.°, 025 '5 38:20.., I0 30 '14 *16 0) cm CHRISTIAN o5 *20 37° Od 1 /40 -`Ct I E Pierce .6 City Fault "P LA‘RENCE STONE I Geology from Geologic map of ID I OP 5e
.2 *1.25 Neosho IS. *1830
'10
1
10° issIPPian Missouri, 1979. / / alen9, t. I MG TANEY I 1.67* 3'.15 20 5.:01 .12 8°. 12
EXPLANATION '10 Reported yield in gal/min. (P,.poor) 2 ,.0.5 0,1 000.02 C\I
Cossville (11 m l Drainage Divide Fault U , Upthrown side 0, Downthrown side N 0.5. "1, 5 0.5.0 5 20 5° *130 7. 1.75s ".75 MP 'nevi Ile *10 Mc DONALD e10°/ Go/ Block i) SCALE o lOmiles 01- 1-1-116 kilometers 34 TR-33-W 1 32 28 I 27 I 26 I R-23-W I ARKANSAS Figure 8.-- Yields of wells completed in the Mississippian limestone in southwest Missouri
R 34 W R 33 W R 32 W R 31W T 29 N T 28 N T 27 N KANSAS 37° 00' MISSOURI OKLAHOMA T 26 N BASE FROM U.S. GEOLOGICAL SURVEY Aaiun Cossvilk Joplin Dtstrlot Monett 909-90 91941-942 Neosho Ritchey 1909-910 8 I941 Rocky Comfort 1936 Er 1940-1941 Sarcose 191013 919 Stotts City 910 6 1919 T 25 N EXPLANATION Lake (Mine Pit) R 34 W R 33 W R 32 W R 31 N uses Mine Shoft LOCATION MAP 0.TO Mississippian Well Ordovician or Cambrian VIII Number is altitude of water level In feet, National Geodetic Vertical Datum of 1929, (r) indicates reported, (e) indicates estimated; all others measured between March and July 1978. Potentiometric contour shows altitude of potentiornetric surface, Contour interval 25 feet, National Geodetic Verficol Datum of 1929. 37° 00. Boundary of Center Creek Basin Proposed Reservoir Township Corners Figure 9.-- Potentiometric mcp of Mississippian limestone aquifer in Center Creek basin and
R 30 W R 29 W R 28 W R 27W R 26 W 94' OG 01,, T 29 N OWN 3,n3, T 29 N "050
:100
Mt Vernon 7 27 N ' , It /'",i6 '3° ' ,,,cI6., : ilb j , , , s. , 0,0, 370 CO'
',
,, ' ,4 *,i6, ' ...„c 5,i142 / , , , „. ,, / i
2"— 7 26 N T 25 N R 30 W -r01422r T 24 N R 28 W R 27W SCALE hikES 14 . i4LOFETERS contiguous parts of Spring River and Shoal Creek basins, Missouri, 1978. (Contour interval, 25 ft.)
oii 09c,. oe den
assr EXPLANATION %5 Mine Snuff Mississippian
CM Spring Weil Number is dqltude of water level In feet, Notional Geodetic Vertices/ Datum of 1929. 17) indicates fi.ing welt. Al! measurements mode in 1955 ano early 1966. /000 Rmentiometric contour snows altitude. of potentiometrk surface. Depression comoom nochured. Contour interval 10 feet Notional GeudeticVertical Datum of 1929. Cent., Crook Drayage Basin Proposed Reservoir LOCATION MAP lot BASE FROM U S. GEO'-06 Joplin District 1906. 37° Figure 10.-- Potentiometric mop of proposed Prosperity Reservoir ore(
'911 cIe 24,4 broao /cqo 101p too° - .-96b 1010 10;50 17: oo' SCALE 4 MILES 6 KILOMETERS in Center Creek basin, Missouri, 1965. (Contour interval, 25 ft.)
.926, oast. seso A g a2 EXPLANATION Lake (Mine Pit ). Mine Shot t o Mississippian Well Spring Number is attitude of water level in feet, Notional Geodetic Vertical Datum of /929. (r) indicates reported, (e) indicates estimated, (f) indicates flowing. All others measured between March ono July 1978. Potentiometric corm, stows aititude of potentiometric surfoce. Depression contours hachure:I. Contour intervol 10 feet, National Geodetic Vertical Datum of /929. Boundary of Center Greek Bosin 37. CO Proposed Reservoir Conservation Pool 973.5 feet elevation , Notional Geodetic Vertical Datum of 1929. Stream Gaging Site BASE FROM U.S. GEOLOGICAL SURVEY Joplin District Figure I I. -- Potentiometric map of proposed Prosperity Reservoir area
ovit. 0/0 goo Sozo aoic 1,7 oan so LOCATION MAP SCALE 4 MILES KLOAILM. O
-'6 Riiom ED , c.o. . t4,44.1 t 1 in Center Creek basin, Missouri, 1978. ( Contour interval, 10 ft.)
Maps based on data collected in 1965 and 1978 drawn with a 10-ft contour interval show in greater detail the changes in slope of the potentiometric surface (fig. 10 and 11). In addition, comparison of the two maps permits contouring of the change in water level between 1965 and 1978 illustrated in the figure shown in the section on "Digital Simulation Model." Ground water in the Mississippian limestone section essentially has a water-table configuration that is controlled by the principal streams drain ing the area. The water-table contours extend upstream along the major streams showing that ground-water flow is from the uplands to the stream. Where the ground-water contours cross the stream valley downstream from the point at which the surface contour with the same altitude crosses the stream, the water table is shallow and a perennial stream occurs, or, at least, flow is continuous until evapotranspiration uses up the water. This is the discharge area. If the ground-water contour crosses the valley upstream from the surface contour crossing,an intermittent stream occurs. This is the recharge area. In carbonate terrane one might expect streamflow -loss in recharge areas downstream from the beginning of perennial flow. Such reaches are not as common in the Mississippian limestone area of the Springfield Plateau as they are in the Cambrian-Ordovician dolomite area of the Salem Plateau farther to the east. This is because solution of the limestone has not been carried to the extreme that it has been carried in many parts of the dolomite area. This difference in solution development is reflected in the relief of the two areas. The authors have observed that in any system of carbonate rocks in the Ozarks the greater the dissection of the land surface, the less precisely the ground-water divides correspond' with the topographic divides. In some areas contours are evenly spaced indicating uniform movement of ground water toward the stream. In other areas the contours are closely spaced. Such areas of close spacing indicate a steep slope in the water table and restriction in the flow of water through the rocks. The restriction may be due to an areal change from open joints, fractures, and bedding planes allowing normal movement of water to a system in which openings are small or few, or filled with secondary minerals and movement is slowed. All wells measured and used for control points are shown on the map. However, some points were disregarded during contouring. Because most of the wells that were measured were in use, some residual drawdown may cause an abnormally low water level, especially if the yield is low and the water use had been large prior to the time of the measurement. It is always possible in such a suite of rocks that sufficient water for domestic use may occur at more than one depth. If vertical connection is poor between the several depths of occurrence of water, several different
water levels may be measured at a specific location. Yet, it was found in inventorying and measuring water levels that considerable consistency in the depths of wells and water levels occurred in some areas. Such areas were several square miles.-in extent. In other areas, depths and water levels were very inconsistent. This areal variation between consistent and inconsistent well depths and water levels is due to variations in the develop ment, or lack of it, of solution along the joints, fractures, and bedding planes. For these reasons, water-level contouring is subjective and the product is the best estimate of the investigator of the validity of the data with which he is working and his understanding of how ground water moves through fractured, dissolutioned rocks. Some wellsdrilled into the Ordovician and uncased through the Mississippian, have water levels that stand below the potentiometric surface of the Mississippian, which indicates that little water was available in the Mississippian at this site. Other wells drilled into the Ordovician, also uncased through the Mississippian, have water levels that differ little with the potentiometric surface of the Mississippian. A substantial contribution to the well from the Mississippian is indicated. Most domestic wells drilled into the Ordovician have only 20 to 50 ft of casing and the Mississippian limestone is open to the well. As a result the water level reco ded in many Ordovician dolomite wells is a composite of the Mississippian an Ordovician rocks. These wells were not used in contouring the poten iometric surface of the Mississippian limestone although they are shown on th- potentiometric maps (figs. 9 and 11). Comparison of t e distribution of brecciation (fig. 6) with the 1978 potentiometric map s ows some relationship between such distribution and changes in the slope of the potentiometric surface (fig. 11). For example, the broad area of hi h water levels in the vicinity of Duenweg is a recharge area encompassing ca ed-in mine workings. It is bounded on the east by noteworthy steepeninof the potentiometric surface toward Grove Creek. Steepening suggests gross change in the transmissivity to steep gradient and low transmissivity. The abutting of brecciated rocks ("hog chaw") by solid limestone ("li e bars") would account for pronounced gradient changes. East of Stoutts Branch is another area of high water levels. Bounding this area on the east is an area of steep gradient, essentially parallel to the area of steep g adient east of Duenweg. Immediately east of the point where the ground-wa er elevation is 1,042 ft (fig. 11), wells are drilled to 400 to 500 ft depth to obtain water from the Ordovician dolomite and sand stone. Drillers an well owners mention the existence of "lime bars" which are interpreted as reas where the Mississippian limestone is relatively tight and little or no water is obtained. Shallow and dug wells constructed years ago in tight reas have since been deepened or replaced as larger volumes of water we e needed. For this reason it is suggested that presence or absence of Missi sippian wells, occurrence of mineralized areas and
brecciated limestone, high and low yields of Mississippian wells, and distrib ution of gentle and steep ground-water gradients are related. Between brecciated limestone areas within the high transmissivity area of the Oronogo-Duenweg belt the limestone may be tight and low well yields may be obtained. Assignment of a high transmissivity to the Oronogo-Duenweg belt is a very general assumption. It is quite apparent that the Mississippian limestone is very heterogeneous and its transmissivity may change in short distances. Change in the slope of the potentiometric surface from Deunweg to Oronogo may be explained by rock falls in the abandoned mine workings that create partial bulkheads behind which pools develop. While continuous movement occurs from Duenweg northwest to Center Creek, variations in the rate of movement are indicated by changes in the slope of the potentiometric surface. This is not as apparent in figure 9 (contour interval 25 ft) as it is in figure 11 (contour interval 10 ft) and on the cross section, figure 4. GROVE CREEK The potentiometric map of the area of the proposed damsite and Grove Creek (fig. 11) shows that the water table slopes from the uplands east of Grove Creek to it and Center Creek. West of Grove Creek the water table slopes to Grove Creek. The stream is usually dry upstream from Scotland Spring except for a reach about 1 mi long extending from an elevation of 1,040 to 1,060 ft. In this reach under normal weather conditions flow usually occurs early in the summer near the lower end of the reach when the stream is dry downstream from that point to the vicinity of Scotland Spring. Willow growth occurs along the stream between elevation 1,040 ft and 1,060 ft (points A and B on fig, 11). Upstream from elevation 1,060 ft and downstream from elevation 1,040 ft willows are absent. In fact, the change from abundant willows to no willows at elevation 1,040 ft is abrupt, the change taking place in a distance of about 500 to 750 ft (points B and C on fig. 11). Flow estimates were made several times in the spring and summer of 1978 as given in the following table. Site designations (A-F) are shown in figure 11.
Flow estimates, 1978, in cubic feet per second Site Mar. Mar. Apr. May June July (fig. 11) A Pools B Flow Flow Flow D Flow 0,2 E Flow F Flow Remarks Along creek in field. Willows and pools absent upstream, present downstream in distance of about one-fourth mile. Highway FF. Flow between pools July 25. Willows, sedges, and rushes abundant. Six-hundred feet downstream from Highway FF. Willows, sedges, and rushes absent. County road bridge. April 28, pooled 750 ft downstream. July 25, no pools. Willows absent. 1-44 bridge. June 8 and July 25, no pools. No willows. Business 1-44 bridge. March 169 April 28, and July 25 no pools. No willows.
From the foregoing data Grove Creek is a losing stream between site B and Scotland Spring. It is likely that the upstream flow in Grove Creek (sites A-B) appears downstream in Scotland Spring. The ground water contours do not suggest loss to Turkey Creek basin or to the Oronogo-Duenweg belt unless a conduit or conduits carries the water in some direction other than that suggested by the contours. A dye trace is needed to confirm a connection between Grove Creek and Scotland Spring and the effectiveness, of Grove Creek as a hydrologic boundary. Water in storage in the Oronogo-Duenweg belt discharges to Grove and Center Creeks. The rise in ground-water levels caused by inflow from the proposed reservoir could range from about 20 ft near the reservoir to 0.5 to 1.0 ft in the southern part of the Grove Creek drainage basin. Any rise in ground-water levels should increase discharge of Grove Creek and Scotland Spring. The increase in ground-water discharge to Grove Creek will have the beneficial effect of diluting mine-water discharge into Center Creek at Mineral Branch during periods of low flow. If conduits extend beneath Grove Creek, on the other hand, increased flow into the mining belt might augment discharge of mineralized water from the belt to Center Creek downstream from the proposed dam. In the reach of Grove Creek upstream from Scotland Spring, the shape of the contours indicates that ground water is moving toward the stream. However, the relation between the ground-water elevation and the surface elevation at any point along that reach, except in the reach between A and B, indicates that the water table is below the streambed. The absence of flow in the reach between Scotland Spring and C that is receiving ground water from adjacent uplands is due to conductance of the water to Scotland Spring beneath the channel, probably through conduits in limestone. In the reach upstream from A, the ground-water contribution is so small that it can only satisfy evapotranspiration requirements and it is probably a normal dry tributary. QUALITY OF WATER Water in the Mississippian limestone is moderately hard and moderately mineralized. The major difference between 1965 and 1976 sampling on the one hand and 1978 sampling on the other, is the broader geographic distribution of samples throughout the Center Creek basin in 1978. Figure 12 shows the distribution of sampling sites in 1965, 1976, and 1978. No samples were collected from the Oronogo-Duenweg belt in 1978, whereas the majority of the samples of 1965 and 1976 were collected from the mining district. Analyses for 1965 are listed in Feder and others (1969, p. 75) and for 1976 are listed in Barks (1977, p. 38) and are not repeated here. Barks, 1977, p. 18) found that ground water from many of the mines contains more than 1,000 mg/L (milligrams per liter) dissolved solids, whereas wells usually contained much less than that amount. Mine water is a calcium sulfate
EXPLANATION Sampling Periods r,
® 1965 & 1976 O 1976 & 1978 94° 001 0",IS Spring (no. in table 2)
1978 (no. in table 2) —a—Drainage Divide SCALE ,ko tir 10 mi les „o 16 kilometers 3:1-Cf®-C---) \22 21 ,C4irthage "--x 12.1 ® R) 19. : 18 "22 s.%... 17 , ls Caw
® ®
Joplin Creek. " 43Monett Neosho MISSOURI PROJECT AREA Figure 12.--Wells 'sampled in 1965, 1976, and 1978, and springs sampled in 1978 in Spring River, Center Creek and Shoal Creek drainage basins, Missouri
type, and concentrations of iron and zinc average 5,100 and 9,400 pg/L (micrograms per liter), respectively. Analyses of water samples collected from wells and springs during the 1978 study are listed in table 2. A comparison of the analyses obtained in 1965, 1976, and 1978 is shown in table 3. Comparison of median sulfate values for the three sampling periods best illustrates the difference in sample distribution. The difference is probably due to the widespread occurrence of sulfide minerals in the rocks of the mining district, their sporadic occurrence in the remainder of the area. Other parameters show geographic variations but they are not as marked. The median value of nitrate (as N) in 1978 is 2.7 mg/L (milligrams per liter) compared with 1.0 mg/L in 1965. This does not necessarily mean that groundwater pollution is greater in 1978 than it was in 1965 because the geographic distribution of samples was different at the two times. Figure 13 shows the distribution of values less than and greater than 2.3 mg/L of nitrate (10 mg/L as NO3) reported as nitrogen (N). Many of the low nitrate values obtained in 1965 were located west of Grove Creek. In 1978 values are in excess of 2.3 mg/L (as N) in a majority of rural domestic wells. Forty-seven percent of the samples collected in 1965 had more than 2.3 mg/L of nitrate (as N) whereas 65 percent of those collected in 1978 exceeded 2.3 mg/L. Only one of 20 samples collected in 1978 exceeded 10 mg/L (as N), the drinking water limit established by the Environmental Protection Agency (1975), whereas 5 of 39 samples collected in 1965 exceeded that limit. Inasmuch as the Mississippian limestone is exposed at the surface or underlies residuum, the opportunity for downward migration of waste exists. In the rural areas where pasture, stock raising, and fertilizing of crops are extensive and domestic waste is disposed of by means of septic tanks, the source of pollution is present. In the urban areas farming is less extensive and septic tanks are fewer. In suburban areas, between the urban areas and the farming areas, many septic tanks exist and the number of homes is increasing. These are areas where the nitrate content of the water may be expected to increase in the future. DIGITAL SIMULATION MODEL When the stage of a reservoir rises above the water table in adjoining aquifers water flows from the reservoir into the aquifers. This water may form a "mound" in the potentiometric surface that did not exist in the aquifers before the reservoir stage rose. The natural ground-water flow system may adjust to this "mound" by diverting flow to new discharge areas, increasing water stored in the aquifer or decreasing the rate of recharge. The changes that occur in the natural flow system depend on the hydraulic properties of the aquifer, types and location of aquifer boundaries, amounts
EXPLANATION 0 2.3 mg./1. Nitrate 2.3 mg./1. Nitrate 94° od Drainage Divide U) SCALE 10 miles 16 kilometers 0 0° 0 (10 Joplin et Neosho Monett s , MISSOURI
PROJECT AREA Figure I 3.-- Variation in nitrate content in water from wells in Mississippian limestone
TABLE 2.--WATER-QUALITY DATA FOR WELLS AND SPRINGS IN CENTER CREEK BASIN, MISSOURI [WELL NOS. 5, 13, AND 18 ARE IN ORDOVICIAN, WELL NO. 23 IS IN CAMBRIAN, ALL OTHER WELLS ARE IN MISSISSIPPIAN. SPRINGS ARE ALL IN MISSISSIPPIAN.] SPECIFIC HARDMAGNEPOTA5MAP DEPTH CONHARD- NESS, CALCIUM SLUM, SODIUM, SLUM, NO. DATE OF DUCTNESS NONCAR- DIS- DIS- DIS- DIS- (FIG. OF WELL, ANCE PH TEMPER- (MG/L BONATE SOLVED SOLVED SOLVED SOLVED 12) STATION NUMBER SAMPLE TOTAL (MICROATURE AS (MG/L (MG/L (MG/L (MG/L (MG/L (FEET) MHOS) (UNITS) (DEG C) CAC03) CAC03) AS CA) AS MG) AS NA) AS K) 1 365748093535601 78-06-14 2 365531093524901 78-06-13 3 365914093550701 78-06-14 365927094033701 78-06-14 1240 5 370044094075901 78-06-20 8,0 370044094075902 78-06-20 7 370106094164101 78-06-22 lb 8 370136094043801 78-06-20 9 370157094223001 78-06-22 7,5 10 370158093582401 78-06-15 11 370255094071701 78-06-14 12 370320094131901 78-06-20 13 370436094205701 78-06-21 1k 370552094240501 78-06-15 15 370604094185101 78-06-13 16 370654094133201 78-06-15 17 370730094213001 78-06-14 18 370734094183501 78-06-14 19 370826094213801 78-06-15 20 370829094230701 78-06-14 370953094250101 78-06-14 370848094161601 78-06-13 370955094215601 78-06-13 7,5
TABLE 2.--WATER-QUALITY DATA FOR WELLS AND SPRINGS IN CENTER CREEK BASIN, MISSOURI--CONTINUED SOLIDS, SOLIDS, NITROCARBON CrtLOFLUOSILICA, RESIDUE SUM OF GEN, PHOS RICARALKADIOXIDE SULFATE RIDE, RIDE, DISAT 180 CONSTINO24403 PHORUS, DATE BONATE CARLINITY DISDISDISUISSOLVED DEG. C TUENTS, DISDIS MAP OF (MG/L BONATE (MG/L SOLVED SOLVED SOLVED SOLVED (MG/L DISDISSOLVED SOLVED NO. (FIG. SAMPLE AS (MG/L AS (MG/L (MG/L (MG/L AS SOLVED SOLVED (MG/L (MG/L HCU3) AS CO3) CACO3) AS CO2) AS 504) AS CL) AS F) SI02) (MG/L) (MG/L) AS N) AS P) 12) 1 78-06-14 2 78-06-13 3_78-06-14 4 78-06-14 5 78-06-20 6 78-06-20 7 78-06-22 8 78-06-20 9 78-06-22 10 78-06-15 9,8 11 78-06-14 9,0 1,1 12 78-06-20 13 78-06-21 14 78-06-15 15 78-06-13 16 78-06-15 17 7d-06-14 18 78-06-14 ?6 19 78-06-15 es 20 78-06-14 21 78-06-13 u 22 70-06-14 23 78-06-13
TABLE 2.--WATER-QUALITY DATA FOR WELLS AND SPRINGS IN CENTER CREEK. BASIN, MISSOURI--CONTINUED MANGACADMIUM COPPER, IRON, LEAD, NESE, ZINC, MAP DATE DISDISDIS DIS DISNO. OF SOLVED SOLVED SOLVED SOLVED SOLVED SOLVED (FIG. SAMPLE (UG/L (UG/L 12) AS CD) AS CU) (UG/L AS FE) (UG/L AS PB) (UG/L AS MN) (UG/L AS ZN) OM OM MO 2 78-06-13 O00 MOO OM OM OM MO MO 4 78-06-14 MO MI. MO OW ND IRO MO OW 0 MO OM figo MO ONO 6310 6 78-06-20 OM MOM 7 78-06-22 MO 1M M. 8 78-06-e0 MO 10 78-06-15 9 78-06-22 11 78-06-14 12 78-06-20 on am WI MI 13 78-06-21 S 15 78-06-13 MO eV MOP Oa .11 OM 16 78-06-15 MOO MO 17 78-06-14 MOO 19 78-06-15 20 /8-06-14 OS MI MOON On. MO MO MO 21 78-06-13 S MO OW MO 22 78-06-14 ONO MO MO
TABLE 2.--WATER-QUALITY DATA FOR WELLS AND SPRINGS IN CENTER CREEK BASIN, MISSOURI--CONTINUED SPELIFIL LONHARDMAP DATE DUCTNESS NO. (FIG. 12) STATION NUMBER STATION NAME OF SAMPLE ANCE (MICROMHOS) PH TEMPERATURE (UNITS) (DEG C) (MG/L AS CAC03) IS 370150094050501 27N-29w-27ACB1 HADDOCK SPRING 2S 370255094002101 27N-28w-17DDA1 CLARKSON SPRING 35 370426094184401 27N-31w-100381 FIDELITY SPRING 4S 370442094101401 27N-30w-11AAB1 DUKARTS SPRING 5S 370533094225101 SCOTLAND SPRING, ATLAS POWDER COMPANY. HARDMAGNEPUTASCARbuN CHLOFLUONESS, CALCIUM SIUm, SODIUM, SIUM, BACAR ALKADIWIDE SULFATE RIDE, RIDE, MAP DATE NO. OF (FIG. SAMPLE 12) NONCARBONATE (MG/L CAC03) DISSOLVED (MG/I. AS CA) DISSOLVED (MG/L AS MG) DISSOLVED (MG/L AS NA) DISSOLVED OWL AS K) BONATE (MG/L AS. HCO3) CARHoNATE (MG/L AS CO3) LINITY (MG/L AS CACU3) DISSOLVED (MG/L AS CO2) DISSGLVED (MG/L AS SO4) DISSOLVED (MG/L AS CL) DISSOLVED (MG/L AS F) 1S 78-06-21 2s 78-06-21 35 78-06-21 45 78-06-21 4,1 0 1,2 5S 78-06-22 SOLIDS, SOLIDS, NITROSILICA, RESIDUE SUM OF GEN, PHOS DISAT 180 CONSTINO2+NO3 PHORUS, 1RUN, MAP DATE SOLVED DEG. C TUENTS, DISDIS D1SNO. OF (MG/L DISDISSOLVED SOLVED SOLVED (FIG. 12) SAMPLE AS SOLVED SOLVED SI02) (MG/L) (MG/L) (mG/L. AS N) (MG/L AS P) (OWL AS FE) 1S 2S 3S L'S 5S
Table 3.--Comparison of analyses of water samples collected in 1965, 1976, and 1978, from Mississippian wells in the Joplin area, Missouri (units are milligrams per liter, except as indicated) Character or constit- uent Zinc Ca/Mg ratio Sulfate Year 1965 No. of values-- 38 Median-- VA Range--- Character or constit- uent Chloride Nitrate plus nitrite as N Potassium Year 1965 1965 a No. of values-- 39 Median-- 4.1 Range---
Table 3.--Comparison of analyses of water samples collected in 1965, 1976, and 1978, from Mississippian wells in the Joplin area, Missouri--continued Character or constituent Year Sodium Dissolved solids 'residue at 180 °C Hardness No. of values Median--- 7.5 Range 3.0-106 Character or constituent Year pH (field) No. of values Median Range--- 6.1-8.3 a1965 values nitrate only.
and location of recharge and discharge, and on the amount and timing of the change in stage of the reservoir. Because the changes in the natural flow system can be complex, this flow system must be quantitatively understood to predict the total effects of a rise in stage of a reservoir. However, the "mound" that a rise in reservoir stage will cause in an adjoining aquifer can be estimated from less compre hensive data. Such an estimate provides a useful basis from which further studies can be planned to more fully evaluate the effects of the "mound" on the natural flow system. The ground-water mound that could form in the shallow aquifer if Prosperity Reservoir is built on Center Creek was evaluated with a digital model. The simulation model assumes two dimensional ground-water flow. The computer program used for this analysis has been documented by Trescott (1976). Finite-Difference Grid This analysis requires that the study area be subdivided into a rectan gular, block-centered, finite-difference grid. The modeled area which includes the Center Creek basin was subdivided into a finite-difference grid having 37 rows and 52 columns. A variable grid spacing was used so that the grid would be finer in the vicinity of the proposed reservoir. The overall dimensions of the grid were 49 in. by 29.7 in. The scale of the grid was I:62,500. (See figure 14.) By convention, nodes are located at the centers of the cells of the grid. Any specific node or cell may be referenced by citing its row and column location. Boundary Conditions and Hydraulic Stresses All of the perennial streams were modeled as constant-head boundaries. Spring River and Shoal Creek, both perennial streams, bound the modeled area on the north and south sides, respectively. The east and west sides of the area were modeled as no-flow boundaries. The area of interest, Prosperity Reservoir, is far enough away from the east and west boundaries to be unaffected by assuming the no-flow boundaries when the head change is imposed in Prosperity Reservoir. Sites of known mine discharge in 1965 were represented in the model by specifying a constant flux at the corresponding nodes. Pumpage of large amounts of water from the shallow aquifer (as occurred in 1965) caused the head in the shallow aquifer to be lower than the head in the deep aquifer causing upward leakage through the confining bed. In
TVIN T2, T 2, ,,, N T 2 7 35. li* es. Use FROM U.S. dEOLOQCALSuRYEY 433W 432W 433W r0°. *54i5 01558.1, 500. SCALE EPLANATI.N vs a Miles NOTE e Kile4MOMS Line of teal head change 11963- TS 1. Contour interval 25 feet. Rows 9-32 and columns 7-32 of the fini fa-difference arid are numbered an thill Cells within the shaded Orea were assigned 0 fronennesnntY Computed hne of equal head dove 0965-781. Contour intervoi 25 feet. of 1,000 f1/c1, oil other cells were assigned a value of 100 feid. 0,5 Computed line of equal head change that 1naY 0000 Los to Prosperity Reservoir. Contour m nfarval variable, in Turkey Creek and Grove Creek are mown only from the beginning of perenmai 11ow wnere mocleled as constant head bounder les. feet. Spring River, Center, Jones, and Shoal Graeae are modeled as constant head boundaries. Figure 14.--Observed and computed head change (1965-1978) for the Oronogo-Duenweg area, and projected head change that may occur due to Prosperity Reservoir
the model the confining layer was assigned a uniform thickness of 10 ft. Initially the vertical hydraulic conductivity assigned to the confining layer was 1.0X10- ft/s. The initial vertical hydraulic conductivity used was determined from a water-resources study in the Springfield area, Missouri (Emmett and others, 1978). This value was later changed to 0.5)(10-9 ft/s by calibration. Aquifer Properties One of the aquifer properties needed for the simulation is a value for transmissivity. The transmissivity of an aquifer reflects the rate at which ground water of the prevailing kinematic viscosity will flow through a unit width of the aquifer under a unit hydraulic gradient (Lohman and others, 1972). The area modeled was divided into a high and a low transmissivity area on the basis of maps showing the distribution of breccia areas in the vicinity of Joplin, Mo. (Missouri Geological Survey and Water Resources, 1922), and on the distribution of well yields in the area. No aquifer-test data were available for the shallow aquifer in the Joplin area. However, transmissivity of the brecciated area in the,southern part of the Oronogo-Duenweg belt was estimated to be 2,000 ft2/d. The estimate was by the closed-contour method as described by Lohman (19725 p. 46-49). The data used were a water-table contour map and discharge data collected in 1965. On the basis of well-yield data, it is estimated that the low transmissivity area is probably an order of magnitude lower than the brecciated area. Time-dependent simulations require a value for storage coefficient for the aquifer. The storage coefficient is the volume of water an aquifer releases from or takes into storage per unit of surface area of the aquifer per unit change in head (Lohman and others, 1972). Values for storage coefficient are not available for the shallow aquifer in the Joplin area. Feder and others (1969, p. 27) do indicate that artesian conditions occur in the nonbrecciated areas of the shallow aquifer and that water-table conditions occur in the brecciated areas. Calibration of the Model To demonstrate that the simulation model is realistic, field observa tions of the aquifer must be compared with corresponding simulations using the model. The field data used were a head change map from 1965-78 (fig. 14). In 1965 seven mine shafts were being pumped (table 4). In 1978 none of the mines were being pumped. In order to simulate the head change map, a steady-state model was used in which the transmissivity of the brecciated area was estimated as 2,000 ft2/s9 and the transmissivity of the rest of the
Table 4.--Summary of mine discharges represented in the model Discharge Mine Node (ft3/s) Athletic 27, 16 George H. 24, 12 Hyde Park 26, 16 Ice Plant 20, 9 King William 28, 16 Kramer 34, 4 St. Regis 28, 17 Total
area wa estimated as 200 ft2/s. A vertical hydraulic conductivity of 1.0X10- ft/s was used for the confining layer. This resulted in an insufficient head change. Several simulation trials tested different combinations of reduced transmissivity. The final selection resulted in a reduction in the value used for transmissivity in both the brecciated and nonbrecciated areas (1,000 ft2/s and 100 ft2/s, respectively). The model was calibrated in the mined area where dewatering had taken place. It was not possible to calibrate the model in the area of the proposed reservoir. Consequently, the value of the calibration is dependent upon the similarity of the transmissivity of the nonbrecciated area near the mines to the reservoir area. After mining had ceased following World War II, pumping from the mines by industries was negligible. In the early 1960's the chemical industry began to pump mine water for their operations. Two small short-lived mining developments (George H. and Hyde Park) started up in the 1963-65 period. Water supplies for two gravel-washing operations were obtained from mines. In all, seven shafts were pumped, but only one (the Hyde Park) was pumped for the purpose of dewatering. The next step in the calibration procedure was to simulate a mine hydrograph which showed the effects of mine dewatering. The hydrograph was from a mine that is 11/2 mi from the mine being dewatered (Feder and others, 1969, p. 25). This time-dependent model required a value for the storage coefficient of the shallow aquifer. Several simulation trials tested different combinations of storage coefficient. A storage coefficient of 0.0001 in the nonbrecciated area and 0.001 in the brecciated area gave the best fit between the observed and simulated hydrograph. To get a closer fit, several simulations were then made using different values for the vertical hydraulic conductivity pf the confining layer. A vertical hydraulic conductivity of 0.5X10y ft/s was finally chosen as giving the best fit (fig. 15). The steady-state model (step one) was then recalibrated using the reduced value for vertical hydraulic conductivity. Transmissivity values of 100 ft2/d in the nonbrecciated area and 1,000 ft2/d in the brecciated area still gave the best fit for the change map (fig. 14). A time-dependent simulation was made imposing the head change on those nodes that would underlie the conservation pool of the lake. These nodes are treated as constant-head boundary cells. The equilibrium simulated head change in the shallow aquifer caused by construction of the lake is shown in figure 14. The head change projected by the reservoir assumes Grove Creek is a fully penetrating drain on the aquifer. Two additional simulations were made, In one simulation the storage coefficients were each increased an order of magnitude. In the other simulation the transmissivity values were each increased five times. Figure 16 compares the results of these two simulations with the initial simulation. A ten-fold increase in the storage
Ui DRAWDOWN . N'N e ., 1 N. N
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,..
'N
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1 1
4
150 210 2 0 .0005 & .005 S .00025 a .0025 KI=1.0 0 f Us S=,0001 & .001 Observed drawdown in Nowata shaft 16 0.5 x 10-9 ft/s 012 x10 ft/s --161.0x1610 ftis E X PLANATION S... Storage coefficient of shallow aquifer - ie= 0 K'— Vertical hydraulic conductivity of confining layer 0 60 120 180 240 300 DAYS SINCE PUMPING STARTED Figure 15.-- Simulation of hydrograph
I I I III1 1 1 1 ETIET 1 I 1 [MI EXPLANATION T Transmissivity of shallow aquifef Storage coefficient of shallow aquifer T=100 ft% B 1000 ft /d NOTE : Vertical hydraulic conductivity S=.001 & .01 of confining layer is a 0,5 x169 ft/s for all
C,) three simulations. 500 ft% & 5000 ft% es .0001 & .001 v away. *dam.
100 ft2/d & 1000ft3'd z Figure 16.-- Computed increase in storage due to construction of Prosperity Reservoir
coefficient results in a ten-fold increase in the amount of water that goes into storage and a longer time (about 11 years) for the cone of impression ("mound") to stabilize than in the initial simulaiton. In the initial simulation the cone of impression stabilized in about 1.4 years. The simu lation in which transmissivity was increased resulted in about a two-fold increase in the amount of water that went into storage; however, the cone of impression stabilized in the same time as the initial simulation. SUMMARY AND CONCLUSIONS Major aquifers in the study area consist of a shallow limestone aquifer of Mississippian age, which underlies the proposed reservoir, and a deep dolomite aquifer of Cambrian and Ordovician age. The two aquifers are separated throughout 90 percent of the area by about 10 ft of low permeability shale. In some localities west of Grove Creek, solution activity was great enough to result in the development of permeability estimated to be an order of magnitude higher than that developed east of Grove Creek. Grove Creek lies near the eastern margin of the Oronogo-Duenweg belt where secondary permeability is estimated to be high. The potentiometric surface in the shallow aquifer slopes with some irregularity from east to west and intersects Spring River and Center Creek at several places, and Grove Creek. The potentiometric surface in the deep aquifer is usually 50-200 ft below that of the shallow aquifer. Major discharge points of ground water from the Mississippian limestone aquifer to the streams lie along Center Creek and the lower reach of Grove Creek. Water in the Mississippian limestone is moderately mineralized. Ground water from the mining belt generally contains more than 1,000 mg/L dissolvedsolids concentration, is a calcium sulfate type, and concentrations of iron and zinc average 5,100 and 9,400 pg/L, respectively. A model study of the area surrounding the proposed reservoir indicates that water will flow from the reservoir into the adjoining aquifer and from a mound in the potentiometric surface. The mound will be about 20 ft high near the reservoir and extend to the southern part of the Grove Creek basinwhere it will be only 0.5 to 1 ft high. Any increase in ground-water altitude could result in increased discharge to Grove Creek or perhaps to the Oronogo-Duenweg mining belt. Also, the natural flow system will adjust to the mound by diverting flow to new discharge areas, increasing storage, or decreasing the rate of discharge. The increase in ground-water discharge to Grove Creek will have the beneficial effect of diluting mine-water discharge at Mineral Branch during periods of low flow.
The adjustment of the natural flow system to the mound in the potenti ometric surface caused by the proposed reservoir has not been evaluated. Additional work is necessary to evaluate this response, its possible effects on flow to and from the Oronogo-Duenweg belt, and the contribution of mineralized water to Center Creek. 1. Additional field data are needed to better define the aquifer characteristics, aquifer boundaries, and the properties of the confining beds. Detailed seepage runs should be made on Grove Creek and a dye trace should be made to-confirm a connection between Grove Creek and Scotland Spring and to help evaluate the efficiency of Grove Creek as a hydraulic boundary. To define the vertical hydraulic conductivity of the confining beds would require tests with observation wells completed above and below the confining beds. 2. These field data need to be analyzed through additional model runs to determine the maximum possible area that could be affected by the proposed dam. Such an analysis will help evaluate the possibility that the proposed dam might increase the flow of mineralized water from the Oronogo-Duenweg mining belt to Center Creek. 3. A monitoring network should be designed and put in operation so that background conditions of flow, altitudes of water levels, and water quality can be established prior to dam construction. 4. Measurements of natural flow in Grove Creek downstream from Scotland Spring, taking into account the quantity used by industry correlated with the flow lost from the upstream reach, would help to corroborate the results of a dye trace and establish Grove Creek as an effective hydrologic boundary.
REFERENCES CITED Anderson, K. FL, 1979, Geologic map of Missouri: Missouri Department of Natural Resources, Division of Geology and Land Survey, 1 sheet, scale, 1:500,000. Barks, J. H., 1977, Effects of abandoned lead and zinc mines and tailings piles on water quality in the Joplin area, Missouri: U.S. Geological Survey Water-Resources Investigations 77-75, 49 p. Brockie, D. C., and others, 1968, The geology and ore deposits of the Tri-State District of Missouri, Kansas, and Oklahoma, in Ore deposits of the United States 1933-1967, the Graton-Sales volume: American Institute of Mining, Metallurgical, and Petroleum Engineers, p. 400-430. Buckely, E. R., and Buehler, H. A., 1906, Geology of the Granby area: Missouri Bureau of Geology and Mines, 2d ser., v. 4, 120 p. Emmett, L. F., Skelton, John, Luckey, R. R., and Miller, D. E., 1978, Water resources and geology of the Springfield area, Missouri: Missouri Department of Natural Resources, Division of Geology and Land Survey, Water Resources Report 34, 160 p. Feder, G. L., Skelton, John, Jeffery, H. G., and Harvey, E. Jo, 1969, Water resources of the Joplin area, Missouri: Missouri Geological Survey and Water Resources, Water Resources Report 24, 97 p. Harvey, E. J, and Maxwell, J. A., 1965, Use of abandoned mines as potential water resources, Joplin district, Missouri: Abstract, Mining Engineering, v. 17, no. 8, p. 51. Howe, W. B„ coordinator, Koenig, J. W., editor, 1961, The stratigraphic succession in Missouri: Missouri Geological Survey and Water Resources, 2d ser., v. 40, 185 p. Lohman, S. W., 1972, Ground-water hydraulics: U.S. Geological Survey Professional Paper 708, 70 p. Lohman, S. W., and others, 1972, Definitions of selected ground-water terms--Revisions and conceptual refinements: U.S. Geological Survey Water-Supply Paper 1988, 21 p. Missouri Geological Survey and Water Resources, 1922, Economic geology maps of the Joplin district, T. 27-29 N., R. 32-34 W., Jasper and Newton Counties. Scale 4 inches=1 mile. Revised 1942. Six sheets.
Robertson, C. E., 1966, The Elsey Formation and its relationship to the Grand Falls chert: Missouri Geological Survey and Water Resources, Report of Investigations 38, 62 p. Rutledge, R. B., 1929, Geologic map of Lawrence County and parts of Newton and Jasper Counties: Missouri Bureau of Geology and Mines. Scale, 1 inch=l mile. smith, W. S. T., and Siebenthal, C. E., 1907, Joplin district (Missouri-Kansas): U.S. Geological Survey Atlas, Folio 148. Trescott, P. C., Pinder, F. G., and Larson, S. P., 1976, Finite-difference model for aquifer simulation in two dimensions with results of numerical experiments: U.S. Geological Survey Techniques Water-Resources Investigations, book 7, chap. Cl, 116 p. U.S. Army Corps of Engineers, 1976, Prosperity Lake--plan of study: U.S. Army Corps of Engineers, Tulsa District 9 p. U.S. Environmental Protection Agency, 1975, National interim primary drinking water regulations: Federal Register, v. 40, no. 2489 Wednesday, December 24, 1975, Part IV, p. 59566-59587.